NYSGA 1956
GUIDEBOOK FOR FIELD TRIPS
IN
WESTERN NEW YORK
MAY 4-6, 1956
TWENTY EIGHTH ANNUAL MEETING
NEW YORK STATE
GEOLOGICAL ASSOCIATION
AT THE
UNIVERSITY OF ROCHESTER
ROCHESTER, NEW YORK

1A: SILURIAN STRATIGRAPHY, GEOMORPHOLOGY
by U of R Students and Staff
The two stops on this trip will afford an opportunity to study the classic Lower and Middle Silurian stratigraphic section of the Rochester area. The route to and between the stops passes many features related to the glacial history of the region (see pp. 47-60) and to the history of the Genesee River (see pp. 5-8).

1A: SILURIAN STRATIGRAPHY, GEOMORPHOLOGY

Post-glacial Genesee
Zero mileage (headed south) at River Boulevard entrance to main quadrangle of U of R River Campus. Erratic anorthosite boulder opposite entrance, With polished and striated surfaces, bears bronze tablet inscribed with "The Genesee", alma mater of the University of Rochester. Proceed south on River Boulevard. River here is in post-glacial course (see p. 8).

West end of Pinnacle Range
For first 3.5 miles, route nearly parallels the Pinnacle Range (see p. 56) of kame moraine hills. Route is on outwash plain and lake beds. U of R Campus is on west end of range.

Mt. Hope Cemetery
Mt. Hope Cemetery to left (N). Northwestern portion of cemetery, adjoining campus, is an area of spectacular kame and kettle topography.

View of Pinnacle Range
View to left (N) of Pinnacle Range, now about a half-mile to the north.

Colgate-Rochester Divinity School
Enter town of Brighton. Colgate-Rochester Divinity School on crest of Pinnacle Range to left (N).

Highest point on Pinnacle Range
Highest point on Pinnacle Range (749 feet) is just west of radio and telephone towers visible here to the left (N).

Pass over Rochester subway
Pass over Rochester subway, in abandoned bed of early Erie Canal.
Now occupied by Interstate 490...

Lockport Dolomite
Pass under New York Central main line. Outcrops are Lockport dolomite showing characteristic pitted and pocketed surface weathering.

Irondequoit Valley
Flat bottom of Irondequoit Valley (e1ev. 270 feet). Valley is part of preglacial Genesee Valley (see p. 7) which here was filled with morainal debris and Lake Iroquois (see p. 54) sands, then re-excavated by post-glacial Irondequoit Creek. Bedrock, till and lake deposits are exposed at places along valley sides; local sand and gravel workings in glacial material and lake beds. Valley slopes marked by several terraces representing levels of Lake Iroquois. One terrace (at 400 feet) visible here forms flat valley rim.

View of Rochester
View to left (w) to Rochester over Irondequoit Valley and in line with Pinnacle Range which is prominent elevation.

Orchards
Next six miles. Orchards here are part of extensive apple and peach belt south of Lake Ontario.
2010: Orchards are now pretty much gone, replaced by suburban sprawl...

STOP 1. Penfield Quarry
Penfield Quarry of the Dolomite Products Co.
The Lockport dolomite is a hard, dark gray, dolomitic limestone, with considerable quantities of disseminated argillaceous matter. A fine to coarse sugary texture and strong petroliferous odor when struck with a hammer are characteristic. The formation is about 180 feet in total thickness, of which about 42 feet are exposed in the quarry wall. The Lockport underlies much of the city of Rochester. It has been used as a building stone but weathers with moderate rapidity. The sometimes fantastically shaped and sculptured blocks resulting from solution by subsurface water are commonly used for ornamental stonework in local gardens. Commercially the rock finds its greatest value today as crushed stone, for which it is quarried in two large quarries operated hy the Dolomite Products Company just outside of Rochester, and by smaller concerns at other localities along its outcrop belt.
Bedding is massive; fossils occur in some layers but are not usually well preserved. Solution cavities and stylolites are common. In the upper levels of the Penfield quarry many of the secondary cavities are filled with crystallized dolomite and other minerals; small fissures may be filled with sphalerite, gypsum, or galena, and residual hydrocarbons occur. For greater detail see comments under Field Trip No. 3C; on that trip there will be opportunity to collect from blocks of the mineral-bearing strata.

Lake Iroquois bar
Ridge Rd. goes to right (E) on Lake Iroquois bar which is inconspicuous here. See mileage 25.5.

Barrier bar
East end of barrier bar carrying road across mouth of Irondequoit Bay which occupies part of re-excavated pre-glacial Genesee Valley.

West end of barrier bar.

Durand-Eastman Park
Durand-Eastman Park, Rochester's largest public park, is in an area of glacial till veneered with Lake Iroquois deposits. The terrane has been dissected deeply by a number of small and closely spaced post-glacial streams which flow directly into Lake Ontario or into narrow inter-divide lakes now sealed from Lake Ontario by massive barrier bars. The Lake Ontario surface is at 246 feet. The crests of the divides increase gradually in elevation southward from about 300 feet a little south of the lake shore to 375 feet two miles farther south.

Two barred lakes
Public bath house to right (N). Two barred lakes south of road.

Narrow divide
For 1.4 miles route follows narrow divide between steep-sided valleys. Note accordant divides (Lake Iroquois bottom) at about 375 feet.

Bottom of Lake Iroquois.
Next mile: Cross near-shore bottom of Lake Iroquois.

Offshore bar
Road is atop offshore bar of Lake Iroquois.

Lagoon
Note lower ground to left (S), lagoon behind barrier bar.

Stop sign. Traffic circle.
Stop sign. Traffic circle. Take third street to right (first one past bridge) where sign says "Norton St. Traffic Turn Here".
2010: Traffic controls are much different now, but this path takes you to Norton Street.

Private Road
Gateway to entrance to Rochester Gas and Electric Company private road to power plant. Park.

STOP 2. Rochester Gorge.
Exposures along private road to Rochester Gas and Electric Company power plant, and in banks of Genesee Gorge.
Bedrock.--Exposures in the new road cut extend from the Queenston shale to the Reynales limestone (Clinton group). Strata above the Reynales, up to the basal few feet of Rochester shale are exposed in the gorge wall below the Hawk-Eye plant of Eastman Kodak Company.
The contrasting lithologic types exposed in the road cut exhibit a variety of sedimentary features reflecting diverse environments (see pp. 9-15). The accessible section here is not generally fossiliferous, beds of Pentamerus coquina provide the best collecting possibilities.
The thin Thorold sandstone forms the lower falls of the Genesee at the power plant, just south of Driving Park Avenue bridge. The middle falls, a short distance farther upstream is formed by the Reynales limestone. The upper falls, not visible from this locality, is over beds in the lower part of the Lockport dolomite.
The accompanying stratigraphic section is based on exposures in this vicinity.
Gorge.--The river gorge here (200 feet deep at this point) is a result of post-glacial erosion. The pre-glacial course at this latitude lay several miles to the east in what is now the valley of Irondequoit Bay and Creek. See page 5 for river history.
Unconsolidated material.--Above the Silurian strata in the upper portion of the road cut are exposed four distinct types of unconsolidated materials with a cumulative thickness of approximately 25 feet and length of exposure of 200 feet. The exposure of these deposits is bounded on the northeast by a graded slope and on the southwest by an undisturbed vegetative covering. The exposure strikes N60°E.
Lowermost of these unconsolidated units at the head of the road cut is a 4- to 5-foot layer of reddish till lying on striated and highly polished Reynales limestone. Striations on the limestone surface strike N 85°E, an anomalous direction for this region. The red till contains striated and well worn pebbles with relatively little sharply angular material. Components of the till range in size from small boulders to clay sized particles, no stratification is apparent. The materials are extremely fresh without visible alteration of any type. Fabric studies of this till show a distinct northwest-southeast preferred orientation of the long-diameter of pebbles.
This unit of unconsolidated sedimentary material extends from the head of the road cut for a distance of 120 feet toward the southwest. At this point it terminates abruptly against Sodus shale, the next stratigraphic unit above the Reynales Formation.
Immediately overlying the red till and in marked contrast to it in the northwest portion of the sequence is approximately 10 feet of highly modified, bouldery material in a jumbled mass. Percolating ground water solutions have altered or disintegrated all types of rock and material, coating and replacing material with various iron oxides. Contained within this unit at a point 100 feet from the head of the cut is a lens or nest of stratified sand 8 feet wide and with a maximum thickness of 2 feet. Any other primary textural or structural modifications within this unit have been destroyed by the alteration of the material. This altered material bevels across the red till-shale contact and, in part, lies directly on the Sodus shale.
At a point about 110 feet southwest along the exposure another type of material wedges in below the highly weathered sediment and overlies the Sodus shale. This is a brown sandy unit containing blocks of limestone and other coarser material along with small lenses and stringers of sand. Weathering of this material has been limited to various stages in the alteration and disintegration fragments into patches of yellow-brown residium. Thickening of this member increases to the southwest at the expense of the highly altered material which correspondingly pinches out in the same direction.
Lying above and again sharply contrasting with the underlying material is 10-15 feet of ashy rubbish exposed throughout the cut. This represents the remains of a city dump. The thickness of this material lessens to the southwest; solutions from it may, in part, account for the alteration of the underlying material.

Lunch Stop
LUNCH STOP at park pavilions. End of trip

1B: GLACIAL GEOLOGY
by U of R Students and Staff
Stops on this trip will be in the Mendon Ponds kame and kettle area (see p. 55) and on the Pinnacle Range of kame moraine hills (see p. 56). The trip ends adjacent to the post-glacial lower gorge of the Genesee River.

1B: GLACIAL GEOLOGY

Drumlins
Note drumlins elongated parallel to N.Y. 65 both east and west of the route.

STOP 1. Gravel pit in kame moraine
Gravel pit in kame moraine, exposing features typical of such deposits in this area. Lenses of sand and gravel show great variety of sedimentary features. The sediments are displaced along small normal faults in places. The gravel lenses tend to be cemented with calcareous material probably derived from pebbles and cobbles of Lockport dolomite. Most abundant pebbles are of red Grimsby sandstone; however, representatives of all formations of the local Lower and Middle Silurian section can be found. In addition there are Ordovician limestones (some fossiliferous) and crystallines from Canada.

STOP 2. Mendon Ponds County Park
In Mendon Ponds County Park are to be seen excellent examples of kame hills, kettles, eskers, and lakes and swamps in poorly drained morainal ground. For general glacial history see pages 47-60; for more specific comments on this park, see page 55. There are two prominent eskers in the park, one east and one west of Hundred Acre Pond which is the largest of several ponds. The recognizable portion of the western esker extends, with only slight interruptions, for a little over two miles. The group will walk along about 0.3 mile of this esker, from a point behind (S) of the park buildings to a conspicuous kettle known as Devil's Bathtub, at which point the esker deposits fan out, apparently at the mouth of the stream responsible for the deposit.

Swamp
Swamp-filled depression to left (N) here continues north to Hundred Acre Pond

Kame-kettle area
Next 1.2 miles. At sharp left curve begins extensive kame-kettle area east of Hundred Acre Pond depression

Eastern esker
Steep slope east (right) of route is eastern esker. Hundred Acre Pond to left (W).

Western esker
Road crosses small swampy area here, then rises abruptly, cutting through the western esker at point about 0.8 mile north of where group climbed upon it at Stop 2.

STOP 3. Cobbs Hill
Cobbs Hill is the easternmost prominent hill of the Pinnacle Range (see p.56). In clear weather an excellent view may be obtained from here. Water elevation 633 feet, about 130 feet above plain to north and south. Water in reservoir is from Hemlock Lake, about 30 miles south of Rochester. To south lie outwash plains and glacial lake beds, with occasional drumlins. Bedrock hills (Bristol Hills, Middle Devonian) rise in distance; Onondaga escarpment not prominent here. To north lies city of Rochester on thin veneer of lake beds and till above Lockport dolomite and Rochester shale. Lake Ontario in distance. To west Pinnacle Range continues toward U of R River Campus. Radio and telephone towers are on the Pinnacle, highest of the Pinnacle Hills, just east of summit.

Pinnacle Range
Route follows along south foot of Pinnacle Range.

STOP 4. Quarry in Pinnacle Range kame moraine.
Sand and gravel quarry in Pinnacle Range kame moraine. The lower part of the cut exposes uniform, well-sorted and stratified sands; bedding southwest at 25~28 degrees. At the upper part of the cut there is a thin covering of till, evidencing brief ice re-advance after kame formation. Fabric studies of the orientation of the long axes of pebbles in the hill show, at the east end of the exposure, an 11% concentration with a plunge of 10 degrees and a southward strike, and at the west end, a dominant plunge of 20-25 degrees and strike concentration in the sector from S30°W to S15°E. The low ridge bordering the ball park on the northwest (old cemetery beyond the concessions stand) is also composed of till.

Erie Canal bed
Cross Rochester subway in old Erie Canal bed.
2010: All is changed, but the path here still takes you close to what the road log says.

Lunch Stop
LUNCH STOP at park pavilions. Park is on east bank of lower gorge (postglacial) of the Genesee River downstream from lowest falls. See pages 4-8. END OF TRIP lB

1C: TOUR OF KODAK PARK
by U of R Students and Staff
Kodak Park, the main plant of the Eastman Kodak Company, is located at Ridge Road and Lake Avenue, a short distance west of the Genesee Gorge opposite Seneca Park. Buses will proceed from the lunch stop directly to Kodak Park via the Veterans' Memorial Bridge (Ridge Road, U.S. 104). After the tour, buses will return directly to the U of R River Campuso
No road log

2: DEVONIAN STRATIGRAPHY; HISTORY OF GENESEE RIVER
The route of this trip extends from the U of R River Campus southward, up the Genesee River Valley, about 50 miles to Letchworth State Park and return. The Genesee River will be seen in both its pre-glacial and post-glacial valleys, including the scenic gorge through Letchworth Park and its history reviewed (see pp. 4-8). Middle and Upper Devonian strata (see pp. 26-46) will be seen at four stops, with opportunity for fossil collecting in rocks of the Hamilton group at two of them. One stop will be a visit to the Mount Morris flood control dam.

2: DEVONIAN STRATIGRAPHY; HISTORY OF GENESEE RIVER

Drumlin to left
Drumlin to left. Route leaves river bank and crosses drumlin at 4.9 miles. A number of the drumlins in this area have wave-cut northern ends developed while partly submerged in glacial lakes (see p. 49).

Top of Drumlin

Two drumlins
Two prominent drumlins to right (SW), one wooded.

Meander bend of Genesee
Meander bend of Genesee River adjacent to road (right). Here route begins to follow pre-glacial valley of Genesee, now with broad flood plain developed on partial filling of glacier-transported debris. Just north of this point, pre-glacial course swung eastward along outcrop belt of soft Upper Silurian shales, and eventually turned northward again in line with present Irondequoit Valley (see pp.. 5-8 and map on p. 4). Except for Irondequoit Valley, the pre-glacial valley north of this point is entirely filled with debris and is without surface expression, the course has been fairly accurately traced through water well records ..

Onondaga limestone
Bridge across stream with outcrops of Onondaga limestone about 150 feet east of road. The Onondaga escarpment has no particular expression at this point because of local prominence of slopes into Genesee Valley ..

Conesus Creek
Bridge over Conesus Creek, outlet for Conesus LaKe

East side of Genesee Valley
Begin ascent of east side of Genesee Valley. Good views to west (right) across valley. This is pre-glacial section between Mt. Morris and Avon (see p. 7).

North branch of Jaycox Run
Small bridge across north branch of Jaycox Run (Wheeler Gully). Road bends slightly right. Menteth limestone exposed in low falls immediately left (E) of road, also as one-foot bed at top of cut in stream bend to right. Shales in stream bend are Deep Run member, Ludlowville formation.

Falls over Tichenor
Falls, 40 feet high, over one-foot bed of Tichenor limestone about 400 feet west (right) of road

STOP1. Jacox Run
Section exposed in stream bed 0.25 mile west of road is as follows:
Moscow formation
Menteth limestone member - impure limestone, makes low falls | 1'
Ludlowville formation |
Deep Run shale member - calcareous shale and thin argillaceous limestones | 11'
Tichenor limestone member - crinoidal limestone, fallmaker | 1'
Wanakah shale member - calcareous shale with thin limestones
and prominent 1-foot limestone bed about 10 feet from top
49'
Excellent fossil collecting in Deep Run shale and shales of Wanakah member. Crinoid columns conspicuous in Tichenor limestone; this is one of the "Encrinal" layers of early reports. See pp. 31-38 for stratigraphic details and faunal lists.

View of Retsof mine shaft
Currently operating shaft of Retsof mine of International Salt Company visible to west across valley. This is reportedly the largest salt mine in the world. A single 9-foot layer of rock salt (in the Camillus facies of the Salina) is being mined at a level 1000 feet below the surface 'at the shaft. The face now being worked is about 2.5 miles from the shaft. An area about 15 miles in circumference has been mined by the room and pillar system, leaving about 60% of the salt in pillars. Mining began in 1885 at a shaft 3 miles south of Retsof (see mileage 78.3). The shaft at Retsof was opened in 1920.

Good view to west.
N.Y. 63. Turn left. After turn, good overlook of valley to west.

Fall Brook to right.
Fall Brook to right (W). Lower end of valley will be Stop 4, this trip. Falls is over Genundewa limestone at base of West River formation (see p. 41).

Breech in west wall of Genesee Valley
Breech in west wall of Genesee Valley, visible in right (W) distance across valley and just to right of water tower and smokestack, is debouchure of post-glacial Genesee from Mt. Morris canyon (see p. 7).

Canaseraga Creek
Bridge over Canaseraga Creek, the misfit stream presently occupying wide Dansville Valley (see p. 5). Route here begins to cross wide flat floor of this valley, originally cut by pre-glacial Genesee, then deepened by ice-gouging and partly filled with rock debris and lake deposits.

Climb out of valley
Route climbs from valley floor, cross railroad. Enter Mt. Morris.

Overlook of Mt. Morris canyon to left.

STOP 2. Mount Morris Dam
Built by Corps of Engineers, completed 1951. Purpose: flood control. Concrete construction using filler of crushed Onondaga limestone from General Crushed Stone Company quarries at LeRoy (20 miles north) and sand from glacial lake delta just north of gorge (see mileage 73.8). Total length of dam: 1028 feet, length of spillway: 550 feet. Drainage area above dam: 1077 sq. miles, maximum reservoir areag 3300 acres. Capacity at spillway elevation: 337,000 acre feet. The base of the dam rests upon the Genundewa limestone at the base of the West River shale (see p. 41). The section exposed in the gorge is as follows:
Glacial cover |
Rhinestreet black shale -- laminated, finegrained shale, making buttresses at gorge rim | 53'
Cashaqua formation -- gray-green shales and thin siltstones, easily weathered and making the long slope of the gorge wall | 121'
West River shale -- dark, thin-bedded shale at foot of gorges> only part exposed | 65'
The Rhinestreet and Cashaqua and the contact between the two are excellently exposed in the cuts of the road leading down to the deck of the dam.

View of Dansville Valley
To the southeast (left front) can be seen the broad Dansville Valley extending into the distance and, to the right of it, in front of the high ground, the Nunda Valley which was cut by the pre-glacial west branch of the Genesee and is now occupied by misfit Keshequa Creek. See pages 4-70

Begin descent into Nunda Valley

Keshequa Creek
Keshequa Creek, misfit stream to left of route.

Locks of abandoned canal
Locks of abandoned canal constructed to carry river traffic from Portageville to Mt. Morris via the Nunda Valley, around post-glacial gorge section of present Genesee River. Canal operated 1852-1877. Lock walls are constructed of Nunda sandstone (see p. 45); typical gray-green flagstone blocks.

Ascend morainal dam
Begin to ascend morainal dam which blocked Genesee from pre-glacial Nunda Valley. Route crosses moraine from here to Portageville.

Descend slope of Portageville moraine
Descend slope of Portageville moraine into pre-glacial Genesee Valley. Good view of valley to left (S)

Genesee River
Bridge over Genesee River. River elevation 1100 feet

View of Genesee River
Railroad overpass. To north (R) Genesee River can be seen where it leaves broad pre~glacial valley and enters narrow post-glacial gorge section.
2010: Railroad is gone, but this should be where it used to be.

Upper Falls
Erie Railroad bridge across gorge. Uppermost of three falls in gorge just north of bridge (height 71 feet) fall-maker in basal Nunda sandstone (see p. 7). Roadcut exposures are Nunda.

STOP 3. Bench between Middle and Upper Falls
Parking area. LUNCH stop. This flat area is a small terrace bench between the middle and upper falls. The middle falls, highest of the three in Letchworth Park, drops 107 feet. Fall maker is resistant layer in Gardeau formation (see p. 45). The lower falls will not be visited.

Good view of middle falls as route ascends hill

Nunda Sandstone
Roadcut outcrops of Nunda sandstone. Bronze tablet to James Hall.
2010: The tablet, placed in 1908, is probably no longer here. A replica was on display at the museum for a time.

Gorge overlook.
Gorge overlook. Camera stop. Gorge wall is Gardeau formation

Wolf Creek

Road cut to right exposes glacial lake sands

North overlook of Mt. Morris Dam is to right

Small Delta
Excavations in small delta built into glacial lake filling Genesee Valley (elev. about 800 feet). Some of sand for dam concrete obtained here.

Re-enter wide pre-glacial valley
N.Y. 36. Turn left (N). Genesee River leaves gorge section and re-enters wide pre-glacial valley 0.25 mile south of this point. Road route now follows along west edge of valley to Leicester.

Type section of Moscow Fm.
In east bank of stream (Little Beards Creek) a quarter-mile north of here is type section of Moscow formation of Hamilton group

Abandoned mine buildings
Sharp right turn in Cuylerville. To left, after making turn, can be seen abandoned shaft head buildings of the International Salt Company mine. Only a small ventilator shaft operates here now; active shaft is about 3 miles to the north. Route now crosses flat floor of broad Genesee Valley.

Genesee River

STOP 4. Fall Brook
Park just past abandoned buildings on right.
This is the type section of the Geneseo black shale (village of Geneseo just to the north) and also affords excellent exposures of the overlying Genundewa and West River and the underlying Leicester marcasite and Windom shale members of the Moscow formation. See pages 35, 39.
The more calcareous layers of the Windom are richly fossiliferous; some large concretions occur. The Moscow-Geneseo contact is marked by the thin but unusual Leicester marcasite which has a Hamilton fauna described as dwarfed or interpreted to consist of small fossils as a result of sorting (Loomis, 1903; Tasch, 1953). Where the lenses of Leicester are absent, the contact is marked by iron staining. The conspicuous laminated bedding and smooth jointing of the Geneseo contrast with the less regular structures of the Windom. The Geneseo is almost unfossilliferous. Large blocks of the fall-making Genundewa limestone show its characteristic lithology; most blocks are replete with the pteropod (?) Styliolina fissurella.

Geneseo black shale
Geneseo black shale with limestone bands and layers of concretions in road cuts.

Trip back goes over same route
Junction N.Y. 63. Turn left. Route from here back to U of R campus follows course of start of this trip from 0.0 to 28.7 miles.

3A: HAMILTON STRATIGRAPHY AND FOSSIL COLLECTING
Exposures of the Ludlowville formation will be visited in an area south of Batavia. The Centerfield member here is prolifically fossiliferous and the relationships of the other Ludlowville members (except the Deep Run) are clearly shown across the Clarendon-Linden monocline

3A: HAMILTON STRATIGRAPHY AND FOSSIL COLLECTING

Ascend Dumpling Hill drumlin
Road swings away from Genesee River. Ascends Dumpling Hill, a drumlin whose northeast end is truncated by the Genesee

Now over Silurian
Turn right (W) on North Rd. at beginning of settlement (Scottsville). Now over Upper Silurian; no exposures

Gravel pits
Scottsville-Chili Rd. Keep straight. Several gravel pits in glacial material to left after crossing

Wooded Drumlin
Stop sign. N.Y. 383. Turn right (W). Wooded drumlin at left after making turn. Behind (S of) drumlin is shallow gypsum mine in Upper Silurian, Plant-visible at 15.3 miles

Oatka Creek bridge.
Creek here runs west-to-east along south edge of outcrop belt of soft Upper Silurian shales. Rise of ground just south of creek in Onondaga escarpment, here supported by waterlimes above Salina shales and by lower part of Onondaga limestone ..

Quarry in Onondaga Limestone to right
Quarry and crushing plant of General Crushed Stone Company to right. Operating in Onondaga limestone

Enter Village of LeRoy, birthplace of Jell-O!

Bridge over Oatka Creek.
Low dam retains pond to left. To right, just north of bridge, is low falls over Stafford limestone member of Marcellus formation, Hamilton group. Banks below buildings on east (right) side of creek below falls used to expose type section, Oatka Creek black shale member of Marcellus (typical Leiorhynchus facies: paper-like black shales with Leiorhynchus and Orbiculoidea. Bank is now parked and exposures are poor.

Levanna member, Skaneateles fm
Outcrops in stream bank to left (SE), adjacent to small bridge on side road, are Levanna shale member of Skaneateles formation.

STOP 1. East Bethany fossil site
Exposures of Hamilton strata along Delaware, Lackawanna and Western Railroad and vicinity, 3 miles west of East Bethany.
This locality is world famous as a collecting ground for Middle Devonian fossils of the typical Hamilton assemblage (see ppe 37-38). The locality is also interesting for structural features, unusual in western New York, which have led to the exposure of over 100 feet of strata in a relatively short, nearly horizontal exposure. The section to be visited extends along railroad cut and hillside exposures for about half a mile east of the bridge carrying Francis Road over the railroad tracks. In this distance the section spans, nearly completely, the Clarendon-Linden monocline, a westward-sloping flexure which displaces the exposed strata about 100 feet. Observable dips at the surface reach a maximum of about .5 degrees. Water and gas well records suggest a greater displacement at depth, and it may be that the monocline evidenced at the surface is but a subdued expression of a major fault at depth.
The stratigraphic section here is as follows (see pp. 30-34):
Ludlowville formation |
| Tichenor limestone | about 1'
| Wanakah shale | 1.5'
| Ledyard shale | 88'
| Centerfiled shale | 2' (+?)
Skaneateles formation |
| Levanna shale | portion near top
The accompanying map and perspective sketch indicate the field relations. The letters in the following discussion refer to these illustrations. The Levanna shale (A) is in typical black shale, Leiorhynchus facies, exposed in the stream bank. The Levanna-Centerfield contact is covered and the actual thickness of the Centerfield cannot be determined. Unweathered blocks occur in place, with horizontal bedding at B, and from here eastward for more than a mile. Most of the material in this cut is weathered Centerfield residuum rich in fossils. At C fresh Centerfield strata occur in the stream bed about 30 feet lower than at B, and in between the two (D) the ground surface is composed almost exclusively of fossils weathered from the Centerfield and washed clean of matrix. Samples of the finer fraction of material here are rich in microfossils: ostracods, sponge spicules, Foraminifera, Bryozoa, crinoid and echinoid plates and spines, immature specimens of larger forms (and oddly shaped cinders!). The larger specimens are mostly corals, brachiopods, gastropods, and crinoids in great variety, and the trilobite Phacops rana.
Severe weathering of a portion of the Ledyard bearing fossils formerly replaced with marcasite has yielded an interesting assemblage of limonitized specimens at E. Most connnon are small gastropods and nautiloids, the goniatite Tornoceras, and nuculoid pelecypods.
Middle layers of the Ledyard, exposed in the railroad cut F, are poorly fossiliferous. Leiorhynchus and Chonetes occur in some of the laminated black shales in this cut. A rather high angle reverse fault (displacement a few feet, dip east) is visible here.
The upper portion of the Ledyard, and the Wanakah, in cuts on both sides of the railroad at G, typify the calcareous shale facies of the Hamilton. Occurring here are Rhipidomella, Athyris, Atrypa, Mucrospirifer, Ambocoelia, Stereolasma, Pleurodictyum, Styliolina. Microfossils are abundant, also, in washed residues of thoroughly weathered material, but variety is less than in samples from the Centerfield. Some of the more coherent layers contain orthoconic nautiloids, gastropods and pelecypods, along with the trilobites Greenops and Phacops.
The resistant lime-rich layer which descends to track level just west of the bridge abutment is the "Strophalosia" bed, replete with the productid brachiopod Productella truncata (formerly Strophalosia). This has been used as the marker horizon separating the Ledyard below from the Wanakah above. This practice is of questionable validity (although followed here for convenience), for the bed does not occur in a consistent position with respect to the top and bottom of the Ledyard-Wanakah shale interval in different exposed sections (see p. 34). At this locality it is unusually high, thus making the thickness of the Wanakah unusually small and that of the Ledyard correspondingly great. It is probably better to consider the Ledyard-Wanakah a single unit with several contrasting facies between the Centerfield and Tichenor 1imestones.
An exposure near the top of the Wanakah, at H, is rich in Chonetes, Mucrospirifer and Pleurodictyum. A little higher on the slope in the same area, tetracorals probably weathered from the Tichenor can be found.

3B: SILURIAN-DEVONIAN CONTACT RELATIONS
Oaks Corners Quarry
The highest Silurian strata (Bertie and CobleskillJ see p. 18), the lowest Devonian strata (Onondaga, see pp. 21-26), and the disconformable contact between them will be examined at a locality near Phelps, N.Y.

3B: SILURIAN-DEVONIAN CONTACT RELATIONS

Pass under railroad. Erie Canal to left.

Sand and Gravel quarries
Gravel and sand operation in water-laid glacial material to right.

Kame-moraine area
High ground to left is western edge of large kame moraine area (Turk Baker Hills, see p. 55).

Gravel pit
Gravel pit in kame material to left

Victor Channel
For next few miles route runs along northern margin of Victor channel, cut by waters flowing parallel and close to the ice front. Onondaga limestone caps high ground to south of valley.

Drumlins and Onondaga escarpment
Next 5.8 miles: The route here runs about a mile south of the southern edge of the great Palmyra drumlin field. Some of the southernmost drumlins are visible to the left (N). The high ground to the right (S) is the Onondaga escarpment, rather feebly developed here.

Cross Canandaigua Lake outlet.

Stone fences
Stone fences are of platy waterlime of Bertie formation

Gravel pit to right (S)

Onondaga escarpment
Clifton Springs to right (S). Rise in ground is Onondaga escarpment

Onondaga outcrop belt
Slight rise in route elevation marks passage onto Onondaga outcrop belt. Note Onondaga blocks in stone fences

Bertie outcrops
Cross Flint Creek. Bertie outcrops in stream bed.

STOP 1. Oaks Corners Quarry
Oaks Corners Quarry and Plant of General Crushed Stone Company. The stratigraphic section exposed here is as follows (measurements from Oliver, 1954):
Onondaga limestone |
| Moorehouse member: medium- to thick-bedded limestone with dark chert | 36'
| Nedrow member: thin-bedded impure limestone with chert | 16'
| Edgecliff member: light gray crystalline coralline limestone, with pebbles of Cobleskill and intermittent sandy zone at base | 10' &plusmn;
Disconformity: Relief up to 5 feet along irregular surface. Contact has been locus of much solution and it is difficult to judge how much of the relief of the contact surface is due to pre-Onondaga erosion and how much to post-depositional solution. Lower Devonian Helderberg-Oriskany sequence missing
Cobleskill formation, Akron dolomite facies, unfossiliferous massive dark dolomite. Vugs near top contain secondary minerals, calcite, dolomite, sphalerite, and gypsum | 10-14'
Bertie formation (in pit in quarry floor) |
| Williamsville member: buff-weathering homogeneous waterlime with conchoidal fracture. A fine, even lamination determines breakage into thin plates. Upper surface makes quarry floor | 5'
| Scajaquada member: medium-bedded dark dolomitic limestone. Only upper portion exposed. | 15' &plusmn;

3C: MINERAL COLLECTING
Itinerary same as for Field Trip no. 1A (see p. 75) from U of R River Campus to Penfield Quarry of Dolomite Products Company (miles 0.0 to 10.3).
No road log

NYSGA 1957
New York State Geological Association
Twenty-Ninth Annual Meeting
Wellsville, N.Y. - May 9 - 12, 1957
Guidebook
for
Geology of S.W. Tier
Oil and Gas Fields
Oil Refining
Field Trips
Edited and Compiled
by
W. H. Young, Jr. and W. L. Kreidler

A: GEOLOGICAL OUTCROPS IN WELLSVILLE AREA
by W.L. Kreidler, N.Y.S. Geological Survey

A: GEOLOGICAL OUTCROPS IN WELLSVILLE AREA

Junction with Rte 19
Junction of Route 19, turn right (south). The Wellsville crops out at the base of the hills to the east which are capped by Germania or basal Cattaraugus.

STOP 1 Hinsdale Outcrop
9:07 A.M. Hinsdale outcrop in road cut along Fords Brook. This is a 20 minute stop. (Sta. 2 on Map 2)
Description:
Top - 7' | Hinsdale - interbedded gray micaceous siltstones 1" to 4" in thickness and gray shales; contain loose sponge spicules, Prismodictya sp. and Cyrtospirifer disjunctus.
Base - 5' | Wellsville - interbedded 1" to 4" dark purple siltstones and shales.

Outcrop to left, across creek

Oil Field
Oil wells in Fords Brook pool on left.

Tank Farm
Sinclair tank farm on left.
2010: Tank farm is gone...

Cross Genesee River
Cross Genesee River and turn left (north) at blinker light onto Route 19. (At northeast end of Genesee River bridge test hole encountered 125' of glacial deposits.)

Glacial and river terraces on right.

Terraces and Scio Oil Pool
Glacial and river terraces on left and Scio oil pool, on right, across railroad tracks. Top of producing sand is at a depth of 290'

Machias formation outcrops
Machias formation outcrops on right across Vandermark Creek.

STOP 2 Cuba and Machias outcrop.
10:00 A.M. This is a 45 minute stop. (Sta. 3 on Map 2).
Description:
Top - (the upper portion is accessible only with great difficulty and therefore the data for these upper units is taken directly from the Wellsville Bulletin)
Top - 20' | irregularly bedded buff sandstone
12' | fissile olive-gray argillaceous shale
13' | buff siltstone and sandstone containing numerous Tylothyris mesacostalis
2' | massive buff sandstone
5' | interbedded buff sandstone and siltstone
1.5' | massive buff sandstone (base of Cuba)
12' | interbedded gray shale and thin gray siltstone (top of Machias)
1' | fossiliferous gray siltstone
10' | mostly gray argillaceous shale with a few thin gray siltstones
1.5' | medium light gray siltstone containing coquinites of Cyrtospirifer disjunctus
6' | fissile medium gray shale with limonitic stain
2' | gray siltstone containing coquinites of Cyrtospirifer disjunctus
15' | mostly medium gray argillaceous shale showing limonitic stain, with a few interbedded 1" to 1' gray siltstone containing crinoid stems
road level - 20' | mostly medium gray shale with a few interbedded 1" to 2' gray siltstone
Base - 6' | interbedded medium gray shale and gray 1" to 2" siltstones (The lower two units are exposed in the creek bed below road level)

Madison Hill oil pool

STOP 3 Wellsville Outcrop in stream bed
11:02 Wellsville outcrop in stream bed about 100 yards north of street. This is a 45 minute stop (Sta. 1 on Map 2)
Description:
Top - 1' | medium light gray 2" to 4" siltstone
7' | olive gray shale with limonitic stain
12' | concealed
2' | medium light gray shaly siltstones and shales containing coquinites of crinoid stems; also present are Chonetes sp., Productella sp, and Cyrtospirifer disjunctus
2' | medium light gray 1" to 6" siltstone containing Cyrtospirifer disjunctus
4' | concealed
5' | interbedded olive gray shale and medium light gray thin to 2" siltstones; contain crinoid stems, Chonetes sp. and Cyrtospirifer disjunctus
3' | medium light gray 1" to 4" siltstones containing coquinites of crinoid stems and Cyrtospirifer disjunctus
15' | olive gray shale with a limonitic stain and only a very few interbedded thin gray siltstones
1' | gray fossiliferous coquinites of crinoid stems and Cyrtospirifer disjunctus
base - 5'
medium light gray thin to 3" siltstones containing flattened concretions ("storm rollers" ) up to 3' in diameter

Sinclair Refinery on left of road
2010: The refinery is no longer here, as it had a bad fire in 1958, the year after this field trip, and there was not enough oil left in the ground to justify rebuilding it. (It had also had a bad fire in 1936, but was then rebuilt.)

B: HARRISON VALLEY ORISKANY GAS STORAGE FIELD
by G. C. Borland, N.Y.St. Nat. Gas Corp

B: HARRISON VALLEY ORISKANY GAS STORAGE FIELD

Glacial terrace on left
Sand bank on left is in glacial terrace material.

On lake or stream terrace
On glacial lake or stream terrace on East side of Genesee valley. Stream cut in opposite side of river valley about 1 mile ahead and on right is old stream channel cut when glacial lake drained this way into the Allegheny River water shed. Present Mississippi River-Great Lakes watershed divide is about 1 mile up this valley West of Genesee River.

Sand and gravel quarry
Small gravel and sand quarry on right in glacial terrace material.

Out of main Genesee River Valley
Straight ahead and up hill out of main Genesee River Valley.

Gas pipe right-of-way
Cross cleared right-of-way of New York State Natural Gas Corporation's main transmission line from Sabinsville Field station to State Line Field Station. Right of way leads off to right at angle.

Drainage Divide
Left onto dirt. Hill top straight ahead is drainage divide between Great Lakes and Atlantic Coast water sheds. Elevation approximately 2200'.

Chemung Outcrops
Straight ahead. Chemung surface outcrop evidence. Catskill on scattered hill tops. Note slightly reddish color of stones in fence rubble and stone piles on these hill tops. These are predominately from sandy formations in the Catskill.( Cattaraugus).

Ida Scoville No. 1 Gas storage well
Gas storage well on right is the Ida Scoville #1 at northwest edge of Harrison Oriskany sand gas field. Oriskany is at 5201' depth.

Courtright storage well
Courtright storage well on left. Surface elevation 2225', top of Oriskany at 5129' in well.

Glacial material on left.
Glacial material on left. Terminal moraine of glaciers is about 10 miles south of this locale.

No. 2 Schofield storage well.

STOP 1 Harrison Compressor Station
New York State Natural Gas Corporation's Harrison Compressor Station, used solely for the storage of natural gas from Texas and the South in this previously depleted Oriskany sand gas field.
Plant Engineer's house and Schofield #3 storage well on left side of road. Park on right side of road next to fence. (see fig. 5).
ABSOLUTELY NO SMOKING INSIDE LIMITS OF FENCE.
11:30 A.M. The tour through the plant and "blowing off" the well will be completed about now. Those people leaving from this area can check their present location by looking at sketch in Chapt. VII, p.38.

C: SINCLAIR OIL REFINERY
Trip through the Sinclair Refining Company's Wellsville plant which processes Allegany crude oil.
No road log.
2010: The refinery is no longer here, as it had a bad fire in 1958, the year after this field trip, and there was not enough oil left in the ground to justify rebuilding it. (It had also had a bad fire in 1936, but was then rebuilt.)

D: OIL FIELDS AND WELL SHOOTING
by W. H. Young, Jr., Bradley Prod. Corp.

D: OIL FIELDS AND WELL SHOOTING

Descend from glacial terrace.
Incline is down off of old Genesee River glacial terrace.

Glacial lake terrace deposits.
Sand and gravel in left bank is at base of old glacial lake terrace deposits.

Pumping station in distance
Sinclair Refining Co. station in distance on right before crossing river pumps oil from Fords Brook field to Wellsville Refinery.

Shady Brook Glen of Fords Brook
Turn right and approach west edge of Genesee River flood plain, going through Shady Brook Glen of Fords Brook. 3" pipeline running along left side of road carries all oil from Fords Brook field to Sinclair refinery. Rocks in Glen are Hinsdale and Wellsville (see Stop 1, Trip A-1)

Oil wells
First few oil wells at extreme NE edge of Fords Brook field.

Gas pipelines
Cross cleared right of way (visible to left, up hill) of 14" and 20" diameter lines carrying gas from Pennsylvania and New York Oriskany gas fields to Rochester. Lines owned by New York State Natural Gas Corporation.

North edge of Fords Brook oil field.

STOP 1 Thornton Co. Warfield pressure plant.
1:50 P.M. STOP NO.1 Thornton Co. Warfield pressure plant. See water supply and injection wells, treating, mixing, filtering, pressuring and measuring of water and the filtering of oil wells for the water flood process of secondary recovery of oil.
ABSOLUTELY NO SMOKING OR OPEN FIRE PERMITTED while away from cars. (see fig. 6)

Injection well boxes
Boxes over water injection wells can be seen either side of road.

Injection wells
Turn left and proceed up very steep hill. On other side of hill road parallels a line of water injection wells (on right) with a different type of cover box.

STOP 2 Bradley Prod. Corp. Wesche property.
3:20 P.M. STOP NO. 2 Bradley Producing Corporation Wesche property. See pumping power, pumping and flowing oil wells, separator, stock tanks and gas saver used in oil recovery by water flooding.
ABSOLUTELY NO SMOKING OR OPEN FIRE PERMITTED in area of this stop. (see fig. 7)
4:30 P.M. Proceed on foot to see a well "shot" on the Bradley Producing Corporation Apco property about 1/4 mile east of STOP 2.

E: STRATIGRAPHY OF SOUTHWESTERN NEW YORK
by W. L. Kreidler, N.Y.S. Geol. Survey

E: STRATIGRAPHY OF SOUTHWESTERN NEW YORK

Leave Pleistocene deposits
Leave the thick Pleistocene deposits of the Genesee River Valley and continue on the Wellsville geological unit.

Station 9 Whitesville
Station 9. Slow down Whitesville (?) exposed in road cut, showing a storm roller zone, and a fine example of cyclic bedding.

Enter Allegany Oil field
On left (south), Sinclair Refining gathering tanks and pump station, entering the Allegany Oil field.

Allentown, N.Y
Allentown, N.Y., caution light near school. NOTE: Oil jacks in front yards and next to store.

Messer Oil Co. Lease
Messer Oil Co. Lease, with water treatment plant on right and power house on left.

Oil tank battery
Oil tank battery on right (north) side of Route #17.

Station 10 Whitesville fm
Slow down. Whitesville (?) exposed with fossils on road cut on right (north) side of road.

Whitesville fm.
Electric jack and Whitesville (?) on left (south) side of Route #17.

Pressure Plant on left

Siltstone outcrops
Siltstone outcropping alongside of road.

Western edge of Allegany Oil Field.

Water Plant on right

Glacial delta and river terraces
Cross over Dodge Creek bridge. Glacial delta and river terraces in the valley.

Dirty outwash material in glacial deposits
Entrance to Wolf Creek Scout Camp. NOTE: On left, stream or lake deposited dirty outwash material in the glacial deposits.

STOP 1 Wolf Creek flat pebbly conglomerates
9:26 A.M. (Station 11 on Map 2)
This is a 75 minute stop including loading and unloading.
Wolf Creek flat pebbly conglomerates in abandoned quarry on hill to right. The type locality of Wolf Creek conglomerate is at Sta. 12, 2.5 miles to the north and on left side of road. The Wolf Creek conglomerates are characterized by flat or discoidal quartz pebbles accompanied by occasional red jasper pebbles.
This quarry was opened about 10 years ago for rip rap to be used for levee dikess along the Allegheny River at Portville N.Y.
Top - 3' | olive gray micaceous siltstone
4' | massive sandstone with a little conglomerate, generally white with some limonitic stain; fossiliferous
3' | white 2" to 6" sandstone; fossiliferous
12' | massive sandstone and conglomerate containing "0rthoceras" sp., generally white with slight limonitic stain
Base -7' | massive white sandstone with a little conglomerate, showing slight limonitic stain
NOTE: From quarry you can see a glacial moraine dam and post glacial stream running from Scout Camp Lake through moraine on west side of valley.

Flood control dike
Flood control dike along Allegheny River on left (south) of Route #17.

Possible delta
To the right, pit in deltaic sands and silts. It might possibly be delta of Haskell Creek into Allegheny River valley during a glacial lake stage.

Olean Tile Company

Cemetery on glacial hill

Bradford Oil Field
Entering northern extension of Bradford Oil Field into New York State. NOTE: Boulders of Olean cgl along both sides of road.

Oswayo outcrop on left (east) side of road.

STOP 2 Cattaraugus red beds
11:24 A.M. STOP NO.2 Cattaraugus red beds with Oswayo above.
This is a 20 minute stop. (sta. 15 on Map 2)
Description: The Oswayo is composed of greenish-gray sandy shales with interbedded shaly, frequently fossiliferous, sandstone layers. The contact of the Cattaraugus and base of Oswayo is believed to be at the top of the highest red shale found in this section which is overlain by a fine-grained, greenish-gray, sandstone. Cattaraugus. A succession of red shales interbedded with greenish grey shales and fine-grained, greenish-gray, thin-bedded micaceous and argillaceous sandstones. It contains several well defined flat pebble conglomerate horizons. The Cattaraugus contains excellent cross-bedding and shows shaling out of the sandstones.

Row of crude oil stock tanks on left of dirt road.

STOP 3 Rock City Park
12:03 P.M. STOP NO.3 Rock City Park - type locality of Olean conglomerate.
NOTE: We will be here 2 hours, have lunch, examine outcrop and leave at 2:00 P.M. Mr. Melborne Cunningham, concessionaire at Rock City Park has made available to us picnic and parking areas. While here, the group will visit the type locality of the Olean conglomerate. (Sta. 16 on Map 2)
Description: The Olean conglomerate type locality is south of Olean, N. Y. at Rock City where it is 64' thick. There is an occasional layer of coarse quartz sandstone present in the conglomerate. Cross-bedding, joint cracks and large rounded or ellipsoidal pebbles are prominent features of the Olean conglomerate. The greater majority of the pebbles are vein quartz and milky in color but a few rose-colored ones are present. Pebbles 30 millimeters long are common, but most range from 10 to 20 millimeters in length.. There are a few pebbles of dark gray slate in the conglomerate. The Olean loses its conglomerate character as it is traced south into Pennsylvania. Fifteen to 20 miles south of the New York-Pennsylvania line it consists of a medium to coarse-grained quartz sandstone. The Olean conglomerate is found as far east as Alma Hill in Allegany County.
From hill is a good view of Olean and the former Socony-Vacuum Refining stock tank farm.

NYSGA 1958
Otto H. Muller
FIELD GUIDE BOOK
New York State Geological Association
30th Annual Meeting
HOST
Department of Geology
The City College
New York 31, N.Y.
Prepared
by
Authors of the Several Chapters
and
J. Kaikow, H. Muskatt, E. Votava
Edited and Compiled
Kurt E. Lowe

1: PALEOZOIC INLIER OF THE PEEKSKILL VALLEY
S. Schaffel
The City College
Trip 1-A, 1-B and 1-E

1: PALEOZOIC INLIER OF THE PEEKSKILL VALLEY

STOP 1. Poughquag quartzite
Walk right (N) on Highlands Ave. and right (E) on approach road to Bear Mt. Pkwy. (approx. 500 ft.). Outcrop of Poughquag quartzite (Cambro-Ordovician) in unconformable contact with Highlands gneiss (Pre-Cambrian). Dips of bedding and foliation are nearly vertical. This relation is considered typical of that between Paleozoic sediments and Pre-Cambrian crystallines along the south side of the Peekskill inlier.

STOP 2. Annsville phyllite
Southwest extension of Gallows Hill underlain by Annsville phyllite (Cambro-Ordovician Hudson River pelite group) and mantled by Pleistocene delta deposits. Interesting consolidation and solifluction structures have been collected at base of hill. Walk through US 9 roadcut following left (W) side of cut only. Take care to stay on the roadway. Observe prominent slaty cleavage (axial plane type), diagonal shear planes, flow folding of quartzite bands and later quartz veins.

STOP 3. Wappinger limestone
Wappinger limestone (Cambro-Ordovician) outcrops on north side of west abutment of bridge. Observe gradational contact with Annsville phyllite outcropping along steep west bank of creek. Specimens from this transition zone are identical with those from the Wappinger limestone outcrop at stop 4.

STOP 4. Critical Outcrops
Outcrops along left (W) side of road, Cambro-Ordovician sequence exposed from S to N (dipping east) Annsville phyllite (approx. 100 ft.) Wappinger limestone (10 - 15 ft. ) is dark gray, fine-granular transition facies (same as in contact zone at Stop 3) Poughquag quartzite, coarse granular (only a few inches exposed), In contact with granite pegmatite (Highlands crystallines). Is this an intrusive or unconformable contact? Pre-Cambrian Highlands gneisses outcrop intermittently from this point northward. Berkey (1919), on his geologic map of the West Point quadrangle (1) shows the northern border fault of the Peekskill inlier passing between the Annsville phyllite and the Poughquag quartzite at this point; (2) fails to indicate the presence of Wappinger limestone; (3) indicates an unconformable contact between Poughquag quartzite and the Highlands crystallines. This critical exposure does not yield clear evidence of faulting either within the sediments or between them and the crystallines. An orderly sequence of Cambro-Ordovician sediments appears to be present here lending support to the concept of the synclinal structure of the inlier (Plate 2). The much reduced thicknesses of the Poughquag and Wappinger support the interpretation of Bucher (1957) (Plate 2. Fig. B).

STOP 5. Annsville phyllite and Highlands gneiss
South side of roadcut shows Annsville phyllite and Highlands gneiss with intervening limestone flow breccia (relations are somewhat obscured by grading): Breccia appears to be tectonic and represents the continuation of highly deformed and metamorphosed marbles along Canopus Creek (to NE) called Grenville by Berkey (1919). Its stratigraphic position, however, makes its correlation with the Wappinger limestone a likely alternative. In that case, the Canopus Creek carbonate belt may be infolded and infaulted Cambro-Ordovician rather than Pre-Cambrian marble.

2: NEW YORK CITY SERIES
K. E. Lowe and S. Schaffel
The City College
Trip 2-B and 2-E

2: NEW YORK CITY SERIES

STOP 1. Fordham gneiss
Quarry behind transformer station at left (N), now used by N.Y. State for gravel and road machinery storage. Typical Fordham gneiss, the oldest formation of the New York City series.

STOP 2. New York City series
The 3 formations of the New York City series outcrop in close proximity, although actual contacts are not exposed.
Manhattan schist (garnetiferous muscovite schist) NW of the intersection along a side road;
Inwood marble (medium grained, crystalline marble, here containing accessory graphite) in road cut on both sides of Granite House Rd.
Fordham gneiss (banded biotite gneiss) a short distance SE along cut-and-cover portion of Catskill Aqueduct. Formations appear conformable with nearly vertical dips. These rocks were traced continuously from the New York City line to this locality by Fluhr (1940). The thickness of the Inwood marble here is much reduced compared with that prevailing in New York City (approx. 750 ft.), a feature which is rather common in Westchester County. It has been explained by "squeezing-out" of the highly plastic rock and by faulting.

Manhattan schist
Manhattan schist exposures for the next 3 miles.

View of Palisades
View of Palisades across the Hudson River (below crest of hill)

Palisades and Hudson Highlands
Next 0.4 miles: Good view of strongly dissected Palisades to west and Hudson Highlands escarpment to northwest

Delta and moraine
Cross Croton River; Croton Point delta and moraine at left (W)

Deltaic deposits
Croton Pt. Ave. (entrance to Croton Pt. Park) left (W); deltaic deposits at right (E).

Palisades and Hudson Highlands

Gravel pit
Remnants of a worked-out gravel and sand pit (part of Croton Point glacial delta)

Manhattan schist
Exposures of Manhattan schist along road

View of Hudson River Gorge
View of southeastern gateway of the Hudson River gorge straight ahead (N)

Cortlandt complex
Exposure of Cortlandt complex hornblende norite with spheroidal weathering having passed over contact between Cortlandt intrusive complex and the Manhattan schist a short distance back (not exposed)

Exposures of Cortlandt complex hornblende norite at right (N)

Exposure of Cortlandt complex pyroxenite at left (S)

Inwood / Manhattan contact
At left (SW) (in front of school) contact between Inwood marble and Manhattan schist

STOP 3. Verplanck Point Quarry
STOP No. 2-3: Verplanck Point Quarry (N. Y. Trap Rock Corp. )
Approach to quarry is down the flank of a large mound of tailings deeply carved by erosion into typical badland topography. Pass several large glacial erratics below (Highlands crystallines).
DO NOT walk too close to the edge of the quarry which has not been in operation for some years.
In east face of quarry (looking north) is well-exposed contact between Manhattan schist above and Inwood marble below showing interbedding. Dips are steeply to the east (into quarry face). The Inwood marble, except for its rather fine texture, appears to be typical. In the schist, biotite predominates over muscovite and the texture is fine-grained and more gneissic than schistose. The variation from the typical lithology of the Manhattan schist in New York City is attributed to the influence of the Cortlandt intrusive pluton.
Depending on the water level in the quarry (the water is approx. 150 ft. deep) evidence of isoclinal folding of the marble can be seen in the north face of the quarry.
Collapse of the top of the east quarry face recently exposed a discontinuous zone of coarse Inwood marble breccia in a greenish to reddish crystalline matrix, close to the contact with the Manhattan schist. Mr. S. Schaffel who first observed this curious rock believes that it is of tectonic origin and that the matrix was affected by gaseous or hydrothermal solutions from the Cortlandt intrusive. Angular fragments of marble appear to be quite fresh and unaltered. Detailed microscopic examination of this rock (unreported from any other Inwood marble locality) will be undertaken in the near future. This interpretation then assumes at least post-Taconic age for the Cortlandt intrusive (see discussion of age relations of the New York City series).
1.5 miles to the southwest across the Hudson River can be seen the Tomkins Cove quarry (N. Y. Trap Rock Corp. ) in Wappinger limestone (Cambro-Ordovician). As discussed under age relations of the New York City series in the preceding pages, several attempts have been made to correlate this series with the Cambro-Ordovician rocks of the Hudson valley. At this locality the Wappinger limestone and Annsville phyllite (Cambro-Ordovician) are in rather close proximity to the Inwood marble and Manhattan schist (uncertain age), with only the width of the Hudson River intervening. This feature makes the correlation of these two rock sequences a tempting possibility. Let us then review briefly the several alternative lines of reasoning:
(1) The Verplanck Point rocks could be the metamorphic equivalent of the Tomkins Cove sediments on the basis of similar composition, stratigraphy and structure. Paige (1956) suggested an anticlinal arch across the Hudson River along which the progressive kinetic metamorphism took place in an easterly direction. The same author also indicated that contact metamorphism associated with the Cortlandt intrusion could account, at least in part, for the metamorphosed nature of the rocks at Verplanck Point.
(2) The authors cannot agree with this interpretation. Contact metamorphism would require an unusually broad contact zone around the margins of the intrusive, a feature which does not seem to be present in other localities at similar distances from the intrusive contact. Also the characteristic contact emery deposits in the mica schist seem to be absent here.
Progressive metamorphism could offer a plausible explanation were it not for the remarkably short distance in which a typical phyllite is supposed to have changed to a biotite-muscovite schist. One way out of this dilemma would be the assumption of westward thrusting (under the Hudson River) to account for the present proximity of the two contrasting metamorphic terranes.
(3) Verplanck Point rocks of the New York City series could be older than the Cambro-Ordovician sediments at Tomkins Cove. In that case the two rock groups must be in unconformable contact with each other beneath the river.
It becomes evident that the clue to this problem of correlation is buried under the Hudson River whose bedrock profile and structure are not known in this locality.
Note a typical kame ridge (in cross-section) on top of the north quarry face.

STOP 4. Inwood / Manhattan contact
Contact between Inwood marble and Manhattan schist on right (S) side of road. Note bands of small cubic pyrite crystals in the marble (influence of the Cortlandt intrusive).

Manhattan schist exposures along road

Cortland complex
Start of massive, glaciated exposures of Cortlandt complex augite norite at right

Cortlandt complex exposures
Intermittent exposures of Cortlandt complex augite norite for the next 1.5 miles

Last exposures of Cortlandt complex rocks (augite norite)

3: THE CORTLANDT COMPLEX
A. Dolgoff
N.Y. City Department of Public Works
Trips 3-A, 3-B and 3E.

3: THE CORTLANDT COMPLEX

View SE gateway of Hudson Gorge
Pause: View of southeastern gateway of the Hudson gorge - on west side of River (from left to right): Dunderberg, West Mtn. and Bear Mtn. (with tower).

Hill at right with outcrops of Cortlandt complex augite norite

Norite outcrops along both sides of road

STOP 1. Olivine pyroxenite
Olivine pyroxenite near northwest margin of "Eastern Funnel" (E on Plates 4 to 8) and "Olivine Region" (Plate 6). Typical spheroidal weathering similar to that of olivine zone in the Palisades. Dickerson Hill (center of "funnel") to the southeast. Banding mapped by Balk (Plate 5) is difficult to distinguish in this exposure. Discussion of structural and petrologic features of the Cortlandt complex.

Pyroxenite
Next 0.4 miles: Outcrops of pyroxenite at right (E)
The outcrops are either on the left (E) or on the right (W).

STOP 2. Old quarry dumps
Old quarry dumps on both sides of road. Collect samples of Pyroxenite (with and without olivine) and augite norite. Note indistinct banding and quartz -pegmatite veins cutting pyroxenite and norite.

Cortlandt complex / Manhattan schist contact
Pause: Passing over contact of Cortlandt complex with Manhattan schist (country rock); schist outcrops on both sides of road.

Schist outcrops at right

STOP 3. Kingston Emery Quarry
Kingston Emery Quarry (operated by Colbate Emery Co. , Peekskill, N. Y. ) presently the only operating emery quarry in the Cortlandt complex. Note the following:
(1) In quarry, down near the working face, excellent rectangular jointing. Rocks are highly magnetic. South quarry wall shows crusts of quartz and calcite, and quartz veins in the pyroxenite.
{2} Walking up cut leading out of main excavation observe the pyroxenite grading into more banded augen schist which becomes a normal schist at the quarry entrance (Colabaugh Rd.). This zone of transition represents the Cortlandt complex - Manhattan Schist contact. The country rock shows evidence of having been mobilized by the Cortlandt pluton during intrusion. The contact effects are also well shown in the schist outcrops near the construction shacks. The quarry has only been in operation since 1942. The contact shown on Plates 4 to 8 is not quite accurate and should be shifted southwestward close to Colabaugh Pond Road.
(3) Emery ore (samples on dump at quarry entrance) is dark blue-gray with an occasional pinkish hue and massive. Quarrying operation has followed ore vein down-dip.

STOP 4. Hornblende norite
Hornblende norite with poikilitic hornblende near western margin of central "basin" (C of Plates 4 to 8). Platy structure of hornblende crystals can be observed.

Poughquag quartzite
Pause: Poughquag quartzite (Cambro-Ordovician) in unconformable contact with Highlands gneisses (Pre-Cambrian) at right (S). Dips are nearly vertical.

4: PLEISTOCENE GEOLOGY OF CROTON POINT
Cecil H. Kindle
Trips 4-B and 4E.

4: PLEISTOCENE GEOLOGY OF CROTON POINT

Former Croton River delta
If one had chanced to come along route NY-129, one would have observed the gravel and silt deposits of the former Croton River delta on the left (S) just before reaching US-9.

Former delta surface
Continuing along US-9 we rise up onto this former delta surface and find a traffic light ahead. Let us turn right (S) here on Croton Pt. Ave. and proceed to the Harmon railroad station (Fig. 1) Here we notice the wide cut made for the railroad and its shops.

Croton Point
We do not stop now, but continue, observing a former tidal swamp, now filled with rubbish, on our left. Soon the delta remnant is behind us and we travel on a tombolo (bathing beach on our right and former swamp on our left) to the outer portion of Croton Point. We proceed to the large parking field at its southern end.
Ahead of us we see a sand pit which furnishes the material used to cover the rubbish in the former swamp. Let us examine this exposure. Here we find another remnant of the old Croton delta with sand and fine gravel resting on varved silty clay. Occasional concretions may be seen in the latter. Some of the silty clay layers are disturbed with horizontal layers above them. Are they the result of slumping or disturbance by floating ice?
Let us now walk S along the shore. We see numerous bricks, castoffs from the days when bricks were manufactured here. Behind some swimming rafts parked above the reach of the tide we see a cattail (freshwater) swamp which marks the source of clay used in brick manufacture.
As we proceed beyond the swamp we see delta sands, and 100 yards or so further we observe these varved clays resting on glacial till containing boulders of various sizes in a reddish matrix. Now we realize the source of the boulders among which we have been threading our way along the beach. The surface of this moraine is uneven and appears to be dropping below sealevel for a distance before rising to 40 or 50 feet above sealevel at Teller's Point (Fig. 1). A boulder bar extending south of Teller's Point marks its further continuation.
As we return to our cars we realize the preservation of the outer remnant of the Croton delta from wave erosion must be credited to this moraine.
We can now drive to the north end of the parking area and examine the north tip of the outer part of Croton Point. The weather and the state of the tide will determine whether we walk along the outer side of the point (more boulders) or the inner side (shorter). Woodchuck holes indicate that the top of the southern end of this point is deltaic sand. At the north end are glacial till and Indian shell beds. Erosion appears to be rapid at all points along the shore. Waves have certainly cut down the size of the Indian campsite (at the point) considerably since the oyster beds were laid there. Was sealevel lower a short time ago? Does the (now buried) tidal swamp south of the tombolo indicate that sealevel was lower when that portion of the old delta was eroded?
Return to cars and drive back to headquarters following the same route as taken at the start of the trip. Compare route description of Trip 2-B between mileages 20.9. to 25.8 and 30.6 to 36.4.

C: THE GEOLOGY OF THE TRIASSIC LOWLAND OF SOUTHEASTERN NEW YORK AND NORTHERN NEW JERSEY.
George F. Adams
Trip C

C: THE GEOLOGY OF THE TRIASSIC LOWLAND OF SOUTHEASTERN NEW YORK AND NORTHERN NEW JERSEY.

Annsville phyllite
Roadcut through Gallows Hill; Annsville phyllite (Cambro-Ordovician) Hudson River pelite group; see Trip 1, Stop 1- 2).

Glacial deltas
Note remnants of glacial deltas along both valley walls

Climb Highlands escarpment
Road starts climbing Highlands escarpment (fault line scarp); continuous exposures of Highlands crystallines (Pre-Cambrian gneisses, schists and granites) from here to Bear Mt. Bridge.

STOP 1. Anthony's Nose
Anthony's Nose lookout point. The Hudson River has cut a gorge through the Pre-Cambrian crystallines below the Schooley peneplane level, here shown by the hilltops. The rock bench on which the Bear Mt. Inn is located is interpreted as a remnant of the Harrisburg peneplane level formed by the Hudson River when it meandered at this level. Since Harrisburg time uplift permitted the stream to cut to lower levels before the valley floor was drowned. Glacial modification of the valley is indicated by its fiord-like walls and the shortcut east of Iona Island. The crystallines form an upthrown block of the fault associated with the Triassic Lowland to the south. See description of Trip D, Stop 1.

Views from bridge
Excellent views crossing bridge:
Left (S): lona Island and southeastern gateway of Hudson gorge; prominent notch at Timp Pass (SW) where major thrust fault crosses Dunderberg-West Mtn. ridge crest
Ahead (W): North side of bridge: Mouth of Popolopen Creek (drowned); Hell Hole fault notch between Bear Mtn. (left) and The Torne (right); Crown Ridge extending northeastward from The Torne; all these owe their topographic prominence to the Storm King granite
Right (N): Southern portion of the Hudson gorge; Sugarloaf Hill on east shore (3 mi.) (Canada Hill granite phase); Livingstone Island (east shore, 1 mi.) and Cons Hook (west shore, 2 mi. ) are separated from the shore by abandoned channels of the Hudson; bedrock terraces, particularly prominent on west shore.

River channel
Iona Island and abandoned river channel at left (E); Doodletown Brook (subsequent stream on Timp Pass-Hudson River thrust fault) at right (W); fault crosses road at this point

White, graphitic marble (Greenville?) at right (W)

View of Hudson gorge and gateway to left (N)

Hudson River Reserve Fleet
Hudson River Reserve Fleet (ship "graveyard" of World War II) at left (E)
There were probably over 130 ships here at the time of the field trip. All were gone by 1972.

View of Verplanck Point quarry
Verplanck Point quarry (Pre-Cambrian or -early Paleozoic Inwoodmarble) across River at left (E).
2010: Also of possible interest, the nuclear reactors Indian Point #1 and #2 are just to the north of the quarry.

Tomkins Cove quarry
Tomkins Cove quarry (Cambro-Ordovician Wappinger limestone) at left (E)

Wappinger limestone outcrop at left (E)

Triassic redbeds
Cross bridge over Cedar Pond Creek; Triassic redbeds along both walls of gorge below

High Tor
Haverstraw railroad station at left (E), Palisades (High Tor) at right (W)

STOP 2. Haverstraw Quarry
level with crusher and loader at right (pick up Company guides)
Haverstraw Quarry of the N. Y. Trap Rock Corp.
Buses follow quarry road to left and take middle road (SE) at fork of roads; gentle uphill grade
Lower Quarry Level (appr. elevation 238 ft. ):
The quarry, extending in a NW - SE direction, is in the intrusive diabase forming the northern arc of the Palisades. Here the strike of the diabase body is oblique to the strike of the Trias sic sediments to the southwest indicating a cross-cutting relationship of the tabular igneous mass.
The prominent columnar structure of the diabase changes in attitude from nearly vertical (in the northeast quarry face) to easterly dips of 450 to 500 (in the northwe st and southeast quarry face s). This feature suggests a rather abrupt change in the attitude of the intrusion with re spect to the country rock from a gently dipping (150 SW) sill-like body to a steeply dipping (450 SW) dike. Prelimiary results of recent extensive diamond core drilling on the Company's property bear out this contention (Fig. 2). It is not yet known whether the sill-like portion (Upper guarry level and Little Tor) is a true sill or a low-angle dike transgressing across the equally gently dipping Triassic sediments. The true thickness of the diabase intrusion appears to be approx. 700 ft.
Farther south the upper contact of the steeply dipping diabase dike can be seen cross -cutting the Triassic sediments at the portal of the West Shore Railroad tunnel (mileage 22.7). No stop will be made at this locality.
Also observe occasional oblique shear planes with narrow zones of brecciation in the northeast quarry face. return (NW) to crusher level sharp right (SE) turn on road leading to upper quarry level; steep grade
Upper Quarry Level (appr. elevation 340 ft. ):
On a clear day, a fine view of the Triassic Lowland shows the low sandstone ridges striking toward the observer and oblique to the diabase dike. The ridge line at the back of the quarry extends southward for several miles showing the mature dissection characteristic of the Schooley peneplane remnants. In the far distance (S) the even summit area of the Palisades is characteristic of the early mature dissection of the Fall Zone peneplane remnants. Sparkill Gap near the boundary of the two surface s is hidden from view. The headwater s of the Hackensack River have been impounded to form the Lake DeFore st re servoir seen directly south. Turning toward the impressive northeast quarry face, osbserve extensive mass wasting aided by the near-vertical columnar structure and joint (.shear) planes dipping toward the quarry floor. A 50 ft. wide bench at approx. 430 ft. elevation, indicating the earlie st quarry level, has been almost buried under weathered debris. This represents one of the hazards of quarry operation, overcome in part by leaving ever wider benches on successively lower levels (thus reducing the rock volume that can be quarried).
Return (NW) to crusher level
2010: Quarry operations over more than fifty years have modified this stop considerably. This path will correspond to the road log after leaving the quarry.

Columnar jointing
Unusually well-developed, polygonal columnar structure at left (SE)

Upper contact of dike
Passing over West Shore Railroad tunnel; portal at right (S) below road shows steep upper contact of diabase dike cross-cutting the Triassic sediments.

Roadcut through Palisades diabase

Triassic Redbeds
Triassic redbeds (arkose of the Stockton formation) dipping gently NW (into cliff) at right (W) (behind bottling plant); top of outcrop approx. 150 ft. above sea level; Tappan Zee at left (E).

STOP 3. Sparkill Gap
Note: Take your belongings, because the party will not return to buses until after lunch (approx. 1.5 hrs.)
As the Gap is approached from the north along the Hudson River several outcrops of the Stockton formation (mileage 30.9) extend up the valley wall to about 150 ft. above sea level. The contact with the diabase is not visible at these localities, but must be above 150 ft. elevation.
Walk across bridge into Tallman Mt. Section of the Palisades Interstate Park. Follow shore road southward. Here the diabase is first seen extending to sea level. Although the contact is not exposed at this point, its position can be estimated from the location of the olivine zone about 30 ft. above sea level. Elsewhere this zone is known to lie about the same distance above visible contacts. It is interpreted as the result of magmatic differentiation by gravitative settling of early olivine crystals in the still fluid diabase magma. The olivine concentration in the zone is up to 25%.
Continuing along the shoreline past the swimming pool, an outcrop of arkose holds up a low terrace a few feet above sea level. A ledge at the back of the terrace is indurated arkose near the igneous contact, which is not exposed. The higher slopes expose fine -grained diabase and farther up the olivine zone.
Farther south, at a place not to be visited, the contact rises to over lOft. above sea level. It is evident, therefore, that there is a sag in the base of the sill at Sparkill Gap which may be associated with faulting. That a thickening of the diabase is not involved, is indicated by a distinct narrowing of the width of outcrop at the Gap. We now walk back up the automobile road to the level of the Gap floor (some 200 ft. above sea level). Here coarser diabase outcrops nearer the interior of the sill. We are close to the north side of the Gap which extends southward for about 2 miles before the slopes rise to the summit at 500 ft. elevation (see mileage 36.1 to 36.7). To the north, we look down on the water gap of the Sparkill. An offset of the diabase on the west side of the gap indicates that this creek follows a cross fault. It is the only stream cutting through the Palisades for its entire length from Haverstraw, N. Y. to Bayonne, N.J. On the other (N) side of the Sparkill the diabase slopes rise to rounded hills reaching heights of 700 ft. Care must be taken to distinguish between the actual water gap of the Sparkill and the interpreted earlier wind gap of broader dimensions and greater height (Plate 9, Fig. A).
Johnson (1931) interpreted the wind gap as a part of the former course of the Hudson River established as a superposed subsequent during the Schooley cycle. Later the river cut a water gap through the Palisades sill during the Harrisburg cycle. This water gap was abandoned when capture diverted the Hudson into its present course southward. At this time a reversal of drainage through the gap established the Sparkill as a tributary to the Hudson along the fault line mentioned above. (Plate 9, Fig. B).
Lunch in picnic grounds at north end of Tallman Mt. State Park return to buses via the same route

Fall Zone peneplane
Turn off road to right in front of large (burnt-out) road house Pause (if time permits): Discussion of Fall Zone peneplane level.

STOP 4. Flatrock Brook
The outcrop of diabase near the road is close to the upper contact of the Palisades sill. It is fine-grained and cut by thin acidic dikes. The hill-slope down toward the Brook approximates the dip-slope of the upper contact. The contact zone appears in the Brook as the diabase gives way to light-colored baked shales with low northwesterly dips. The actual line of contact is obscured by cover. Similar baked shales are found at the lower contact near Edgewater, N. J. but of much darker hue. The baked shales of the upper contact continue south along the strike of the sill. Their most impressive exposure is in Granton Quarry at North Bergen, N. J. where they underlie a subsidiary sill of diabase. Fossil fish (coelacanths) and a small crustacean (ostracod) have been collected from that locality. Both the lithology and fossil content of these beds strongly suggest the Locatong formation, although they occur many miles north of the main outcrop area of this formation.
Looking east from the road outcrop, one sees US-4 descending a valley which runs oblique to the upper contact in a northerly direction. The valley follows a fault line of the gravity type with downthrow on the east. The vertical displacement is approx. 100 ft. and appears to be related to adjustments connected with the emplacement of the magma.
Looking west, one sees the drowned valley of Overpeck Creek and beyond the low sandstone ridges of the Brunswick formation, approx.at the Harrisburg level. The skyline ridge is the First Watchung Mountain, a lava flow (fissure type) approximating the Schooley level. It should be possible to make out the Paterson wind gap which is similar in form and origin to the Sparkill Gap.

STOP 5. Brunswick Formation
Woodcliff Lake area - Brunswick Formation Construction of the Garden State Parkway below produced this new road and outcrop. These are rather typical sandy beds of the Brunswick formation. The shaley beds are usually found in the valleys. The brown sandstones here contain a few pebble beds which could be stream channel deposits. Conglomerate cobbles similar to those found near the border fault (Stop C-6) in alluvial fan deposits suggest a westerly source. This outcrop is about 8 miles from the border fault.

STOP 6. Triassic Border Fault
Park at right (on US-202): outcrop along road (uphill) at left (NW) The outcrop consists of badly sheared, Pre-Cambrian (granite) gneisses. Many slickensided surfaces are parallel to the surface of the border fault. The lineation (fault striae) approximates the direction of relative motion along the fault. While this is not considered to be the actual fault plane (dipping steeply southeast with downthrow of Triassic sediments to the south), it is probably within the fault zone. From a high point one sees the escarpment (Ramapo Mts. of the Hudson Highlands) extending beyond the Thruway toward the southwest. This escarpment is the product of differential erosion along the fault whose relative motion dropped the Triassic beds down on the southeast in contact with the Pre-Cambrian crystallines. The whole mass was deeply eroded by the time the Schooley peneplane was produced. The escarpment was developed later as a consequence of regional uplift. Looking southeastward toward the Triassic Lowland, a prominent hill just across the Thruway is an eroded plug-like intrusion of diabase (now being quarried for crushed rock).

Highway leaves fault line
US-202 swings away (S) from fault line proceeding on the rocks of the Triassic basin

STOP 7. Triassic Border Conglomerate
Y-intersection with Viola Rd. (Antrim Playhouse sign); park in triangular plot at right of US-202; outcrops on both sides of road These outcrops are about 1/4 mile east of fault line. Here the Mahwah River has etched a valley along the fault zone in Triassic beds. The outcrop at left (NW) side of road indicates former alluvial fan which was banked up against the original fault scarp. The presence of early Paleozoic cobbles, sometimes only slightly rounded, and the absence of the crystalline cobbles lead to several conclusions: (1) streams cutting into the upthrown block were relatively short, (2) the upthrown block was much higher than at present and contained a thick Paleozoic cover, (3) as the streams cut into this cover they nowhere reached the Pre-Cambrian basement, and (4) the upper surface of the fan must have been higher than the present Schooley level. What we see now are a few remnants of this fan showing typical torrential cross-bedding and rapid changes in grain size. Cobbles consist of Cambrian quartzite, Cambro-Ordovician limestones and Silurian-Devonian conglomerates. None of these rocks are now present on top or within the Pre-Cambrian crystallines of the Hudson Highlands directly to the northwest. Some have been preserved, however, as inliers to the west (along the New York-New Jersey border and in the New Jersey Highlands). They also outcrop abundantly in the Great Valley beyond the present Highlands to the north and northwest. On the east (SE) side of the road, pebble beds decrease and a more normal Brunswick aspect appears, similar to that seen at Stop C -5.

Fine-grained diabase
Lime Kiln Rd. at right (S); fine-grained diabase; intrusions of diabase outcropping intermittently along south (right) side of road for the next 1.5 miles are presumed to be one or more plug-like bodies or dikes; rare contact exposures show cross-cutting relationships.

Coarse border conglomerate at right (S)

Coarse border conglomerate on both sides of road

Diabase with columns
Next 0.2 miles: fine-grained diabase with columnar structure at right (S)

STOP 8. Mt. Ivy Glacial Delta
Park at entrance of sand and gravel pit at left (N) side of road This appears to be a fairly normal delta deposited in a periglacial lake, with typical top and foreset beds. No varved clays are exposed. The elevation of the delta top is 400 + ft., which indicates that it was a local lake feature not connected with the Hudson River 4 miles to the east.

View of Palisades
View of Palisades ahead to right (E); westerly end of hook-shaped Palisades ridge (dike) rising from beneath Triassic sediments (Plate 13)

STOP 9. Triassic Fanglomerate
This remarkable remnant of another alluvial fan consists almost entirely of semi-rounded Wappinger limestone (Cambro-Ordovician) pebbles poorly cemented by calcite and hematite. The source formation can be seen in place along a road to the north (mileage 86.5) and has wide exposure in the Tomkins Cove quarry 0.5 mile to the north. The occurrence of the Cortlandt complex and some gneisses of dubious age at Stony Point to the east suggest some complicated step-faulting in the region.

Wappinger Limestone
Roadcut through folded Wappinger limestone (Cambro-Ordovician); this belt of limestone widens northward where it is quarried at Tomkins Cove (0.5 mile)

D: PRE-CAMBRIAN AND PALEOZOIC GEOLOGY OF THE HUDSON HIGHLANDS
Kurt E. Lowe
Trip D

D: PRE-CAMBRIAN AND PALEOZOIC GEOLOGY OF THE HUDSON HIGHLANDS

STOP 1. Anthony's Nose
Anthony's Nose Lookout (See Plates 10 and 11, Fig. B)
Lithology: Canada Hill phase of Highlands Complex (Canada Hill granite of Berkey, 1919) - biotite oligoclase granite with epidote pods; gneissoid structure not pronounced; interpreted as granitized meta-sediments
Hudson Gorge: Southeastern gateway of Hudson gorge; superposition versus progressive headward stream erosion of the Hudson River; Iona Island and abandoned River channel; significance of bedrock terrace at Bear Mt. Inn
Faulting: Timp Pass - Hudson River thrust fault; channel fault (?) at Dunderberg ML ; Hell Hole tear fault (Popolopen Creek)
Regional Structure and Intrusive Plutons: Synclinal plutons of Storm King granite: Dunderberg and West Mts. (lower pluton) Bear Mt. - The Torne and Crown Ridge (upper pluton)

Views crossing bridge
Excellent views crossing bridge:
Left (S): Iona Island and Southeastern gateway - prominent notch at Timp Pass, where fault crosses West Mt. - Dunderberg ridge
Ahead (W): South of bridge: Bear Mt. terrace North of bridge: Mouth of Popolopen Creek (drowned); Hell Hole fault notch between Bear Mt. (left) and The Torne (right)
Right (N): Hudson gorge (southern portion); Sugarloaf Hill on E-shore (3 mi. NE) (Canada Hill granite phase); abandoned river channels at Livingston Island (1 mi. on E shore) and Cons Hook (2 mi. on W shore); bedrock terraces, particularly on W-side of river

STOP 2. Bear Mt. Inn Terrace
Walk N along W-edge of playing field: glaciated and striated outcrops of pegmatitic Canada Hill granite phase (S of roller skating rink); outcrop of sillimanite-garnet-biotite gneiss and schist (metasediments of Highlands Complex) at SE corner of rink
Hessian Lake: Shallow, glacially scoured contact line depression in Grenville (?) metasediments (including marble bands); intrusive contact with Storm King granite pluton along Sand W shores of lake; Canada ~lill granite phase along NE shore (Plate 12).
Ancient landslides of large Storm, King granite blocks (SW shore) from near vertical cliffs (obscured by trees) developed along major NE trending longitudinal joints in granite; prominent exfoliation of Storm King granite along W -shore; steep W -shore profile developed parallel to linear and platy structure of hornblende crystals in Storm King granite

STOP 3. Storm King Granite Contact
This stop on SW flank of Bear Mt, will be reached on foot (.6 mi. from entrance), because buses are not permitted on the Perkins Drive. It is regrettable that the planned visit to the top of Bear Mt. had to be eliminated for the same reason.
Keep to the left side of the Drive facing traffic and watch for cars on this winding 2-lane, 2-way road.
Layered sequence of Highlands Complex rocks: Biotite and hornblende gneisses and schists with intercalated bands of pseudo-alaskite (Canada Hill granite phase); interpreted as the result of selective granitization of metasediments (micro-pegmatite bands parallel to structure; replacement of quartz by plagioclase feldspars and perthite in thin-section); biotite in places makes rock indistinguishable from Canada Hill granite of Berkey.
Lower contact of Storm King granite pluton: (at nose of syncline) with metasediments; xenoliths near contact; dark- green, chloritized, quartz-rich contact phase of Storm King granite 500 ft. NW along road; prominent exfoliation of massive granite; typical "rubbly" weathering along linear hornblende structure; if time permits: visit to eclogite locality 100 feet below on abandoned road; metamorphic pyroxene (diallage) - garnet - graphite - quartz layer in Highlands Complex; source rock questionable.
2010: Path shown assumes users will not be in buses.

Banded metasediments
Prominently banded metasediments (biotitic and graphitic gneisses and schists) at left along Palisades Parkway.

Brooks Hollow marble
Passing between Lake TeAta. (left -S) and Lake Massawippa (right -N); construction of dam (at N end of Lake Massawippa) across the Brooks Hollow Creek temporarily uncovered a striking coarse-grained marble (contact-metamorphosed by intrusive Storm King granite) consisting of pink calcite, pale-green diopside and brownish phlogopite (named the Brooks Hollow marble).

STOP 4. Popolopen Natural Bridge
Walk 0.25 mile to SW end of Popolopen Lake
Natural Bridge across creek flowing into Popolopen Lake, developed through coarse, white, chondrodite-bearing marble; spinel dike on down-stream (lake-side) of bridge; curious dense, dark gray rock paralleling marble and creek on upstream side; thin-section study suggests a metamorphosed graywacke; both rock types along creek are completely different from known Pre-Cambrian metasediments in the Hudson Highlands; preliminary reconnaissance also indicates strong deformation of Highlands rocks along both sides of Popolopen Lake valley; rocks at this locality are, therefore, interpreted as infolded (and possibly infaulted) Paleozoic sediments(inlier).

Top of Escarpment
Top of NE-trending fault-line escarpment of crystalline Hudson Highlands; view of Central Valley (belt of early Paleozoic limestones)

Brecciated zones
Brecciated zones in Highlands gneisses at right (only evidence of steeply SE dipping border thrust at base of escarpment)

Last outcrop of Highlands crystallines (Pre-Cambrian)

View of Schunemunk Mt.
Passing over N. Y. Thruway; view (straight ahead) of Schunemunk Mt. (Devonian orthoquartzite and conglomerate).

STOP 5. Devonian Sediments
Cross railroad tracks to prominent outcrops along E-side of right of way. Devonian shaly sandstones (Oriskany-Esopus-Schoharie horizons)
Fossils:
Lower strata: poorly preserved sponges of type Titusvillia (?)
Leptocoelia flabellites, Leptaena rhomboidalis and other brachiopods
Middle strata: Spirophyton caudagalli (worm burrows or algal swish marks? ? )
Upper strata: Cypdcardinia (pelecypod)
Brachiopods (several genera)
Phacops and Dalmanites (trilobites) (confined to a single layer, hard to find)
Time will not permit to traverse across hill to E; in valley E of hill can be found (in descending stratigraphic order) Lower Devonian and Upper Silurian limestone (with corals), Silurian red shales (Longwood) followed by Lower Silurian conglomerate (Shawangunk) in Pine Hill beyond. Between Pine Hill and the Highlands escarpment to the E are beds of Wappinger limestone (Cambro-Ordovician). The exact structural relations between these stratigraphic sequences are not known with certainty. Westward across the valley of Woodbury Creek the shaly sandstones of the Highland Mills station appear to include the Hamilton group and are finally overlain by (Uppper ?) Devonian orthoquartzites and conglomerates of Schunemunk Mt. (a shallow syncline).
Approximately 1 mile to the north, along the E-side of the railroad, rocks of Oriskany lithology have been correlated with the Kanouse horizon (Onondaga) on good fossil evidence. (Eidman and Kindle. 1955)

Glacial delta deposits on both sides of narrow valley

STOP 6. Overthrust in Highlands Outlier
Walk S on Mountain road, crossing bridge to outcrop in hill at left (E) side of road (appr. 300 yds.)
Overthrust of Storm King granite (Pre-Cambrian) on intensely crumpled slaty shales of the Hudson River pelite group (Cambro-Ordovician).
Thrust plane dips rather gently toward the southeast. Small hill appears to be an outlier because Lower Paleozoic sediments have been found between it and the Highlands escarpment a short distance to the SE. Attitude of thrust plane here is atypical of Highlands border thrust which generally dips at high angles (70° in Delaware Aqueduct Tunnel E of Hudson River) to the SE.

STOP 7. Crow's Nest Lookout
View of middle Hudson gorge; West Point Military Academy on rock terrace below; Constitution Island with abandoned river channel; similar to Iona Island (Stop No. D-l), but on E-side of valley; Schooley Upland level E of the Hudson.

Large xenoliths
Large xenoliths of hornblende gneiss in pegmatite phase of Storm King granite at right (W)

Return
2010: Cross bridge and return by the same route taken to get here.

GEOLOGY OF THE CAYUGA LAKE BASIN
A Guide for the 31st Annual Field Meeting of the
New York State Geological Association
prepared by
Staff and students of the Department of Geology
Cornell University
"....We must especially collect and describe all the organic remains of our soil, if we ever want to speculate with the smallest degree of probability on the formation, respective age, and history of our earth."
Second (Revised) Edition
Ithaca, New York
May, 1959

A: ENFIELD GLEN (ROBERT H. TREMAN STATE PARK)
by Staff and Students
of
Cornell University

A: ENFIELD GLEN (ROBERT H. TREMAN STATE PARK)

Cross delta plain
Down the eastern wall of the Cayuga trough, and west across the delta-plain to Albany street, turning south.

Views of Coy Glen
Excellent views west from this stretch of road of the surface of the delta plain and the sequence of hanging deltas through which the Coy Glen stream has cut its gorge.

Railroad underpass
Just south of this underpass the end of the interglacial Buttermilk gorge may be seen on the east to be followed slightly to the south by the hanging valley waterfalls made by the post-glacial Buttermilk stream as it descends the oversteepened eastern wall of the Cayuga trough. The large gravel pit to the south of the Buttermilk falls was excavated in the hanging delta sequence made by Buttermilk creek.
The bed-rock exposed in Buttermilk Falls is the Ithaca formation. The upper member of the Ithaca shale begins at about the top of the first cascade.

Cross delta-plain
The road crosses the delta-plain to the west side of the valley and continues southward on glacial deposits

West wall of trough
From the floor of the Cayuga trough the road climbs the west wall. Small hanging deltas may be observed in several of which gravel pits have been opened.

Treman State Park
Upper or western entrance to Treman State Park. The parking area is in a post-glacial, excavated part of an interglacial gorge (see diagram for details). (The buses will leave the parties and later meet them at the lower or eastern entrance.) From the parking area, walk to the entrance of the post-glacial section of the gorge. This post-glacial gorge is nearly at right angles to the drift-filled interglacial gorge which swings around the rock island which forms the north wall of the post-glacial gorge. The outstanding feature of the post-glacial gorge itself is the perfection of joint-plane control of the stream course.

Lucifer Falls
Lucifer Falls at the eastern end of the upper gorge is slightly upstream from the main southern wall of the interglacial gorge which has been excavated by the post-glacial stream. The upper gorge is cut in the Enfield shale. The base of the Enfield formation is about at the top of Lucifer Falls. The lower sector of Enfield Glen is in the Ithaca formation.
Several sedimentary features are well developed in the rocks in the vicinity of Lucifer Falls, including current ripple marks that demonstrate that the general current direction was from northeast to southwest. Moreover, there is a submarine erosion channel which shows well in the south wall of the gorge above Lucifer Falls.
View eastward before descending into the interglacial part of the Enfield Glen the eastern, over steepened slope of the Cayuga trough.

Eastward from Lucifer Falls.
The trail follows down the drift-filled interglacial valley and thence along the excavated part of interglacial valley. Sulphur falls and the Lower falls represent spurs of the interglacial valley upon which the post-glacial stream was superimposed.

B: CAYUGA INLET TROUGH
by Staff and Students
of
Cornell University

B: CAYUGA INLET TROUGH

Downtown Ithaca
From Cornell campus descend into Cayuga trough to downtown Ithaca built on compound delta of four creeks. Valley fill more than 400 ft. thick. Bottomlands subject to flooding.

STOP 1. Buttermilk Falls.
Lower portion of Enfield and upper portion of Ithaca formation exposed. Representative of notched lower reaches of hanging valleys of Cayuga trough but contrasts with gorges initiated prior to last glaciation. Buttermilk Creek was diverted by glacial deposition in its interglacial gorge. Hanging deltas exposed in gravel pits 150 yards south.

STOP 2. Coy Glen hanging deltas.
Excavations by Rumsey Ithaca Corporation expose structure of massive deltas built into pro-glacial Lakes Warren and Dana during recession of the continental ice sheet in late Wisconsin time. Coy Creek in incising a meander initially developed across the main Dana delta has imposed on it second order meanders controlled by bedrock joints.

Kame and Kettle topography
Continue south on Route 13 over kame and kettle topography. Contrast steep southeast wall with gentler northwest wall of Cayuga trough.

Enfield Glen
Pass Enfield Glen and entrance to Robert H. Treman state Park

STOP 3. Shaffer Road overlook.
Meltwater from a pro-glacial lake briefly impounded near Newfield flowed through ice-walled channels, cutting the bench followed southeastward by Shaffer Road and debouching across kame terrace to the southeast. View across stagnant ice deposits which fill the southern end of Cayuga trough.

Kame complex
Descend into Cayuga trough over kame complex, via Piper St. to Stratton

Stagnant ice deposits
Turn right (south) on Route 34 at Stratton, riding across a complex of stagnant ice deposits which mark minor glacial oscillations during down-wasting of the Cayuga ice tongue in recession from the Valley Heads terminal moraine.

High point on road
Route 34 climbs to 1130 feet, about 750 feet above Cayuga Lake.
Tributaries to Cayuga trough have entry angles pointing north, whereas tributaries to the through valley south of this point have entry angles pointing south, suggesting that the present depositional divide between St. Lawrence and Susquehanna watersheds corresponds approximately with an interglacial or preglacial bedrock divide.

Enter outwash
Highway passes onto outwash where moraine ridge curves southeast.
Pitting and large kettle lakes (e.g. Spencer Lake) indicate outwash deposition onto unmelted stagnant ice. Valley Heads terminal moraine about 2.5 miles south of this point is largely buried in outwash.

Large kettle lake
Cross swampy edge of large kettle lake. Toward east side of Cayuga trough road curves north to parallel low, narrow ridge which separates it from south-flowing Michigan Creek.

STOP 4. Point. O'Rocks.
Ice and ice marginal deposits near the Valley Heads maximum crowded Michigan Creek against the side of its valley, forcing it to cut a bedrock channel around this point. During ice wastage Michigan Creek deposited a fan into which it is now cutting. Kame exposed in borrow pit.

Moraine
Moraine deposited by ice moving south down Michigan Hollow crosses valley.
Kames exposed in cuts and gravel pits to east near road. Valley bottom widens northward with swamp and ponds, the remnants of a small pro-glacial lake impounded behind the moraine until drained by Michigan creek.

Moraine ridge trending northeast across Danby Valley.

View of Portage escarpment
Road is here at 1500 feet above sea level on the glacially modified upland erosion surface. View northeast across Hungerford, Snyder and Turkey hills at the edge of the deeply dissected Portage escarpment.

Former ice-walled spillway
Descending the upper slope of Sixmile trough, cross rock bench at 33.6 miles.
This bench at 1030 ft. is continuous northwest to the abrupt nose on South Hill which marks a former ice-walled spillway.
Here the waters of pro-glacial West Danby Lake in Inlet trough first escaped eastward into Slaterville lake in Sixmile trough just before the two joined to form Lake Ithaca with outflow southeast past White Church and Willseyville.

C: AROUND CAYUGA LAKE
by Staff and Students
of

C: AROUND CAYUGA LAKE

Views of Cayuga trough
North towards Trumansburg (Views of Cayuga Lake trough to right. Note southerly dip of rocks on east shore of Lake; prominent datum plane is the Tully limestone).

Taughannock State Park.
East along upper Taughannock creek; exposures of middle part of Ithaca formation.

STOP 1. Main Falls Lookout.
Exposure of Geneseo, Sherburne, and Ithaca formations in gorge walls.

Delta and lower falls
Continue down hill to Rte. 89, south across Taughannock Creek and present delta, with view on right of lower falls over Tully limestone.

STOP 2. Hubbard Quarry.
Contact of Geneseo and Sherburne formations, Middle-Upper Devonian boundary. Fossils. Septarian concretions.

STOP 3. Fayette Town Quarry.
Upper Skaneateles (Levanna) shale in lower part of quarry; lower part of Centerfield member in upper part. Fossils from both members; septarian concretions.

STOP 4. Old Wolf Quarry (Warren Bros. Road Co.).
Upper Onondaga limestone (Seneca member). Tioga metabentonite.

STOP 5. Lunch Stop: Cayuga Lake State Park

STOP 6. Yawger's Woods.
Walk west from road 0.5 mile to woods, through woods to outcrop of Manlius (Olney) limestone and Oriskany sandstone.
Fossils from Oriskany (sledgehammers useful!).

STOP 7. Portland Point Quarry.
Upper Moscow (Windom) shale, Tully limestone, Lower Geneseo shale. Fossils. Alnoite dike. Low-angle thrust.

GUIDEBOOK FOR FIELD TRIPS
32th Annual Meeting
NEW YORK STATE GEOLOGICAL ASSOCIATION
prepared by
David Hawley and Donald B. Potter
HAMILTON COLLEGE
Clinton, New York

A: FRANKFORT GULPH SILURIAN SECTION
Purpose: The trip visits exposures of the Frankfort-Oneida disconformity, the overlying Clinton group, and the Vernon shale. These are the best exposures of the Clinton group in the type area.
Acknowledgments: The itinerary was suggested, and the localities described in Marshall Kay's "Geology of the Utica Quadrangle," 1953, New York State Museum Bulletin #347.
General: The unconformity at the base of the Oneida conglomerate is a reflection of the Taconian orogeny in New England. Most of the upper Ordovician and all of the lower Silurian are missing in this time gap. The overlying formations reflect a shoreline encroaching from west to east across New York State. The peculiar environment of deposition of the Clinton iron ores is discussed in section B of this guidebook. The Vernon shale, lowest member of the Salina group, represents the mud flats of a great delta built out from the east, which was intermittently encroached upon by hyper-saline seas from the west (Fisher, 1957). The extension of Seas eastward across the state during Silurian time accompanied the erosional reduction of the Taconian mountains in New England.

A: FRANKFORT GULPH SILURIAN SECTION

Bertie waterlime quarry
Abandoned quarry to right (S) of road, in Bertie waterlime. This is Crow Hill.

View of Mohawk Valley
Downhill into Sauquoit Valley. Mohawk Valley in distance to left (N).

Lake Herkimer delta foreset beds
Gravel pit on left (N) has coarse gravel foreset beds. It is a delta that was deposited in Lake Herkimer. Elevation of top is 1280'.

STOP 1. (the only stop on this trip) South Moyer Creek section.
Very sharp curve just beyond bridge over Moyer Creek. Park buses on right beyond curve and disembark.
KEEP WELL OVER TO OUTSIDE OF CURVE. EXAMINE THE FRANKFORT-ONEIDA CONTACT, AND MOVE ON SO OTHERS MAY DO SO.
This is one of the representative sections described by Kay (1953) as being the best, almost continuous exposure of the Silurian in the Utica quadrangle, and the following description is partly abstracted from his (p. 28-32).
At the bend of the road at the junction of Moyer and South Moyer Creeks, the road cut exposes the Sauquoit sandstone over the Oneida conglomerate, which in turn lies unconformably on the Frankfort shale (Moyer member). The Oneida is a massive quartz-pebble conglomerate which in the lower part contains many fragments of the underlying Frankfort. The basal 4-6 inches is impregnated with pyrite. The Oneida-Sauquoit contact is not accessible here, and is not sharply defined. It is inferred to be just below the strongly cross-bedded sandstone about 20 feet above the base of the Oneida.
About two hundred feet up the road, descend the bank on a trail, cross Moyer Creek, and proceed up the valley of South Moyer Creek.
Several hundred yards upstream the creek flows in a narrow channel cut in clayey till.
Upstream from the channel-cut till is the first Sauquoit sandstone, pebbly, dark greenish-gray heavy ledges. About fifty yards farther are the r1pple-marked, coarsely (3') cross-bedded ledges figured by Kay (1953, p. 34). Worm trails 1n the sandstone str1kingly resemble recent trails on bottom sand, often found here.
Farther upstream, 100' above the Sauquoit base, is a 20-foot zone of hematit1c sandstone with red and greenish-gray clay galls and prom1nent cross-bedd1ng (Grossman, in Kay, 1953, p. 68).
Still in the Sauquoit are beds of green shale interbedded with fine-grained sandstone. Interference r1pples show well on several beds. These beds are somewhat fossilliferous.
Farther upstream on a l2-l8-inch fine conglomerate bed are giant current ripples (WL about 30"), and above that a sandstone bed with prominent smaller current ripples. Current modified interference ripples appear on ledges about fifty yards farther upstream.
In the upper Sauquoit are heavy ledges of hematitic sandstone.
Above this the contact with the overlying Willowvale, and its basal oolitic hematite bed, is covered. The Willowvale is green, thin-bedded shale with some interbeds of fine-grained sandstone and siltstone, 30 feet thick.
The base of the overlying Herkimer is marked by a prom1nent 1-2 foot bed of strongly cross-bedded, sandy, oolitic hematite, which in other localities is as much as 3 feet thick (Kay, 1953, p. 35. fig. 25). The Herkimer is 80 feet thick, of interbedded rusty-weathering, pyritiferous, sandy dolomite and dolomitic sandstone, and gray shale. Several cascades are formed by resistant beds in the Herkimer.
The top of the Herkimer is distinct, though the contact with the overlying Ilion Shale (Fisher, 1960) is covered. Within a few feet of cover there is a change from the dolomitic sandstone of the Herkimer, below, to dark gray, fissile shale with 2-4 inch dolomite beds. The Ilion (Lockport?) is shown in fig. 24, p. 35 of Kay. It is 55 feet thick here.
The overlying Vernon has at its base 5 feet or more of green shale which is noticeable lowest in the stream channel. Above the basal green shale zone, which contains a few dolomite concretionary beds, is the typical red, crumbly, practically unbedded mudstone. The Vernon continues to the top of the exposed section in South Moyer Creek.
Board the waiting buses and return to the Hamilton Campus

B. CLINTON METALLIC PAINT COMPANY MINE
Clinton Metallic Paint Company Mine, Brimfield Street, Clinton, N.Y.
Proceed to mine by your own transportation. Small groups will be taken underground at regular intervals between 1:30 P.M. and 4:15 P.M.
Owner: Mr. Bruce M. Bare
Mine Foreman: Mr. Robert Barry
In charge of Mine Trip: Mr. Alvin J. Snyder
EVERYONE VISITING THIS MINE MUST SIGN A WAIVER AND GIVE IT TO MR. SNYDER BEFORE GOING UNDERGROUND. PLEASE SHOW DUE RESPECT FOR ALL PROPERTY AT THIS TIME.
This mine closed in 1963.

Clinton Metallic Paint Company Mine
The mining of oolitic hematite at Clinton, N.Y. dates back to 1797. Up until the first World War ore was used as a source of iron and the smelting was done locally at Franklin Springs and Kirkland. The Clinton Metallic Paint Company sank its Brimfield Street shaft in 1928. The mining is a modified longwall operation; the ore is hand sorted at the working face and again at the mine head. At the company's plant in Franklin Springs the ore is crushed to pass 325 mesh, bagged, and sold as a paint pigment, coloring agent for cements, and as a casting powder. There are two principal beds of oolitic hematite in the Clinton Group (see details below and general stratigraphic position in the Table of Silurian Formations, Trip A) The Westmoreland ore is the bed mined at Brimfield Street. Alling (1947) shows that the Westmoreland ore at Clinton, N.Y. consists of a lower one-foot layer of oolitic hematite separated by two feet of "siliceous" rock from an overlying two-foot layer of oolitic hematite. At the Brimfield Street mine this intervening "siliceous rock" or shale parting is generally absent so that the Westmoreland ore bed is about 30 to 36 inches thick and quite homogeneous. The Kirkland "red flux", a low grade dolomitic hematite bed, occurs 18 feet stratigraphically above the Westmoreland ore bed but the former cannot be seen in the encased shaft of the mine.
Sharp upper and lower bedding plane contacts are typical of the Westmoreland ore. Current ripple marks having a wave length of more than one foot are seen along the upper contact of the oolitic hamatite at several places in the mine. Oolitic hematite beds in the south branch of Moyer Creek (See Trip A) exhibit well developedcrossbedding. Dale (1953) notes the presence of ripple marks and channel fillings in the overlying fossiliferous Willowvaleformation, and both he and Alling conclude that the oolitic hematite beds are integral members of a shallow water marine depositional sequence.
Tbe oolitic hematite consists principally of small ellipsoidal concretions or oolites from one to four millimeters in maximum dimension. Each oolite (Alling, 1947) consists of "onion Skin" layers of fine grained hematite and chamosite (iron-rich chlorite) surrounding a nucleus of well-rounded quartz, calcite, or hematite. The oolitic ore is dominantly a dull (Tuscan) red with some irregular thin lenses and seams of bright red microcrystalline earthy hematite. Interstitial to the oolites is silica (largely quartz, minor chert), dolomite, calcite, glauconite, pyrite, and francolite apatite). Newland and Hartnagel (1908, p. 62) give the following average chemical analysis for oolitic hematite from the mines at Clinton, N.Y.
SiO2 | 12.63
Al2O3 | 5.45
Fe2O3 | 63.00
MnO | 0.15
CaO | 6.20
MgO | 2.77
S | 0.23
P2O5 | 1.50
CO2 | 6.15
H2O | 2.77
Crinoid columnals and tests or brachiopods, cephalopods, bryozoa, and gastropods, all replaced by hematite, are quite common in the ore. Alling (1947) proposes a diagenetic replacement origin for the ore and summarizes the evidence as follows: 1) they (the ores) are of the bedded type in the strictest sense; 2) they are thin, long lenses, which pinch out and come in again; 3) they are very extensive (oolitic hematite beds of this age occur as far west as Wisconsin and as far south as Alabama); 4) they are associated with sediments of shallow-water origin; 5) they are integral members of a stratified series; 6) they are not the result of replacement long after the deposition and lithification of the rocks, otherwise the ores would be "pockety", and the iron would stain the adjacent rocks; 7) many stages of replacement including replacement of fossil fragments by hematite can be seen in thin section; 8) groundwater played no essential part in the formation of the ore. Alling believes that solutions carrying iron, silica, and alumina were introduced into moderately turbulent, yet clear shallow seas and there precipitated by reaction with carbonates, the marine salts, and possibly by bacteria and oxidation. The oolites may represent precipitation of hematite and chamosite (iron-rich chlorite) from a colloidal state during a period of some agitation of the water.

C: PRECAMBRIAN GEOLOGY OF THE ADIRONDACK MOUNTAINS
Purpose: To visit the Remsen, Ohio and Piseco Lake Quadrangles and see several of the Adirondack Mountain lithologies, the Piseco Dome, and smaller structures.
Acknowledgments: The information presented here is based largely on the work of Miller (1909) in the Remsen Quadrangle, Nelson (recently completed field work) in the Ohio Quadrangle, and Cannon (1937) in the Piseco Lake Quadrangle
General: The Remsen, Ohio, and Piseco Lake Quadrangles lie in the southern part of the Adirondack Mountain Highlands Core, and in these quadrangles can be found most of the major lithologies of the Core.

C: PRECAMBRIAN GEOLOGY OF THE ADIRONDACK MOUNTAINS

Terraces
Proceed up slope over several terraces (500-780 feet) of glacial Lake Amsterdam.

Lake Amsterdam terrace
Broad terrace of Lake Amsterdam at foot of Marcy Hill. Bedrock beneath terrace is Utica shale. Marcy Hill, immediately to north, is capped with Frankfort Formation (Ordovician).

Top of Marcy Hill
Adirondack Mountains visible in the distance on a clear day. As we proceed north from Marcy Hill we are traveling down section in the Ordovician formations: Frankfort Formation at the crest of the hill, Utica shale on the north slope, and Trenton limestone group in the broad valley north of the hill.

Lake Herkimer delta
Route cuts through delta (el. 1000 feet) which is part of a large delta plain built into glacial Lake Herkimer.

Morainal belt

Lake Forestport delta
Deltaic deposit of Lake Forestport Elevation 1200feet.

STOP 1. Sillimanite gneiss
Sillimanite gneiss, mapped by Miller (1909) as "syenite-Grenville complex." The dominant rock here is a medium grained gray sillimanite-biotite-quartz-feldspar gneiss. The foliation planes on weathered surface are accentuated by flattened white matts of fine grained fibrous sillimanite (fibrolite), quartz, feldspar, and magnetite. This rock does not resemble any of the syenite gneisses. It is probably a metasediment of the Grenville sequence. Does the presence of sillimanite distributed through this gneiss indicate that the parent rock was sedimentary? Magnetite seems to be more abundant in this rock than in other lithologies of the region. Why is it associated with sillimanite?

STOP 2. Grenville sequence
On southeast side of river, downstream from the bridge, the following steeply dipping interlayers of the Grenville sequence can be seen: medium grained garnetiferous quartzite medium grained rusty weathering diopside-quartz marble graphitic calcareous tremolite-diopside quartzite biotite gneiss silicified metasediments: well defined nearly vertical bedding preserved in a solid mass of quartz which exhibits nearly horizontal jointing. About two hundred yards above the bridge on the southeast side of the river is exposed a sillimanite-biotite-quartz feldspar gneiss.

Trenton group
Cincinnati Creek. Exposures of Trenton group.

Prospect.
Proceed to 4-way intersection northwest of small village triangle. Cross intersection and follow Rt. 287 and signs to Hinckley. The West Canada Creek makes a sharp bend at Prospect, reflecting a postglacial diversion. The West Canada Creek rises in the West Canada Lake region of the Adirondacks and flows southwesterly to Prospect; at Prospect the river turns abruptly southeast and flows through the Trenton Gorge and southeast to the Mohawk River. Presumably the pre-glacial West Canada Creek had a continuous southwesterly course from source to the Mohawk River near Rome; an ice or drift dam deflected the West Canada Creek at Prospect in late glacial time and caused the river to flow southeasterly from this point and cut the Trenton Gorge. At Prospect Falls, just east of the village,there are excellent exposures of fossiliferous Coburg Formation (Trenton group).

Dam across West Canada Creek.
Hinckley Reservoir (Utica water supply) begins here and extends 5 miles upstream.

STOP 3. Coarse grained gneiss
Low hill with outcrops on north side of road. Dirt road from Wheelertown enters main route (287) from north about 100 yards east of outcrop. Coarse grained hornblende-quartz-microperthite gneiss; dominantly pink, some greenish. Note contorted and wavy foliation planes. Mapped by Miller (1909) as "syenite". This rock is more massive than the bulk of the granite and syenite gneisses in the region. This lithology is interesting because it points up the problem of rock nomenclature in the Adirondacks. On the basis of mineralogy, is this a syenite gneiss?

STOP 4. Small quarry
Note that Figure C-2 indicates that this rock is part of the great wedge of granite that tapers westward from the Piseco Dome. Nelson has recently mapped this rock as a mixed Grenville and granite gneiss unit, and notes the migmatitic nature of this exposure. The rock is a medium grained biotite gneiss with augen of pink feldspar and seams of aplitic and pegmatitic material parallel to the foliation. The foliation strikes between north-south and N 60 E, and dips to the west or northwest.

STOP 5. Part of Grenville sequence
Nelson maps this as part of Grenville sequence. The rocks here are coarse grained and gneissic. The dominant lithology is a coarse hornblende-garnet-quartz-plagioclase gneiss. Many large gray crystals of labradorite occur in this gneiss. In places these large crystals and smaller plagioclase crystals in the matrix of the rock exhibit a blue play of colors. The composition of one of the larger crystals was determined to be An52, and it was seen under the microscope to be crowded with small inclusions. (See "Problem" 5 under "Summary of Precambrian of the Adirondack Mountains.")
Interlayered with this hornblende-labradorite gneiss are dark bands of amphibolite and thin bands of biotite gneiss.

STOP 6. Quartz syenite gneiss
Broad outcrops along west side of West Canada Creek. Nelson maps this as equigranular quartz syenite gneiss and notes the presence of streaks of granite and amphibolite. Also present are coarse grained hornblende-feldspar pegmatite bodies. Note sheet structure which dips toward the stream on both banks, thus forming a natural gutter for the stream course. Pot holes on gently sloping rock surface on east bank.

STOP 7. Phacoidal quartz syenite gneiss.
PLEASE BE CAREFUL NOT TO DAMAGE THE CHRISTMAS TREES.
Exposure of dark greenish gray phacoidal quartz syenite gneiss. Texture is best seen on weathered surfaces. Cannon (p. 26) reports calcic andesine "xenocrysts" in syenite at "quarry just east of Morehouseville." This quarry is presumably south of the road. North of the road the gneiss is finer grained, phacoidal texture is not as obvious, and there are a few small pegmatite dikes. Note (Figure C-2) that this stop is about midway on the large east-west trending belt of quartz syenite gneiss that extends across the middle of the Piseco Lake and Ohio Quadrangles. Cannon considers this to be a thick, isoclinally folded porphyritic quartz syenite sill dipping steeply south.

South flank of Piseco Dome
Turn left (east) on Rt. 8. For the next 8 miles Rt. 8 runs along the east-west belt of "porphyritic" quartz syenite gneiss. Prominent row of mountains immediately north and parallel to the road is underlain by equigranular quartz syenite on the south flank of the Piseco Dome.

STOP 8. Lineated granite gneiss
Strongly lineated granite gneiss with sheets of metagabbro. Note that this stop is in the granite gneiss on the western nose of the Piseco Dome. The gneiss in the vicinity of the dome is strikingly lineated; the development of this lineation bears no obvious spatial relation to the faults. Note the elongated and flattened pencils of quartz and feldspar and the difficulty in identifying the "dark minerals" in this rock.
The metagabbro presents a special problem. Cannon (p. 17) notes that these tabular bodies are generally dark gray and fine grained; principal minerals are labradorite (An57), hypersthene, and augite. He postulates that the gaboro intruded the Grenville sequence, and then the granite intruded both; the granite intrusion completely "disintegrated" the Grenville so that the gabbro sills are the only remnants of the older Grenville-gabbro sequence. Smith (1894), however, interprets the gabbro bodies as sills intrusive into the granite. Note: the general conformity between foliation in the granite gneiss and metagabbro contacts; the conformity as to direction and magnitude of plunge of lineation in the gneiss and in the metagabbro; the apparent chill borders of the metagabbro (Cannon says the crystals in the centers of the metagabbro sheets are not coarser grained than those near the borders; the crystals in the center are merely clumped together giving the appearance of larger grain size); locally metagabbro sheets transect the foliation in the granite gneiss; at a few places thin dikes of granitic material cut the metagabbro. Who is right, Cannon,or Smyth?

STOP 9. Piseco Dome cross section
Southeast shoulder of Irondequoit Mountain. Begin STOP 9 which is a series of designated places chosen to exhibit a cross section at right angles to the axis of the Piseco Dome.

Point Comfort State Campsite.
LUNCH HERE IF A GOOD DAY. Lunch served by Methodist Church, Speculator. Bedrock exposed along west side of road is blocky, jointed greenish quartz syenite gneiss; same sill referred to in STOP 9A.

Cross contact
Cross contact between quartz syenite gneiss and granite gneiss.

STOP 9B. Lineated granite gneiss
Outcrop 200 feet west of road. Low ledges and blocky talus of strongly lineated granite gneiss. The axis of the Piseco Dome is in the vicinity of this stop and mileage note 86.5.

Strongly lineated granite gneiss
Strongly lineated granite gneiss plunging gently east-southeast along west side of road; houses close to road on east side.

Cross contact
Cross contact between granite gneiss and quartz syenite gneiss.

STOP 9C. Hornblende-quartz syenite gneiss
Entrance to Little Sand Point State Campsite. About 200 feet north of campsite entrance and 200 feet west of the road is STOP 9C Outcrops of equigranular hornblende-quartz syenite gneiss on the north limb of the Piseco Dome. Note development of hornblende, as contrasted to the mafics in the granite gneiss, and the fact that lineation is not as conspicuous in this gneiss as in the granite. This is the same "sill" as noted at STOP 9A. Note north-dipping foliation.

Contact
Contact between quartz syenite gneiss and granite gneiss along west side of road.

Gentle north dip
Note gentle north dip of strongly lineated pink granite gneiss.

STOP 9D Pink biotite granite gneiss
Outcrops west of road in woods. Lineated pink biotite granite gneiss. Foliation planes dip gently to north.

Contact
Approximate contact between granite gneiss and quartz syenite gneiss on the north limb of the Piseco Dome.

Granite gneiss on left.

Lunch stop.
LUNCH STOP IF RAINY DAY. Piseco Fish and Game Association, Inc. Lunch served by the Methodist Church, Speculator. After lunch trip will continue clockwise around Piseco Lake.

STOP 10. Road cut and broad flat outcrop.
Strongly lineated granite gneiss with some dark bands of amphibolite. Note (Figure C-2) that this granite gneiss corresponds in stratigraphic position to the granite gneiss at STOP 8. The equigranular quartz syenite sills which we saw at STOPS 9A and 9C presumably lie beneath the granite at this stop. Continue southwest from STOP 10; outcrops include quartz syenite gneiss and dark greenish gray biotite granite.

STOP 11. View looking west:
Look west across Piseco Lake along axis of Piseco Dome. Note asymmetry of higher mountains which are underlain by equigranular quartz syenite gneiss. Granite gneiss in core of dome is less resistant and forms lower ground. Note (Figure C-2) that Cannon postulates a normal fault (east side down) along the west edge of Piseco Lake.

Outcrops
Return to main highway and follow Rt. 8 to the southwest. Outcrops of granite gneiss and "porphyritic" quartz syenite gneiss along road between here and next mileage notation.

"Porphyritic" quartz syenite gneiss.

STOP 12. Outcrops on north side of Black Creek
Park near intersection and visit outcrops on Black Creek above bridge about 200 yards upstream from Road 4 (road from Gray north to Wilmurt Corners). NO SMOKING ON THIS PROPERTY, PLEASE. The principal lithology here is garnet-quartz-feldspar-biotite gneiss. Feldspar-rich layers, garnet-rich, and garnet-poor layers, and thin layers of amphibolite give the gneiss a marked banded appearance. Coarse white feldspar augen are present in many of the bands. The gneissic banding strikes about N60E and dips steeply southeast. Note (Figure C-2) that this garnet gneiss is one of the principal Grenville lithologies in the southern half of the Ohio and Piseco Lake Quadrangles. Tight isoclinal folds plunging 20 degrees northeast and involving garnet gneiss and fine grained biotite gneiss are well exposed at one place. At a small peninsula of rock there occurs a coarse augen gneiss containing three or four angular blocks of rusty weathering calcareous amphibolite. Note that the foliation in these amphibolite blocks is discordant to the foliation in the surrounding gneiss; note the angularity of the blocks and the fact that borders of these blocks contain less amphibole than the block as a whole; note tight folding of the gneiss in the vicinity of these blocks. What is the origin of this lithology and structure?

Glacial outwash deposit
Approaching glacial outwash deposit of unknown origin. Its steep,irregular north and east sides rise about 120 feet above the surrounding land to a flat top that has an elevation of 1400 feet. It is perhaps a delta built in contact with wasting ice.

Utica shale and Frankfort formation
Bedrock throughout most of the route from here south to Utica is the Utica shale; the Frankfort formation caps the hills.

D: LITTLE FALLS AREA TO TRENTON GORGE
Purpose: The trip was arranged to permit observation of salient structures and the stratigraphy of formations in this area from the Frecambrian through most of the Trenton group. In the sections observed there is evidence for the existence of an Adirondack arch, extending southwest through the Little Falls area.
Acknowledgements: Both the itinerary and the information in the field guide are heavily dependent on the work of Marshall Kay, particularly where the Trenton group is involved. For the Little Falls quadrangle the older work of H. P. Cushing has been used, and James R. Dunn, who has recently remapped the area, helped with the selection and explanation of localities in the field, and provided the summary of its geology for the guidebook. Donald W. Fisher helped with advice in the field, particularly regarding the extent to which Canadian formations are found in this area, and criteria for their identification.
General: The structural behavior of an arch extending southwestward from the south central Adirondacks through the Little Falls - Canajoharie area affected the types of sediment deposited, and whether or not any was deposited (or at least preserved) during the first half of the Ordovician period. Canadian formations, subject to intermittent warping during their deposition in the eastern Mohawk Valley, extend only as far west as Little Falls (Fisher, 1954). Of the Black River group, 230 feet thick in the Black River Valley, only the Lowville limestone reaches this area, and it is absent from Canajoharie eastward to the Amsterdam area (Young, 1943, and Fisher, 1954). Of the Trenton group, the lower formations (Rockland and Kirkfield) thin southeastward toward the arch, and are missing at Canajoharie where the Shoreham rests directly on Canadian strata (Kay, 1953).
The Shoreham is the youngest Ordovician formation to extend as a limestone around the south flank of the Adirondacks. The overlying Denmark, mostly limestone at Trenton Falls, changes eastward through the Dolgeville facies in the Little Falls quadrangle, to the much thicker Canajoharie shale of the eastern Mohawk Valley. The Cobourg similarly undergoes a facies change eastward, thickening and becoming the lower member of the Utica shale, if this may be called Utica (Kay, 1953, p. 46). The influx of argillaceous sediment from the east accumulated in greater thickness east of the arch, suggesting more rapid subsidence there than on the arch and westward from it, and the arch acted as a facies barrier during Denmark time. The muds spread westward across the arch during Cobourg time, though at Trenton limestone is found. Above the Cobourg, the Utica and younger shales indicate that the entire region was depressed and tilted southeastward, the direction in which the shales thicken. Details of this history are discussed in Kay (1953), pp. 74-76).

D: LITTLE FALLS AREA TO TRENTON GORGE

Hills to right and left
Hills across the valley to the right (S) are the escarpment of the Clinton group, and are the northern edge of the Appalachian plateaus. Hills to the left (N) are underlain by Utica shale, and capped by the Frankfort shale.

Large road cuts in black, fissile Utica shale at left.

View of terminal moraine
Knobby hills across the valley to the right (S) are terminal moraine of the Ontarian lobe, a last-gasp glacial advance in this area. This represents its easternmost extent.

Gravelly delta
To the left (N) in a large gravel pit are foreset beds of a gravelly delta. As its top elevation is about 520', it would be assigned to post-glacial Lake Amsterdam of Fairchild.

Climb up 520 foot terrace
Cross West Canada Creek, leaving Herkimer, and climb hill to the top of the 520-foot terrace along the north side of the Mohawk Valley.

Gravel pits
To the left are large gravel pits in lenticular coarse gravel and sand beds.

STOP 1 Moss Island, in Little Falls, N. Y.
The bedrock here is quartzose syenite gneiss of Precambrian age, faulted up on the Little Falls fault block. The same rock forms the cliffs to the south, across the canal. The line of the top of the cliffs is approximately the unconformity on which the Cambrian Little Falls dolomite lies, though the dolomite is not visible from here, in the woods above the cliffs. This raised block of resistant rock formed the pre-glacial divide between the Hudson and St. lawrence drainage basins. However, following melting back of the continental ice sheet to the extent that the Hudson and Mohawk valleys were open, and the St. Lawrence still dammed, this valley drained ice melt-water from the entire eastern Great Lakes (Lake Iroquois). This discharge, probably at least as large as the present Niagara River, cut down the divide here, resulting in its westward shift to Rome, N. Y.
Walk northward across Moss Island. Along most of the northern margin is a complex of enormous potholes cut when the post-glacial Great Lakes drainage spilled over Moss Island in a thundering cataract.

Syenite gneiss
Road cut in Precambrian greenish-gray, brown-weathering syenite gneiss.

Little Falls fault-line scarp
Downgrade toward the east, Rte. 5 crosses the Little Falls fault-line scarp. On the Little Falls block is Precambrian gneiss. East of the fault is Utica shale covered with glacial and alluvial deposits. Cushing estimates the displacement here at between 750 and 850 feet.

Gravel pits
To the left (N) are large gravel pits cut into the side of the 460-foot terrace.

STOP 2 East Canada Creek gorge at Beardslee power station.
FOLLOW LEADERS CLOSELY PAST STATION. DO NOT ENTER STATION OR GO NEAR HIGH TENSION LINES AND TRANSFORMERS.
Water levels permitting. we will go down the steps by the station, cross the creek bed on a concrete wall, and hike for about one half mile up the gorge. Opposite the power station the Manheim fault is well exposed. The displacement is estimated by Fisher (1954, p. 78) to be about 400 feet. Sulphides in the fault zone once led to an abortive attempt to open a lead mine. The upstream (upthrown) wall is Little Falls dolomite. At the base of the downstream (downthrown) wall are a few beds of the uppermost Shoreham limestone (coarse calcarenite) overlain by about 25 feet of the Dolgeville facies, interbedded barren limestones and dark shales between fossiliferous Trenton limestones and overlying black shale. Overlying the Dolgeville beds is the Canajoharie blaok caloareous shale, equivalent to the Denmark limestone of lower Trenton Gorge (Stop 6).
About 100 feet upstream from the fault are two thin (6") alnoite dikes bearing biotite phenocrysts. In the same locality the dolomite contains a greenish-gray chert bed about 8 inches thiok, and an intraformational breccia bed several feet thick exposed on the wall beside the lower pool.
In the middle area of the gorge, opposite the old mill ruin, there are several large potholes loaded with the tools of their erosion. Just above the area of the potholes is 1 to 2-foot bed of contorted laminated sandy dolomite, with some cabbage-head forms attributed by Dr. Donald Fisher to cryptozoon. In this part of the gorge there are fractures and vugs containing calcite and quartz crystals, and anthraxo1ite (identified by Dr. James R. Dunn).
Upstream from the broad upper pool the uppermost 10 to 15 feet of the Little Falls formation is the "reddish zone", whioh contains graded sandstone and intraformational breccia beds. The overlying Lower Ordovician Tribes Hill formation is composed of fossiliferous limestone and dolomite, commonly muddy and sandy, with a "fretwork" weathered surface. One of the least inconspiouous of -the fossils is a gastropod, Ophileta sp. The Tribes Hill formation, about 45 feet thick here (Fisher, 1954, P. 93), forms the ledges for some distance both down and upstream from the old dam.
Overlying the Tribes Hill with a distinct change in lithic type is Lowville limestone, of Black River age, a gray calcilutite. This appears below the newer dam, with its distinctive worm tube, Phitopsis. Here also there are several minor faults, and veins containing pyrite. There are some veins of anthraxolite and quartz crystals, along joint surfaces.
Return to buses by walking south next to the penstock until there is room to pass beneath it.

Manheim fault to left
To the left the bluff is the fault-line scarp of the Manheim fault, which will be seen at close hand at the Beardslee power station.

View of Little Falls fault in distance.
Bluff in the distance to the left (W) is the fault-line scarp of the Little Falls fault. Little Falls dolomite forms the bluff, faulted up against the Utica shale (down on the east).

STOP 3 Disembark for lunch.
Lunch stop. Lunch is being served by the Rebeccas of Dolgeville in their hall to the rear of the brown frame building on the southwest side of the street.

Little Falls fault-line scarp.
Ahead and to the left (W) is the Little Falls fault-line scarp. Precambrian Grenville rock underlies the hills, with down-faulted Trenton limestone and shale opposite on the east.

STOP 4 Basal Cambrian unconformity.
Diamond Hill. Disembark, and walk downstream on the near side of Spruce Creek, to the right of the old bridge.
Little Falls fm. on Grenville gneiss. Conglomeratic basal beds on the upper Cambrian Little Falls formation overlap northward a hill of Grenville quartzose gneiss. Upstream the gneiss occupies an elevation 100 feet or more higher than the basal beds of the Little Falls lying on the gneiss at the foot of the cascades. The initial dip of the Little Falls beds is noticeable.
Shoreham limestone crops out only one half mile WNW at an altitude of 1460 feet. Inasmuch as Grenville gneiss crops out on Diamond Hill at least as high as 1360 feet, only about 100 feet are available for all the formations between the Shoreham and Precambrian. The Little Falls alone is 450 feet thick in cliffs south of the Mohawk River at Little Falls.
MR. D. H. BURRELL, THE OWNER OF THIS PROPERTY, HAS GIVEN US PERMISSION TO BE HERE, AND REQUESTED THAT NO ONE EXCAVATE IN SEARCH OF LITTLE FALLS "DIAMONDS". BE ESPECIALLY CAREFUL NOT TO DEFACE THE NATURAL BEAUTY OF HIS PROPERTY.

Climb through stratigraphic section
The road west climbs up through the stratigraphic section from Little Falls to Utica shale, and back down again as it descends into West Canada Creek Valley at Middleville.

View west into West Canada Creek Valley.
View west into West Canada Creek Valley. Harter and Hasenclever Hills, on the opposite side of the valley, are underlain by Utica shale, capped by Frankfort shale. Precambrian gneissoid syenite crops out in the bottom of the valley at Middleville.

Road cut in Kirkfield and Shoreham limestones.

Road cut in Little Falls dolomite.

STOP 5 Stratigraphic section on "City Brook"
At junction with gravel road, forking downhill to left, stop and disembark, and walk down the gravel road to "City Brook" (Wolf Hollow Brook). This locality is known as Old City.
This section, discussed by Kay (1953), includes much of the Little Falls dolomite, and extends upward through the Lowville, Kirkfield, Shoreham and well into the Denmark formation.
The top ot the Little Falls formation is the top of the sandy dolomite stratum in the bed of the creek immediately upstream from the bridge at Old City. Crytozoon is abundant in four feet of dolomite about 60 feet below the top of the formation.
The Canadian strata, present at Stop 1 (45 feet of Tribes Hill fm.), are missing between the Little Falls and Lowville on City Brook.
The Lowville formation forms the lower 26 teet of the cascades and is exposed in the small quarry south of the creek. The lower member, seven feet thick here, is tan-weathering, gray-brown, medium textured, heavy-ledged, tough, sandy and muddy limestone. The upper member, here 19 feet thick, is light-gray-weathering, medium gray calcilutite with some shale partings. A 3-inch metabentonite bed can be seen approximately at the base of the upper member, well exposed about 3 feet above the floor of the quarry. The Lowville is the only member of the Black River group present. The Rockland limestone is not present here, even though it is 13 feet thick above the Lowville at Ingham Mills on East Canada Creek, and 8 feet thick in a quarry one mile northwest ot Newport.
The Kirkfield formation, overlying the Lowville here, is interbedded thin-bedded limestone and black calcareous shale, abundantly fossiliferous, about 45 feet thick at City Brook. A metabentonite bed is weathered far back in a recess part way up the falls, about 8 teet above the formation base. The uppermost beds are thick calcarenite strata, some ot which have para-ripples.
The Shoreham limestone, overlying the Kirkfield, is 45 teet thick here. The lower part is interbedded thin-bedded shell limestone and calcareous shale, with the trilobite Cryptolithus common a few feet above the base on City Brook. The upper 9 feet, called the Rathbun member by Kay (1953, p. 44), has a basal ledge of calcarenite, above which are interbeds of calcilutite, coquina-calcarenite, and calcareous shale. Below the upper bridge is a zone where the bryozoan Prasopora is large and common.
The basal Denmark beds, of the Poland member, appear in a ledge to the right of the creek as one proceeds about 100 feet upstream from the upper bridge. They are black, irregular, impure bituminous limestone beds in which the cephalopods Geisonoceras, Endoceras, and Trocholites are abundant. About 3 feet above this Trocholites zone is the lowest Poland metabentonite. In its lower 50 feet here the beds are typically Poland in rock type, heavy-ledged, fine-grained, fossiliferous limestone, though there are some relatively barren, knobby-surfaced calcilutite beds. Farther upstream are barren, fine-grained limestone beds intercalated with black calcareous shale, typical of the Dolgeville facies, probably equivalent to the lower Russia member (upper Denmark) at Trenton Falls (Kay, 1953, p. 53).

View of terrace
The conspicuous terrace across the valley to the left (SW) is the result of resistant limestone beds at the base of the Poland member of the Denmark limestone (Kay, 1953, p. 105).

Post glacial lacustrine sediments
Northwest of Newport, there is a low-level floodplain terrace to the right (NE). Higher knobs northeastward are dissected remnants of once continuous varved clay overlain by sand. The top of the clay is persistent at about 800 feet, and the top of the sand at about 1000 feet (Kay, 1953, p. 97). They are post glacial lacustrine sediments.

Basal Poland limestone stratum plain terrace
The basal Poland limestone stratum plain terrace continues across the river to the left (SW).

Kames to the right
Knobs to the right (NE) are probably kames. In some cases, at least, they are composed of sand and gravel (Kay, 1953, p. 97).

STOP 6 Lower end of Trenton Gorge.
Stop at intersection in Trenton Falls hamlet, and disembark. Cross the bridge over West Canada Creek, keeping in narrow file on the upstream side of the bridge. Turn left at east end of bridge, and descend to ledges. The ledges upstream from the bridge are in the lower part of the Poland member of the Denmark formation, and are only a few feet higher than the lowest beds of the Trenton Falls section which Kay has described (1953, p. 27). Here the Poland member is composed of heavy ledges of black, fine-grained, fossiliferous limestone interbedded with fossiliferous calcareous shale. Upstream one hundred yards or so can be seen the two metabentonite beds, about nine feet apart, weathered back into the wall of the gorge. These are the second and third metabentonites in the Poland. The Poland limestone ledges in the stream channel above the bridge are equivalent to the Canajoharie shale above the thin remnant of the Dolgeville facies downstream from the fault at Beardslee power station (Stop 1).

STOP 7. Middle Trenton Gorge.
Turn left before reaching gate, toward parking area by barn. Disembark, and walk up the road through the gate. The ledges exposed in and beside the road are in the upper part of the Rust member of the Cobourg formation. About 300 yards up the road one can look down into the gorge to the right (E) and see the brink of the upper high falls. The base of the Cobourg is at the base of the upper high falls. The Rust member, 115 feet of thin limestone beds intercalated with shale, forms most of the gorge wall here. Just below the parking area and garage-like building at the dam, an abandoned road leads diagonally down the wall of the gorge toward the base of the dam. The weathered road cut is abundantly fossiliferous. From the bottom of this road, above the penstocks below the dam, one can look across the gorge to see the 15-foot contorted zone just below the lip of the spillway. This zone is discontinuous, but appears in varying thicknesses at this horizon in many places on the gorge wall. It is the result of a submarine slide. This is indicated by the coarse calcarenite bed immediately overlying the contorted zone, which fills in hollows and around fragments at its base, and has a comparatively even upper surface. At the top of the eastern gorge wall, above the dam, are the thick beds of the Steuben limestone, the upper member of the Cobourg. In the vicinity of East Canada Creek (stop 1) the entire Cobourg formation and most of the Denmark have changed facies to black calcareous shale in which the contact between the Canajoharie and Utica shales is obscure.

Crest of Marcy Hill
Crest of Marcy Hill, capped by lower Cincinnatian Frankfort shale. The lower slopes of the hill, both north and south, are underlain by Utica shale.

GUIDEBOOK TO FIELD TRIPS
NEW YORK STATE GEOLOGICAL ASSOCIATION
33rd Annual Meeting
Robert G. laFleur
Editor
Contributing Authors
James R. Dunn
Donald W. Fisher
Philip C. Hewitt
Shepard W. Lowman
Lawrence V. Rickard
Host
RENSSELAER POLYTECHNIC INSTITUTE
Troy, N. Y.

A: GLACIAL FEATURES IN THE VICINITY OF TROY, N.Y.
by Robert G. laFleur
Depte of Geology, Rensselaer Polytechnic Institute
2010: No actual trip is described in the Guidebook, however a number of "Selected Exposures" are. Their locations are often not well constrained. Only some have been found, sometimes using considerable guesswork.

STOP 1. Drumlins
Dozens occur between the Wynantskill and Moordenerkill in the towns of North Greenbush, East Greenbush, and Schodack. Long axes trend about N20W. See Plate II.

STOP 2a. Esker at Moule's Lake
Eskers. Many occur throughout the Albia-Burden Lake moraine. The most typical are at Moule's Lake, Coopers Pond and West Sand Lake. Two others feed the Schodack Terrace at East Greenbush and along the Vlockie Kill. Esker deltas are extensively excavated 2 miles ESE of West Sand Lake.

STOP 2b. Esker at Coopers Pond
2. Eskers. Many occur throughout the Albia-Burden Lake moraine. The most typical are at Moule's Lake, Coopers Pond and West Sand Lake. Two others feed the Schodack Terrace at East Greenbush and along the Vlockie Kill. Esker deltas are extensively excavated 2 miles ESE of West Sand Lake.

STOP 2c. Esker at West Sand Lake
Eskers. Many occur throughout the Albia-Burden Lake moraine. The most typical are at Moule's Lake, Coopers Pond and West Sand Lake. Two others feed the Schodack Terrace at East Greenbush and along the Vlockie Kill. Esker deltas are extensively excavated 2 miles ESE of West Sand Lake.

STOP 2d. Esker at East Greenbush
Eskers. Many occur throughout the Albia-Burden Lake moraine. The most typical are at Moule's Lake, Coopers Pond and West Sand Lake. Two others feed the Schodack Terrace at East Greenbush and along the Vlockie Kill. Esker deltas are extensively excavated 2 miles ESE of West Sand Lake.

STOP 2e. Esker along Vlockie Kill

STOP 2f. Esker delta pit
Esker deltas are extensively excavated 2 miles ESE of West Sand Lake.

STOP 3a. Kame SE of Wynantskill
Kames. Exposed along Rt. 66 SE of Wynantskill, south of Eagle Mills, and E. of the Wynantskill at West Sand Lake. Solitary kames occur one mile north of Poestenkill.

STOP 3b. Kames south of Eagle Mills
Kames. Exposed along Rt. 66 SE of Wynantskill, south of Eagle Mills, and E. of the Wynantskill at West Sand Lake. Solitary kames occur one mile north of Poestenkill.

STOP 3c. Kames at West Sand Lake
Kames. Exposed along Rt. 66 SE of Wynantskill, south of Eagle Mills, and E. of the Wynantskill at West Sand Lake. Solitary kames occur one mile north of Poestenkill.

STOP 3d. Solitary kame

STOP 3e. Solitary Kame

STOP 4a. Ice contact north of Sheer Road
Several ice contacts cross the Albia-Burden Lake moraine. Three (in order of sequence) occur (1) north of Sheer Rd., (2) one mile SE of West Sand Lake, and (3) along Rt. 154 at Moule's Lake. All of these contacts are fed by eskers some of which are a mile in length.

STOP 4b. Ice contact SE of West Sand Lake
Several ice contacts cross the Albia-Burden Lake moraine. Three (in order of sequence) occur (1) north of Sheer Rd., (2) one mile SE of West Sand Lake, and (3) along Rt. 154 at Moule's Lake. All of these contacts are fed by eskers some of which are a mile in length.

STOP 4c. Ice contact at Moule's Lake
Several ice contacts cross the Albia-Burden Lake moraine. Three (in order of sequence) occur (1) north of Sheer Rd., (2) one mile SE of West Sand Lake, and (3) along Rt. 154 at Moule's Lake. All of these contacts are fed by eskers some of which are a mile in length.

STOP 5. Schodack Terrace.
Extensively developed through the Town of Schodack. Kamey in part with large kettles and a few short eskers. Deltaic sediments exposed along the western edge.

STOP 6a. Hampton Ice-margin delta.
Exposed at Hampton Park and one mile east of Rensselaer. Extensive gravel pits at both localities. Especially good bottomset structures at the latter.

STOP 6b. Rensselaer Ice-margin delta.
Exposed at Hampton Park and one mile east of Rensselaer. Extensive gravel pits at both localities. Especially good bottomset structures at the latter.

STOP 7. Superglacial kame terrace
Superglacial kame terrace and ground-laid ice-border outwash gravels are extensively exposed in a pit south of Williams Rd., North Greenbush. Terrace is continuous south to Defreestville where it terminates in a small delta.

STOP 8a. Lacustrine varved clays
Lacustrine varved clays with interbedded sands underlie a large area west of Rt. 4 and the Boston and Albany tracks. Good exposures are limited but occur along the entrance road to the paper company just north of Castleton ...

STOP 8b. Lacustrine varved clays
Lacustrine varved clays with interbedded sands underlie a large area west of Rt. 4 and the Boston and Albany tracks. Good exposures are limited but occur [...] along Mill Creek north of Rysedorph Hill...

STOP 8c. Lacustrine varved clays
8. Lacustrine varved clays with interbedded sands underlie a large area west of Rt. 4 and the Boston and Albany tracks. Good exposures are limited but occur [...] along Spring Street where about 35 feet of clay overlying gravel is exposed in a pit.

STOP 9a. Beaches
The Lake Albany beach is well developed, with frequent storm ridges, at (1) one mile SE of South Schodack [...] Gravel pits provide cross-sections through the beach at all of these locations.

STOP 9b. Beaches
The Lake Albany beach is well developed, with frequent storm ridges, [...] along the Wedge of the Schodack terrace between Brookview and East Greenbush [...]. Gravel pits provide cross-sections through the beach at all of these locations.

STOP 9c. Beaches
9. Beaches. The Lake Albany beach is well developed, with frequent storm ridges [...] from Defreestville E of Rt. 4 north along Blooming Grove Rd. Gravel pits provide cross-sections through the beach at all of these locations.

STOP 10. Peat bog
Peat bogs are common throughout the area. Peat is presently being dug from a bog one mile SE of West Sand Lake.

STOP 11a. River terrace
River terraces are best developed along the Poestenkill between Eagle Mills and Troy, and also ....

STOP 11b. River terrace
River terraces are best developed along the Poestenkill between Eagle Mills and Troy, and also ....

STOP 11c. River terrace
River terraces are best developed along the Poestenkill between Eagle Mills and Troy, and also...

STOP 11d. River terraces
River terraces are best developed [...] , and also along the Wynantskill in Albia.

STOP 12a. Post-glacial rock gorges
Post-glacial rock gorges with falls are found on the Poestenkill near Pawling Ave. in Troy...

STOP 12b. Post-glacial rock gorges
12. Post-glacial rock gorges with falls are found [...] on the Wynantskill along the Airport Rd. in Troy...

STOP 12c. Post-glacial rock gorges
Post-glacial rock gorges with falls are found on [...] Mill Creek along Rt. 151 near Rensselaer.

STOP 13a. Panoramic view of Hudson Valley
13. Promontories at Teller Hill near Sherwood Park [...] offer panoramic views of the Hudson Valley.

STOP 13b. Panoramic view of Hudson Valley
Promontories at [...] Rysedorph Hill, [...] offer panoramic views of the Hudson Valley.

STOP 13c. Panoramic view of Hudson Valley
Promontories at [...] Prospect Park in Troy offer panoramic views of the Hudson Valley.

B: SOME ASPECTS OF TURBIDITE SEDIMENTATION IN THE VICINITY OF TROY, NEW YORK
By Shepard W. Lowman
Dept. of Geology, Rensselaer Polytechnic Institute
In the course of geologic field work in the vicinity of Troy, New York, much interest and controversy have been evolved locally on the subject of deep water flow sediments, generically called turbidites. Numerous and highly varied types of turbidites are exposed within the immediate environs of Troy. Complicating factors in field mapping are the Logan Line thrust fault and the sharp local folding both of which produce tectonic breccias and otherwise complicate the definition and identification of stratigraphic units.

STOP 1. Deepkill Euxinic Assemblage
The first stop will be at the type locality of the Deepkill, one-quarter mile east of Grant's Hollow, ten miles north of Troy on Route 40.
The upper Deepkill is separated from the lower by a covered interval of 800 feet, and its rocks comprise a different assemblage from the euxinic lower Deepkill. The upper Deepkill is a series of mud flows, clay-in-clay brecciolas, a few lime-in-clay brecciolas, porcelanites, and thin beds of chert. Near the bottom of the section there is a small amount of graptolitic black shale and dark gray limestone. This part of the Deepkill is mentioned because its proximity makes it available for those who may be more interested in spending a half-hour on this additional sedimentary type than in collecting graptolites and turbidites from the lower Deepkill.
Both the top and the bottom of the lower Deepkill are covered. The part of the section which is exposed is made up of black shale, gray shale, light gray thin bedded siltstones in banks one to four feet thick, and various types of brecciolas and graded beds.
This assemblage appears to be produced by two sets of factors. First, the underlying euxinic chemical environment dominated by H2S affects Eh much more than pH (Krumbein and Garrels 1952). This permits the accumulation of lime mud at one time and sapropelitic black mud at another depending on alternating chemical controls that are related to tectonic activity on the basin margin. An example is the Black Sea where the lime muds overly sapropelitic ooze (black organic shale) and the two are separated by a thin layer of terrigenous sand (Archanguelsky 1927). The second set of factors are those which produce turbidites of various kinds, brecciolas and graded beds of one kind or another depending on the speed of flows from the upper parts of continental slopes triggered by faulting or by overloading of metastable shelves. More gentle currents from continental shelves would bring a steadier supply of sand and silt to build the banks of thin bedded siltstones.
When turbidity flows were in action and diluted the euxinic environment, then lime muds or organic ooze would not be present as pure rock types, but when the flows died down the euxinic deposits would form the dominant rock type with alternation from lime to mud to organic ooze, and with an occasional turbidite flowing into the depositional area from one side of the basin or the other,
The faunal evidence as analyzed by Ruedeman fits well with the postulated euxinic environment. The predominant fossils are graptolites which are thought to be pelagic or pseudopelagic (i.e. living attached to seaweed). Other fossils are rare and are thin shelled chitinous forms which appear to be well adapted to a pseudopelagic environment. Other bottom dwelling types are wanting in the shales, silts, and calcilutites.

STOP 2 - OVERVIEW
Schodack Brecciola Assemblage: See Figure 3. Four brecciolas are described which apparently belong to the Schodack (West Castleton) Formation. These are typically developed at the following locations: School 14, west edge of playing field at 13th St. and College Ave., Sage Avenue, 250 feet west of 15th Street, R.P.I. Campus, east end of football field, and Troy High School, northwest corner of athletic field. All four occurrences appear to be distinctive, and they are not noticeably lenticular like the brecciolas of the upper and lower Deepkill some of which lens out across the outcrop. The Sage Avenue brecciola occurs at four localities one-half mile apart, and is clearly recognizable at each locality. The Troy High School sequence of brecciolas occurs in two extensive outcrops, approximately 800 feet apart, at both of which it possesses the same distinguishing characteristics. All four brecciolas are sharply distinct from one another, except that all are ten to twenty feet thick without marked lenticularity. They differ in this respect from the Deepkill brecciolas, which are inches thick and sharply lenticular. The brecciolas described by Migliorini in the Apennines appear to be closer to the Deepkill variety than to those of the Schodack. The Grand Banks brecciola of 1929 was calculated to be 16 to 40 inches thick. By comparison, the Schodack brecciolas are unusually large, although not to be compared to the Rysedorph megabreccia facies of the Snake Hill (Middle Ordovician) (J.G. Elam, 1960 unpublished).

STOP 2A. School 14 locality
(North of College Age. along an extension of 13th Street at west edge of playground of School 14.) One hundred feet of outcrop extends north-south, strikes N25E and dips 45° southeast with the top of the section to the southeast as judged by graded bedding. The south end of the outcrop is a pale, gray-green quartzite, poorly sorted and mostly fine grained. The MATRIX is a brownish purple, fine grained sandstone or siltstone with frequent coarse, round, sand grains and some clay, much calcareous dust and small calcareous fragments, many blobs of clay varying from black to light gray, and also with frequent light gray calcareous granules. The FRAGMENTS are coarse-grained, light-gray, massive, and fossiliferous limestone varying in shape from irregular to round to tabular. Average size is 2"-5" with some longer dimensions up to l5". There are also a few large slabs the largest of which is two feet thick and eight feet long. The general orientation of fragments is subparallel to the boundaries of the main flow. Abundant small clay blobs about 2" across are also found, along with some dense light gray limestone fragments and a few sandy fragments. At the north end of the outcrop the ratio of pebbles to matrix is about 30:70 varying to 20:80 near the middle, and dropping to 10:90 at the south end of the brecciola outcrop. This indication of grading suggests the beds are right side up with the top to the south east.

STOP 2B. Sage Avenue locality - 15th Street occurrence.
The outcrop is buried beneath the buildings along 15th Street in the vicinity of the 15th Street Lounge. Large boulders 4' by 6' were blasted from an old quarry wall and moved by bulldozer to their present location between the South Parking Lot and the tennis courts. There is one predominant type (TYPE 1) of rock, which makes up about 90% of the boulders and there are several subsidiary types. TYPE 1. FRAGMENTS: About 80% of the fragments are coarse grained, fossiliferous, light gray, limestone, averaging 4" to 6" in size, irregular to sub-spherical in shape, with no linear distribution, and with no noticeable grading. Since the occurrence is a pile of boulders there are no observable stratigraphic relationships. Minor constituents are small fragments of light gray, dense limestone and sandstone of which the former is more abundant. MATRIX is a brown-weathering dolomite mud with numerous medium to coarse, rounded sand grains. About 20 to 50% of the matrix is composed of light gray, dense, calcilutite fragments averaging 0.25" in diameter. These give the matrix the appearance of a pebble conglomerate. The relative abundance of matrix and fragments is variable from boulder to boulder but the general average is about 60% fragments, not counting the 1" calcilutite fragments that appear to make up a considerable part of the conglomeratic matrix.

STOP 2C. R.P.I. Campus locality
(12' brecciola outcropping on R. P. I. campus east of football field) The general dip of 20° to the east places this brecciola beneath the "Sage Avenue brecciola". It is underlain by greenish-gray clay with interbeds of dolomitic fine-grained sandstone two to three inches thick and six to ten feet apart. The brecciola is overlain by greenish-gray shale with thinly interbedded siltstone or very fine grained sandstone. The interval from the top of the "campus brecciola" to the base of the "Sage Avenue brecciola" appears to be 15 to 30 feet, with the latter being the younger of the two. MATRIX is dark gray, flow-streaked mudstone. No evidence is seen of stratigraphic differentiation, graded bedding, or direction of flow. FRAGMENTS are predominantly (80%) coarse grained light gray, fossiliferous limestone, ranging in size from 2" to 1.5 feet, irregular in shape and with no preferred orientation. There are a few small fragments of dense light gray limestone, about one per cent by volume. Medium grained, rounded sandstone makes up about 20% of the fragments with irregular distribution and no preferred orientation. FRAGMENTS & MATRIX: Relative percentage of fragments to matrix is 4O:60 to 50:50: Evidence of scour is seen in the presence of green clay blobs in the lower part of the flow. Load casts are also present in the form of green clay injected into the base of the brecciola. STRATIGRAPHIC CORRELATION: This brecciola is lithologically closely similar to the lower brecciola at Dunn Garden Apartments (Hoosick & Burdett). It also falls in the same succession of beds and is thought to be stratigraphically equivalent.

STOP 2D.

STOP 2E. North side of Beman Park

STOP 2F. Dunn Garden Apartments.

STOP 2G. Troy High School Playing field.
(Sequence at the east end of the track and playing field north of Troy High School on Burdett Avenue.) Strike of these beds is N15E, dip is 75 west, top of the stratigraphic section is to the west, The brecciola sequence is made up of three members with eleven submembers. It is overlain by thin bedded, fine grained sand and shale with a possible thickness of 200 feet. The brecciola sequence is underlain by brown weathering green claystone with dark gray wispy interbeds, having a possible thickness of 300 feet. The thickness of the brecciola sequence is approximately 90 feet. The Troy High School outcrop is the most extensive and gives the best picture of both the brecciola and the beds associated with it. Brecciola Sequence (in descending order) Bed 3b; Mostly covered but with occasional patchy outcrops of dense, light gray limestone fragments in a dark gray clay matrix. A large outcrop that is probably stratigraphically equivalent occurs at the southeast corner of Burdett Avenue and West Peoples Drive., This outcrop has a ratio of fragments to matrix of about 15:85; the fragments are uniformly light gray, dense limestone, 2" to 3'" thick, 8" long, and randomly oriented. The matrix is uniform dark gray claystone. 3a. Thin bedded light gray dense limestone, interbedded with thin beds of dark gray shale. Unit is regularly bedded but slightly disturbed, giving the appearance of layers being slightly pulled apart in sedimentary boudinage. This occurrence, which is 2 feet thick and over 8 feet long, may be a large mass that slid or flowed some distance without turbulence, or it may have slid only a few inches or feet, but enough to cause the disturbance noted. Similarly bedded limestone in a similar stratigraphic position occurs about 500 feet to the east across the High School playing field. Bed 2e. Three feet of tan weathering green claystone with numerous black wispy streaks that show flow bedding. 2d. One and one half feet of light gray, dense limestone fragments in a dark gray matrix with 10:90 ratio, fragments are 2 by 6 inches and randomly oriented. 2c. Two and one half feet of tan weathering green claystone. 2b. One foot of green clay blobs (1" to 2") in maroon weathering clay matrix; ratio 20:80. 2a. Seven feet of green clay with black wispy interbeds and one interbed of coquina one inch thick with worm borings, giving supporting evidence of top and bottom. Bed 1d. Four feet of light gray dense limestone and black shale fragments in a rusty, medium-grained, rounded sand matrix with a 20:80 ratio. Fragments and trains of fragments are subparallel to the margins of the flow. A small percentage of the limestone fragments are granular and fossiliferous. A few others are light brown and well-bedded. Average size of limestone fragments is 3 by 6 inches. 1c. One foot thick, similar to above but with sand and clay matrix 50:50, and showing an increase in the percentage of limestone fragments to matrix, to about 40:60. 1b. Black shale boulder one foot thick and eight feet long, oriented parallel to the margins of the brecciola. 1a. Brecciola bed five feet thick, ratio of limestone fragments to clay matrix is 80:20. Orientation of fragments is sub-parallel to the boundaries of the brecciola. The limestone fragments are mostly dense light gray limestone, granular fossiliferous light gray limestone, and light brown well-bedded limestone in a ratio of 60:20:20. The matrix is dark gray clay. SYNOPSIS OF MAIN BRECCIOLA MASS (Beds 1a-1d) GRADED BEDDING. The sand matrix shows incipient grading above bed lc which is mixed sand and shale. The main mass of the flow 1a-1d shows marked increase in the abundance of limestone fragments downward through the flow. OTHER CRITERIA OF TOP AND BOTTOM. Worm borings: as noted under 1a. Scour: the basal portion of 1a shows many wispy blobs of green clay that appear to have been scoured from the underlying green clay beds while they were unconsolidated. STRATIGRAPHIC DIFFERENTIATION. MATRIX: The sand and clay matrices appear to be well differentiated stratigraphically FRAGMENTS: The fragments are less well differentiated than the matrix but they do show a notable differentiation from the top to bottom. Toward the top of the bed, the limestone pebbles are mostly calcilututes while at the base the pebbles contain about 10% of calcarenites. The pebble-to-matrix ratio is perhaps 20:80 toward the top, increasing to 80:20 toward the base. At the top of the main brecciola the matrix is nearly pure sand; this changes gradationally downward to sandy clay and to nearly pure in clay in the base of the flow. Correlation of separate outcrops on the west and east sides of the athletic field is satisfactory. On the west side the units are oriented from top on the west to bottom on the east; on the east side the orientation of the same sequence has the top on the east and bottom on the west. In spite of this structural complication the correlation of the various brecciola units can be made in some detail.

C: SILURIAN AND DEVONIAN ROCKS OF THE CENTRAL HUDSON VALLEY
By James R. Dunn
Dept. of Geology, Rensselaer Polytechnic Institute
and
Lawrence V. Rickard*
N.Y. State Geological Survey, Albany, N.Y.
Limestones, shales, sandstones, and conglomerates comprise the Silurian and Devonian sequence of the Hudson Valley. Only the youngest portion of the Late Silurian is represented (Rondout Formation), whereas most of the Early and all of the Middle Devonian is present. Late Silurian (Cayugan Series) rocks are thin, and rest unconformably upon folded and eroded Middle Ordovician shales and sandstones. The Early Devonian rocks are divided into the Helderbergian and Ulsterian Series (Rickard, in press), and consist of limestones in the lower part and shales and sandstones in the upper portion. The overlying Middle Devonian sequence (Erian Series) begins with the Onondaga Limestone and continues above into marine and non-marine shales and sandstones of the Hamilton Group. Fossils are common throughout most of the Silurian-Devonian sequence of the Hudson Valley. Marine assemblages are particularly rich in the Helderberg limestones, the Onondaga Limestone and the lower, marine portion of the Hamilton. Plant fragments are the only abundant fossils in the non-marine rocks near the top of the sequence.
*Published by permission of Ass't. Commissioner, N. Y. State Museum and Science Service

STOP 1A. Callanan Road Improvement Company Quarry, NE part.
Outcrop has Normanskill shales, siltstones, and graywackes at the base, overlain by the full thickness of the Rondout Formation and 12 feet of the Manlius Formation. All units are essentially conformable even though they are of Ordovician, Silurian (7) and Devonian ages. Of particular interest are the abundant Tentaculites in the lower unit of the Manlius Formation and the transparent obtuse rhombohedrons of calcite associated with quartz crystals in the Rondout Formation.

STOP 1B. Callanan Road Improvement Company Quarry, center.
The walls of the quarry have typical Hudson Valley thrust fault structures. The Rondout, Manlius, Coeymans and part of the Kalkberg formations are exposed in the walls of the quarry. Plate VI is a picture of the quarry, looking south, in which the faults and formations are indicated.

STOP 2. Synclinal structure
New Scotland Limestone, Becraft Limestone, Glenerie Sandstone and Chert (Oriskany) and Esopus Shale are exposed. The Becraft Formation is thrust over the Glenerie Formation at the east side of the structure, and a zone of cleavage and shear in the Becraft branches north-northwestward from the thrust fault. Plate V is a map of the area and Plate II shows a cross-section through the structure which was core drilled about 10,000 feet southeast of Stop 2.

STOP 3. An exposure of the Esopus Formation in a cliff.
The Glenerie Formation and the Becraft Formation are exposed at the base.
2010: It appears that this cliff has been consumed by quarrying operations.

STOP 4A. Mt. Marion beds, lower part.
The exposure is in an old quarry from which flagstone was produced. Brachiopods and Tentaculites are abundant.

STOP 4B. Mt. Marion Sandstone, upper part.
The exposures are in a quarry from which flagstone was produced. Lack of marine fossils and the fairly common plant remains suggest non-marine origin.

STOP 5. Onondaga Reef.
This is one of the reefs which is typical of the Onondaga Formation in New York. Fossil collecting is excellent.

STOP 6. Broncks Lake stratigraphic section.
All units of the Kalkberg Formation are exposed but not fully. All of the New Scotland and Becraft Formations can be seen, and 24 feet of the Alsen Formation is visible. The strata dip steeply westward and are cut by a fault which repeats part of the Kalkberg Formation.

D: STRATIGRAPHY AND STRUCTURE IN THE SOUTHERN TACONICS (RENSSELAER AND COLUMBIA COUNTIES, NY)*
By Donald W. Fisher
Geological Survey, N.Y. State Museum and Science Service, Albany, N. Y.
"The structural [and stratigraphic] investigation of the Taconic region is only in its beginning stages, and ... the interpretation of one particular area, to be satisfying, should allow correlations with adjoining areas. In this region of dense underbrush, extensive forests, widespread till cover, low relief, and few fossil localities, facts and observations are hard to accumulate, and their interpretation is beset with difficulties."
*Published by permission of the Assistant Commissioner, New York State Museum and Science Service.

STOP 1. Slump blocks of Austin Glen
Slump blocks of Austin Glen Graywacke and Trenton Limestone in badly deformed Snake Hill Shale.

STOP 2a. Greenish-gray slaty argillite of Mettawee Formation.

STOP 2b. Vertical beds
Interbedded black shale, limestone and calcareous sandstone, beds nearly vertical, Lower Cambrian.

STOP 2c. Grayish-green slaty argillite of Mettawee Formation.

STOP 2d. Vertical beds
Principally on west-bound lane; essentially vertical beds of interbedded black shale, limestone and calcareous sandstone, probably Lower Cambrian.

STOP 2e. Nassau Formation
Principally on westbound lane; purple and green shales with interbedded thin red and green siltstones. Nassau Formation.

STOP 2f. Walloomsac (?)
Black slate, presumably Walloomsac, no fossils yet found, purple and green Nassau beneath, along town road. Nature of contact disputable.

STOP 2g. Anticline in Walloomsac (?)
Anticline in black slate (Walloomsac ?) on east-bound lane. Amos Eaton born at New Concord (Historic marker), 1.1 miles south of East Chatham.

STOP 2h. Mile of Stockbridge dolomites
Along both lanes; 1 mile of exposures of eastward dipping Stockbridge dolomites and dolomitic limestones, locally much deformed.

STOP 3. Eastward dipping Stockbridge carbonates

STOP 4. Balmville and Austerlitz
Fossiliferous Balmville Limestone on dolomite and underneath Austerlitz purple and green phyllite.

STOP 5. Austerlitz
Eastward dipping Austerlitz purple and green phyllite with interbedded thin green chloritic quartzite, black slate outcrops 500' to the west along the R.R.

STOP 6. Austerlitz, Stockbridge, Balmville
In tunnels of the B. & A. R.R.; Austerlitz purple and green phyllite thrust on Stockbridge carbonates, fossiliferous Balmville Limestone locally present.

STOP 7. "Berkshire" black phyllite.

STOP 8. Rensselaer Graywacke
Rensselaer Graywacke with many quartz veins, some of which are feldspar-bearing.

STOP 9. Pine Plains
Interbedded dolomite and shale with ripple marks (?) or flow structure (?) on dolomite, Pine Plains Formation.

STOP 10. Everett Schist
Taconic State Park, green Everett Schist on north side of N. Y. 344 at eastern edge of Park.

STOP 11. Copake and Balmville
Copake Limestone and Balmville Limestone with distorted fossils due to flowage.

STOP 12. Balmville Limestone thrust on Walloomsac Slate

STOP 13. Argillite and quartzite
Green argillite (Elizaville) and chloritic quartzite (Curtiss Mountain) along both sides of Parkway

STOP 14. Germantown
Exposures on both sides of U.S. 9, 0.5 mile south of southern edge of Becraft Mountain; interbedded graptoliferous black shale and limestone (Germantown Fm.) and greenish-gray silty shale with Deepkill graptolites.

STOP 15. Normanskill
Red and green shale and much green chert, lower member of Normanskill Group.

STOP 16. Germantown
Ferruginous quartzite overlying quartzose greenish-gray shale (Germantown Fm.)

STOP 17. Deformed Mt. Merino Shale of Normanskill Group.

STOP 18. Germantown and Mettawee
Interbedded black shale, limestone and limestone brecciola of Germantown Fm. overlying Mettawee green argillite.

STOP 19. Type locality of Stuyvesant Falls Fm.
Type locality of Stuyvesant Falls Fm.; interbedded green silty shale and flow-cast green siltstones and chertified argillite underlying Mt. Merino shale of Normanskill Group.

STOP 20. Type locality of Schodack fm.
Grayish-green argillite (Mettawee) with fossiliferous limestone brecciola (Stuyvesant Conglomerate) near top, Mettawee overlain by laminated siltstones and interbedded black shales. Type locality of Schodack Formation.

STOP 21. Type locality of Normanskill
Type locality of the Normanskill; gray and black shale with interbedded graywacke.

STOP 22. Type locality of the Deep Kill Formation
Type locality of the Deep Kill Formation; interbedded limestone and black shale in lower portion and greenish-gray shale in upper portion overlain by red shale of basal Normanskill. A reverse fault here repeats a portion of the section.

STOP 23. Type locality of Schaghticoke Formation
Type locality of Schaghticoke Formation; interbedded green and black shale and thin limestones and siltstones, all badly deformed.

GUIDEBOOK TO FIELD TRIPS
NEW YORK STATE GEOLOGICAL ASSOCIATION
34th Annual Meeting
Port Jervis, New York
May 4-6, 1962
Wilbur G. Valentine, Editor
Contributing Authors
Helen Antine-Biren
Sidney Fink
Frank W. Fletcher
Elizabeth and Howard Jaffe
John H. Johnsen
William A. Oliver Jr.
Christopher J. Schuberth
John, B. Southard
HOST
Department of Geology
Brooklyn College
Brooklyn 10, N. Y.
Additional copies available from Pennanent Secretary of the New York State Geological Association
Kurt E. Lowe
The City College'
New York 31, N.Y.

A: THE ONONDAGA LIMESTONE AND THE SCHOHARIE FORMATION IN SOUTHEASTERN NEW YORK
William A. Oliver, Jr.
John H. Johnsen.
John B. Southard.
.
Correlation and facies changes in the Schoharie, and Onondaga Formations; relationship to the Esopus Formation; relationship of the outlier at Highlands Mills to the main belt along the Catskill Front.

A: THE ONONDAGA LIMESTONE AND THE SCHOHARIE FORMATION IN SOUTHEASTERN NEW YORK

STOP 1. Erie Railroad Cuts near Highland Mills
Railroad cuts just north of Pine Hill road, NW ninth of Popolopen Lake 7.5' quadrangle, Schunemunk 15' quadrangle.
The contacts between the Highland Mills Member, the middle member, and the Woodbury Creek Member are marked with white paint on the railroad cut.
Watch out for trains.
Although there is a complete section of the Esopus Formation, (p. 13) and the Kanouse sandstone exposed on the east side of the New York Thruway one-half mile east of Highland Mills, the stop will be made at the cut on the Erie Railroad a few hundred yards west of the Thruway, because of traffic danger on the Thruway. Here the Highland Mills Member, the middle member, and the lowest 60 feet of the Woodbury Creek Member (p. 14) are exposed. One-half mile north, the upper non-conglomeratic part of the Kanouse sandstone (p. 14) is exposed on a steep slope just east of the railroad.

STOP2. Leeds Gorge
(Not visited as part of the 1962 trip, but in the Guidebook.)
Gorge of Catskill Creek, just west of Mill Pond in Leeds, SE corner, Leeds 7.5' quadrangle, Coxsackie 15' quadrangle.
Onondaga Formation
This is one of the most complete sections of the Onondaga in the trip area. With a steep easterly dip, the lower 115 feet, conformably overlying the Schoharie Formation, are exposed in a fairly short distance in the bed of the creek. Although the formation is well exposed, only a short time will be devoted to the Onondaga at this stop. Facies changes between here and Kingston (stop #4) are minor and the nature of the rocks and the fossils can be observed to better advantage at that place.
The Leeds Gorge section is as follows:
Moorehouse Member (upper part not exposed):
25'+ | Middle unit; medium-dark-gray, fine-grained limestone with abundant dark-gray chert; corals and bryozoans common, brachiopods and other fossils present.
12' | Lower unit; light-medium-gray, medium-grained limestone with no chert; corals common; other fossils present.
Nedrow Member:
4' | Light-medium-gray, medium-grained limestone with few chert nodules; platyceratids, corals and brachiopods. This unit is lithologically and faunally transitional to the Moorehouse.
39' | Light-medium-gray, medium-coarse and fine-grained limestone with abundant light-medium-gray chert; platyceratids, corals and brachiopods.
Edgecliff Member:
32' | Light-medium and light-gray, medium-coarse and coarse limestone with abundant light-medium-gray chert; large crinoid columnals common, corals, and brachiopods.
3' | Medium-gray, fine-grained limestone with no chert; fragmental fossils.
Transition to Schoharie Formation:
1.5' | Alternating limestone-and gritty limestone.
Schoharie Formation | The entire Schoharie Formation is excellently exposed at the falls in the gorge of Catskill Creek. The strata are nearly vertical to overturned.
Saugerties Member:
1.6' | Interbedded light-grey weathering limestone and yellowish-brown weathering muddy limestone; proportion of less pure limestone beds decreases upward; purer limestone beds are continuous layers except for a few layers of limestone nodules in lower part; grades up into Onondaga Limestone.
Aquetuck Member:
40' | Yellowish-brown weathering dark gray, calcareous mudstone, becoming sandy and glauconitic in uppermost 3 feet; interbedded light weathering muddy limestone beds not sharply set off from the mudstone; abundant indistinct layers of dark weathering rock and layers of small chert nodules.
Carlisle Center Member:
13' | Yellowish-brown and yellowish-gray weathering dark gray calcareous mudstone with interbedded lighter weathering slightly limier layers; glauconite and quartz sand, both in upper part and lower part, but not in middle; "black bed" (p. 11 ), 3 feet thick, 5 feet from base. Abrupt contact with underlying Esopus Formation.

STOP 3, New York Central Railroad Cut, Kingston
Cut on the N.Y.C. (West Shore) Railroad, just north of West O'Reilly Street, Kingston West 7.5' quadrangle, Rosendale 15' quadrangle.
Cuts on both sides of the track a few hundred feet north along the track. Contacts between members of the Schoharie are marked with white X's on both sides of the track. The top and bottom of the black bed in the Carlisle Center Member are shown by paint marks along the bedding.
LISTEN FOR TRAINS - they come by often.
The entire Schoharie Formation is excellently exposed in a small syncline beneath the Edgecliff Member of the Onondaga Limestone.
The section is as follows:
Saugerties Member:
30' | Interbedded light-gray weathering limestone and yellowish-brown weathering muddy limestone; prominent banding shown on surfaces of cut; possible to recognize several subunits.
Aquetuck Member:
44' | Yellowish-brown and yellowish-gray weathering very calcareous mudstone or very muddy limestone; interbedded layers of light-gray weathering limestone nodules; a few continuous limestone layers; thin inconspicuous dark-weathering layers in the calcareous mudstone.
Carlisle Center Member:
143' | Yellowish-brown and yellowish-gray weathering calcareous mudstone; interbedded limier layers, becoming more distinct and more calcareous upward; prominent burrows in upper two-thirds; Taonurus in lower part; "black bed" 55 feet above base; basal bed of sandy glauconitic calcareous mudstone less cleaved than above, truncates dark gray non-calcareous mudstone of Esopus Formation.

Lunch STOP.
The Ulster County quarry (Stop No.4) borders Forsyth Park on the north. The Schoharie-Onondaga contact is located along Lucas Ave near the Park entrance and the outcrops within the Park give a section through the Edgecliff and Nedrow Members.

STOP 4. Ulster County Highway Department Quarry, Kingston
Quarry southwest of Route 209 on west side of Kingston, 0.2 mile WSW of Route 209-28 intersection. Kingston West 7.5' quadrangle, Rosendale 15' quadrangle.
This is an excellent exposure of the Nedrow and Moorehouse Members with good (and typical) fossil collecting in both units. The beds are flat lying and fossils are best observed on the extensive flat surfaces in, and at the top of, the quarry.
The section is as follows:
Moorehouse Member (upper part not exposed):
24' | Middle unit; lithology as at Leeds; brachiopods, gyroconic cephalopods and small horn corals are common; trilobites and sponges ("Hindia" sp.) are also present. .
7' | Lower unit; lithology as at Leeds; fossils are common but hard to collect in quarry face.
Nedrow Member (lower part not exposed):
8' | Moderately coarse and light-colored limestone with medium-light- gray chert; platyceratid gastropods, brachiopods, bryozoans, corals, "Hindia" sp.

STOP 5. Abandoned Quarry in Wawarsing
Small quarry north of Route 209, 0.5 mile northeast of Vernooy Kill Road, Kerhonkson 7.5' quadrangle, Slide Mountain 15' quadrangle.
Between Kingston and Wawarsing the lower part of the Onondaga becomes darker and finer grained. The characteristic Nedrow platyceratids are not present and the member cannot be recognized. The Edgecliff is marked by characteristic large crinoid columnals but is otherwise hard to distinguish from the superjacent Moorehouse Member.
The section is as follows:
Moorehouse Member (upper part not exposed):
29' | Medium-dark-gray limestone in beds 2 to 10 inches thick, some shaly beds in upper part; trilobite fragments; 2-inch chert bed at base.
20.5' | Limestone similar to above; Levenia lenticularis, brachiopod fragments and apparent juveniles are common; trilobite fragments, gyroconic cephalopod, small horn corals.
Edgecliff Member:
13' | Medium-gray, medium-fine-grained limestone with scattered chert nodules in the lower-middle part; large crinoid columnals and small horn corals are common; brachiopods and bryozoans are also present.
Transition to Schoharie Formation:
2-3' | Brown-weathering silicous limestone forms the lowest beds in the quarry.

STOP 6. Trilobite Mountain
On northwest facing hill between two roads and the Erie R.R. near Port Jervis Golf Club, 1.1 miles northeast of Tristates, Port Jervis South 7.5' quadrangle, Port Jervis 15' quadrangle.
Cuts along both sides of road.
Only the lower few feet of the Edgecliff Member are exposed here on the northwest side of the hill, facing the Country Club. The beds are lithologically and faunally similar to the Wawarsing exposures and to the Stroudsburg outcrops farther south. Corals, brachiopods, and the large crinoid columnals are fairly common and make up most of the fauna. The Schoharie Formation is exposed between the Edgecliff face and the Erie railroad tracks. There are a few large unexposed intervals. Thicknesses, based on dip and slope measurements, are approximate.
8' | Unexposed up to the Onondaga Limestone.
Saugerties or Aquetuck Member:
25' | Yellowish-gray and yellowish-brown weathering muddy limestone containing vague layers of nodules of purer limestone.
21' | Unexposed (concealed by road).
Carlisle Center Member:
12' | exposed
25' | unexposed
24' | exposed | Olive-gray weathering dark gray calcareous mudstone; interbedded lighter weathering limier layers; a few distinct limestone beds in upper part; traces of burrows (p. ll)
70' | unexposed
41' | exposed
30' | Concealed by railroad tracks down to dark gray mudstone of Esopus Formation.

STOP 7. Tristates Point
(Not visited on the 1962 trip, but in the Guidebook.) Delaware River shore near Tristates Point in Laurel Grove Cemetery just west of Tristates, Port Jervis South 7.5' quadrangle, Port Jervis 15' quadrangle. An estimated 25 feet of dark-gray limestone is exposed on the west side of the cemetery. The rock is part of the Moorehouse Member but its exact stratigraphic position is unknown. Corals, small gastropods, and trilobite fragments are fairly common.

B: GEOLOGY OF THE PRECAMBRIAN CRYSTALLINE ROCKS, CAMBRO-ORDOVICIAN SEDIMENTS, AND DIKES OF THE SOUTHERN PART OF THE MONROE QUADRANGLE
By H. W. Jaffe and E. B. Jaffe The area covered by this trip lies in the southern part of the Monroe 7.5' quadrangle, and consists chiefly of Precambrian crystalline rocks of the Hudson Highlands. The crystalline prong is thrust at a high angle to the west over Ordovician and Devonian sediments of the northern extension of the Green Pond syncline. The fault trough is filled with lakes and glacial deposits. To the east, a high-angle fault running roughly parallel to Route 17 and continued through Tuxedo Lake to the south separates the block from the main body of the Ramapo Mountains., A small inlier of Wappinger dolomite, possible downthrown, extends nearly a mile into this fault trough, which also is covered by glacial deposits. The northern end of the block is unconformably overlain by Poughquag quartzite(Lower Cambrian) succeeded by Wappinger dolomite (Cambro-Ordovician); both dipping gently off and roughly paralleling the present outcrop pattern of the crystalline rocks. This may represent original sedimentary onlap with subsequent gentle warping during uplift of the crystalline block. This northern contact of the crystallines, and also some probable fault zones within the crystalline block, are obscured by glacial deposits which form a school of drumlins and drumlinoid hills, trending north to northwest across the regional strike of the crystallines and indicating glacial movement to the southeast. This is further corroborated by the thick glacial deposits on the east side of the northeast-southwest valleys. Within the crystalline block, strikes and dips of the foliated gneisses indicate a series of folds trending about N 50°E and plunging very gently to the north, with some local warping indicated by south plunges. A generalized cross-section normal to the foliation might show: 1) a steep syncline overturned to the west in the easternmost belt of hornblende granite gneiss; 2) an isoclinally-folded recumbent anticline, possibly thrust to the west, in the belt east of Lake Mombasha; 3) a steep syncline, again overturned to the west, with an axis just west of the west shore of Lake Mombasha; and 4) a steep isoclinal anticline along the last ridge at the west of the block. This generalized picture is very difficult to corroborate in detail because of the complexity of the folding, the large amounts of glacial fill at crucial contacts, and the considerable amounts of faulting. At least two series of faults may be recognized in addition to the aforementioned border faults to the east and west. The oldest group (not shown on the map), trending roughly N-S at a small angle to the foliation and dipping steeply, can be recognized by the small steep trenches they form, and at times by considerable silicification and skarn formation along their trend. They may have influenced the location of the frequent small magnetite deposits. This older series is offset by a set of high angle gravity faults roughly normal to the foliation. Field and petrographic evidence indicates that these may be hinge or pivot faults, with the greatest displacement to the west. Vertical or steeply dipping transverse joints strike northwest, and several of these are filled with melano and leucophyr dikes, which also cut the Poughquag quartzite and Wappinger dolomite. A subordinate set of joints strikes northeast parallel to the gneissic foliation. A description of the rock types is given in the detailed itinerary which follows. Speaking very broadly, a series of calcareous and siliceous sediments and basic volcanics of the flysch facies were folded in a eugeosyncline and wholly recrystallized with attendant modification by granitic fluids. Were these liquids derived by magmatic fractionation from a basaltic substratum, or by fractional melting of sediments in place, say 10-20 km down? Evidence for temperatures high enough to melt granitic rocks is found throughout the minerals of the crystalline block. For example, microperthites were probably homogeneous at temperatures above 640°C below which they unmix. Further, the oxygen isotope thermometer gives a temperature range of 320-550°C for staurolite zone minerals and at least a part of this area is in the higher grade sillimanite zone. Almost all of the granitic rocks show concordant relations with the paragneisses. This leaves syntectonic magmatic intrusion or in-place fractional melting as the two most probable means of deriving the granitic rocks and migmatites. In either case, the granitic rocks would have passed through a magmatic stage. The persistence of shredded and partially ingested metasedimentary remnants in most of the granitic-quartz dioritic gneisses of the area would tend to favor an in-place fractional melting hypothesis. The age of the granitic rocks and associated gneisses is believed to be about 1100 million years, based upon the best evidence from radioactive dating. Pb/U isotope ages on zircon from the Storm King granite are essentially concordant at 1100 M. Y. [discordant Pb/U ages on uraninite and monazite in the Highlands, A/K ages on mica, and Pb/α ages on zircon range from 620-900 M.Y. A recent Pb/α age of 770 M.Y. was obtained on zircon from granite interlayered with amphibolite near the Suffern entrance to the N.Y. Thruway. All of the ages below 1100 M.Y. do not necessarily date a true recrystallization. For example, a metamorphism 300 M.Y. ago might cause, 1100 M.Y old zircon to lose enough of its lead to give an age of about 770 M.Y. The absence of any ages of 200 to 400 M.Y. on minerals from the Highlands, however, indicates that the Precambrian .... rocks were not completely recrystallized during the Acadian or Appalachian orogenies.

B: GEOLOGY OF THE PRECAMBRIAN CRYSTALLINE ROCKS, CAMBRO-ORDOVICIAN SEDIMENTS, AND DIKES OF THE SOUTHERN PART OF THE MONROE QUADRANGLE

Wappinger dolomite and drumlin
At 2.0 miles observe gently dipping Wappinger dolomite outcropping in field on west side of Orange Turnpike, and large drumlin directly ahead to the, southeast.

STOP 1.
Walk 0.16 miles due west over hilltop to edge of cliff formed by 10' section of Poughquag formation (Lower Cambrian). The section consists of alternating 2" to 2' thick beds of ferruginous quartzite, conglomerate, and arkose, striking N 50°W and dipping 8°NE. Return to top of ridge and note 5.5' basic dike intrusive into Poughquag quartzite. Continuing east along hilltop note small outcrops of Poughquag quartzite and Wappinger dolomite on eath side of concealed contact. Continuing east, stop at 10' thick basic dike on northeast edge of hill. The dike strikes N 18° W and is essentially vertical; it shows flow layering parallel to the strike, and chilled borders. The modal composition of this dike is:
| 1 | 2
dark red-brown alkalic hornblende | 46.5 | 37.0
augite-pigeonite | 6.0 | 13.1
chlorite | 8.4 | 9.0
prehnite | 0.2 | --
calcite | 0.3 | --
(calculated SiO2 content: 44-46%)
The texture is seriate-porphyritic with hornblende and augite forming the phenocrysts, which lie in a groundmass of albite laths.
This rock is a melanophyr, here defined as a dark, dense, fine-grained, porphyritic dike in which only the mafic minerals form phenocrysts. The abundance of the alkali-rich red-brown hornblende and the low calculated silica content indicate that this dike is compositionally related to the understurated alkalic rocks (camptonite lamprophyre of Johanssen). It is not a diabase or a "basaltic dike" but a true alkalic rock. This dike and two others in the area intrude the Wappinger dolomite and are here considered to be of post-Orodivian age. Similar dikes are found in the Adirondacks in close association with true diabases and in the Champlain Valley without the accompanying diabases. The Champlain Valley dikes are clearly post-Ordovician with the upper age-limit unknown. The melanophyr dikes in the southern and central part of the Monroe quadrangle are numerous; they intrude the crystalline rocks and Cambro-Ordovician Poughquag-Wappinger series; but none have yet been found cutting the immediately adjoining thick section of Devonian sediments in the same small quadrangle. This would suggest that the dikes are older than the Triassic diabase sequence. Further evidence suggesting a pre-Triassic age is the presence of garnet and abundant epidote presumably formed during a pre-Triassic orogeny. Inasmuch as albite should not be expected in a rock containing 75% of mafic minerals, the epidote may be assumed to have unmixed from an originally more calcic plagioclase during a regional metamorphism. In thin-section most of the epidote is included in the albite laths. Return east to the road and observe outcrop of blue-gray Poughquag arkose or feldspathic quartzite. This rock consists of 1-3 mm subrounded strained detrital quartz, microcline-microperthite, and minor oligoclase in a finer-grained quartzo-feldspathic-clay-sericite-"limonite" matrix. The principal cement is authigenic quartz overgrown in optical continuity on detrital quartz. The absence of rock fragments and the low interstitial paste content indicates that the rock is not a graywacke. Minor amounts of zircon, sphene, brown tourmaline, anatase, and opaques are present. The abundance of microcline microperthite and quartz suggests that the rock was derived from the adjoining Precambrian granitic gneisses.

STOP 2.
Leaving Stop 1, the Orange Turnpike turns southwest and crosses the concealed unconformable Cambrian-Precambrian contact. Beyond the Lipalian interval, the first Precambrian rock encountered is a fine-grained pink alaskite with no more than 1% of dark minerals. It is composed mainly of 1-3 mm microcline microperthite, microcline, and quartz, with much less sericitized albite-oligoclase and an occasional flake of biotite or chlorite. Within 100' to the south, the pink alaskite grades through a narrow zone of coarse biotite microperthite oligoclase granite and granodiorite into a medium-grained, gray, essentially massive quartz diorite gneiss which forms the bulk of the southern outcrop at this stop. The quartz diorite gneiss (quartz oligoclase gneiss of other workers) consists of oligoclase antiperthite about 70%, quartz about 25% and hypersthene, biotite, magnetite, chlorite about 5%. In thin-section, quartz is not uniformly distributed and forms long tongues which embay adjoining oligoclase grains. Oligoclase is well-twinned and antiperthitic. On top of the outcrop, observe several tongues of biotite hornblende hypersthene labradorite (An55) pyribolite infolded in the quartz diorite gneiss. Foliation measured on the pyribolite is N35° -50°E, dip is essentially vertical. Slickensided joint faces strike N 24°W and N 65°W. About 0.3 miles south (not a scheduled stop) the quartz diorite gneiss darkens in color, the quartz content drops and the rock grades to an augite diorite gneiss with abundant interlayered hornblende hypersthene oligoclase-andesine pyribolite. Where quartz becomes locally abundant, it embays and replaces both plagioclase and the ferromagnesian minerals.
The quartz diorite gneiss is thus formed from the reconstitution of pyribolite accompanied by the introduction of silica and small amounts of potash. These constituents could logically be derived from granitic liquids formed from the fractional melting of sediments.

STOP 3.
Turn east on Harriman Heights Road. A fresh road-cut exposes a dark gray and pink banded migmatite. The gray rock is a calcarious siliceous paragneiss composed of quartz, microcline, bytownite (An80, nγ = 1.575), augite, epidote, dark brown sphene, zircon, apatite, and magnetite. The pink bands consist mainly of quartz and microcline or microcline microperthite. Other samples of this migmatite carry anorthite with An95 (nα = 1.574, nε = 1.581 nγ = 1.585, 2V-≡ 75° , opt. -). This migmatite carries abundant epidote produced by a retrograde metamorphic alteration of anorthite and augite.

Return west to Orange Turnpike and turn south, parking at Monroe Town Line sign. The prominent road-cut on the east side of the road is gray and pink banded biotite migmatite. The dark gray rock is a siliceous, calcareous paragneiss composed of quartz, labradorite (An50), biotite, microcline, hornblonde, epidote, apatite, zircon, augite, and ilmenite. The pink bands consist wholly of quartz and microcline, the latter occasionally microperthitic. These kalialaskite bands are believed to be formed from low-temperature metasomatic introduction of quartz and microcline. In-place melting would require an appreciable amount of albite, which is not present. Asthe microcline is only occasionally microperthitic, it is doubtful that it could hold much soda in solid solution. The foliation strikes N 24°E and dips 45°SE; fold axes plunge gently NE.
The outcrop on the west side of the road, just south of the Town Line, is the same rock. Here the foliation strikes N 22 E, dips only 12°SE and fold axes plunge 5°NE. The gentle dip is due to isoclinal folding overturned to the west.

Continue south on Orange Turnpike to top of hill with prominent overhanging cliff to the east aide of the road. The cliff is made up of a silicified epidotized migmatite with some coarse recrystallized hornblendes in the granitic component. The outcrop is strongly warped, part of it showing recumbent isoclinal folding overturned west, part of it showing fairly steep dips east. The undersides of overhanging bedding planes are commonly slickensided and silicified. Both this outcrop and the one immediately preceding it suggest an old period of thrusting to the west.

Continue south to the junction with the second of two roads entering from the west. Outcrop on the west side of the road shows a 20-25' hornblende albite melanophyr (spessartite) dike which strikes N 38°W, dips 86°NE, and cuts across the foliation of the granite gneiss which strikes N 55-75°E and dips 80°SE. The dike shows normal green hornblende phenocrysts up to 0.25" lying in a matrix of albite laths, 0.2 x 0.4 mm. The modal composition of the dike is:
albite | 53.3
hornblende | 21.5
epidote | 12.6
chlorite | 7.3
apatite | 0.1
opaque | 3.2
quartz | 1.2
calcite | .4
K-spar | .4
| 100%
(calculated SiO2 content = 53.5%)
The granite gneiss contains occasional schlieren of biotite-rich gneiss.

The road parallels the contact of granite gneiss (east) and pyribolite (west). At 8.4 miles the road crosses this contact. Stop 7 shows a 16' thick granodiorite leucophyr dike which strikes N 48°W, cross-cutting the foliation of the surrounding amphibolite which strikes N 57°E and dips 20° SE. Note large wedge of amphibolite in center of dike and occasional pink potash-feldspar-quartz bands in the amphibolite. This dike is unique in this quadrangle and perhaps in the Highlands. It is composed of sparse phenocrysts of oligoclase, quartz, less microcline, and rare biotite, lying in a matrix which is again porphyritic on a microscopic scale. The second generation of micro-phenocrysts is made up of square to rhombic zoned potash feldspar and laths of albite-oligoclase. These lie in a very fine granophyric groundmass made up of feldspar, quartz, mica, chlorite, and "limonite." The "limonite" forms megascopic crenulated black streaks which give the dike a flow layering in places. A mode was not obtained because of the fine-grained nature of the groundmass. X-ray data on a powdered sample indicate that oligoclase >quartz > microcline, hence the dike is of granodioritic composition. East of the road the dike is not found, and may be cut off by a north-south fault; if this is so the dike is very old. An outcrop of the same type of rock was found 0.25 miles to the west cutting migmatite: this may be an extension of the same dike.

Continue north on East Mombasha Road stopping at steep cliff on east side of road. This is a fine-banded dark gray and pink biotite migmatitic paragneiss, the fine-bedded analogue of stop 4. The dark gneiss bands here are more altered and are marked by the appearance of muscovite and epidote replacing biotite and plagioclase. A small amount of rutile is formed from the titanium present in biotite. Occasional large pods of pink alaskite are concordantly interleaved in the migmatite. The foliation strikes N 37°E and dips 20°SE.

STOP 8A.
Continue north on East Mombasha Road stopping at the sillimanite-bearing outcrop just north of number 8A on the map. This is a tightly folded, crenulated biotitic. paragneiss in the sillimanite zone of metamorphism. It is composed of thin bands of a gray biotite microcline labradorite quartz paragneiss interlayered with orthoclase cryptoperthite (anorthoclase) quartz bands. Abundant garnet (almandite-pyrope), dark blue-green tourmaline, and minor prismatic sillimanite are developed at the interfaces of the biotitic and alaskitic layers. The biotite is pleochroic from "paprika-red" to almost colorless and is an iron-rich variety. Sillimanite and tourmaline lie in the foliation planes with their long axes parallel to the fold axes. The fine paragneiss bands have an average grain size of 0.3 mm, the coarse alaskitic bands, up to 10 mm.

Continue north on East Mombasha Road to sharp bend north after short jog east. Outcrop on east side of road contains abundant garnet in biotite migmatitic paragneiss. Outcrop to the west in an open field, near swamp, shows a biotite migmatitic paragneiss and pyribolite intimately folded in medium to coarse massive alaskite. The alaskite forms the core of a fold plunging north and the outcrop may be a small anticline overturned to the west. Here chloritized amphibolite pods are completely enclosed in alaskite. A thin section of the dark gneissic rock showed completely fresh hypersthene: (normally an unstable mineral) and biotite associated with completely scapolitized plagioclase, and quartz. Garnet occurs sparingly. To the west the rocks grade rapidly to almost pure alaskite. This is the northernmost outcrop of garnet migmatite.

Continue northeast on East Mombasha Road to bottom of hill at rough track to the west. On the east side of the road is an outcrop of coarse, gneissic, partly recrystallized amphibolite. It contains plagioclase ranging from andesine to bytownite with abundant hypersthene, brown and green hornblende, and less biotite, the composition varying with layering. To the east in the woods (not visited) the plagioclase is all scapolitized, the hypersthene serpentinized, and a pale blue-green hastingsite or edenite amphibole is developed near the contact with the alaskite of stop 2. On the west side of the road, about 60' in the woods, a thin layer of foliated green hypersthene quartz oligoclase gneiss (quartz diorite gneiss) is in sharp contact with fine-grained pink alaskite. This may be a fault contact. Boulders of Poughquag conglomerate, and a melanophyr dike (camptonite), parallel the contact zone.

Note NW-trending drumlins to the west.

Continue NE to Orange Turnpike, then NW past stop 1 to Rye Hill Road. Turn sharply SW, noting NW-trending drumlins to the west. Stop 11 is the first outcrop beyond the glacial fill on the east side of the road, which now is called Berry Road. The outcrop contains abundant layers and schlieren of biotite two-feldspar quartz paragneiss in coarse pink granodiorite and granite with abundant antiperthite, microperthite, and oligoclase. A swarm of eight or ten small melanophyr (camptonite) dikes, up to 2' thick, fill a tension fracture pattern striking N 8 W to N 48°W. The foliation of the host granitic rock strikes N 52°E, and dips 50-60°SE. To the west, in the woods; the biotitic paragneiss is resorbed by massive biotite granite-granodiorite. Occasional samples are of quartz syenite composition.
It is worth noting here that melting of biotite would yield an additional large amount of potash feldspar and magnetite:
KFe2AlSi3O10(OH)2 --> KAlSi3O8 + Fe3O4
biotite ---- > K-feldspar + magnetite
This would sweeten the granitic liquid and perhaps explain the frequent occurrence of potash-feldspar pegmatites in association with the many small magnetite deposits of the area. It should further be noted that many of the alaskites in the quadrangle contain magnetite as the only accessory mineral of consequence.

Continue SW on Berry Road, noting alternation of folded dark gneiss and pink granite-granodiorite; turn NW on West Mombasha Road, then NE on Cedar Cliff Road to stop 12, about 200' beyond farmhouse. Outcrop on east side of road shows fine-grained narrow bands of folded pyribolite (here amphibolite) overturned slightly to the west and being replaced by coarse massive buff-gray granodiorite. The granodiorite cuts across the folded amphibolite and contains schlieren of the latter which retain their original attitude in the folds. The infolded amphibolite contains brown hornblende, albite-oligoclase, microperthite (introduced), biotite, magnetite, and apatite. The granodiorite is composed of albite-oligoclase, quartz, less microcline microperthite, biotite, hornblende, zircon, and some fragments of altered hornblende, plagioclase, and calcite. Pyribolite layers are very abundant in this zone but are not continuous, the widest observed being 80' thick near the old magnetite mine on Mine Road. Westward the rocks grade to contaminated gneisses and then alaskite, which forms the western edge of the crystalline block.

C: THE STRUCTURE AND STRATIGRAPHY OF THE PORT JERVIS SOUTH-OTISVILLE QUADRANGLES
Co-authors:
Sidney Fink, Dept. of Geology, Brooklyn College
C. J. Schuberth, The American Museum of Natural History
The area of this field trip, Port Jervis South-Otisville Quadrangles, (Fig. 1) includes parts of the Folded Appalachian Mountain, Great Valley and the Appalachian Plateau geomorphic provinces. The Paleozoic formations, deposited originally as horizontal sediments in an extensive geosyncline, have in this area an aggregate thickness in excess of 5,000' and consist of the following units, in ascending order: Martinsburg Graywacke Shale and Sandstone (Middle (?) and Upper Ordovician), Shawangunk Conglomerate (Lower to Middle Silurian), High Falls Red Beds (Middle to Upper Silurian), Poxono Island Shale, Bossardville Limestone and Keyser Group (Upper Silurian), Helderberg and Oriskany Groups, Esopus Shale and Onondaga Limestone (Lower Devonian), and the Hamilton Group (Middle Devonian). Quaternary glacial drift and till occurs throughout the area (Pl. 1).

C: THE STRUCTURE AND STRATIGRAPHY OF THE PORT JERVIS SOUTH-OTISVILLE QUADRANGLES

Roadcut through kame (at sharp turn).

Esopus Fm.
Outcrop of Esopus Formation (along right side of road); well-developed southeast slaty cleavage.

Base of Appalachian Front on left (NW)
Traveling along base of Appalachian Front on left (NW). The lowland is underlain by the Onondaga Limestone which is hidden by a cover of till.

Helderberg Ridge
Helderberg Ridge (lower Devonian) on right (SE); dip-slope of Kittatinny (Shawangunk) Mountain farther east.

Marcellus Shale
Marcellus Shale dipping gently NW (into Appalachian Front) at left (NW). Overlying these black fossiliferous shales are the olive-gray graywacke shales and sandstones of the Hamilton. group. These represent the sediments derived from source areas to the east at the onset of the Acadian Orogeny.

Unsorted and unstratified glacial till

Crossing Neversink Valley covered with glacial till

Entering Helderberg Ridge

STOP 1. Esopus Formation.
The rocks exposed along the road are the black shales of the Esopus Formation. This formation is characterized by its well-developed southeast dipping slaty cleavage. The normal north-west dip of these lower Devonian beds is obscured due to the cleavage. The Esopus is the most important formation in the ridge west of Shawangunk Mountain (Pl. 5, Fig. 1). At the crest of this ridge is the Glenerie Cherty Limestone. The Glenerie is a limestone facie of the Oriskany Sandstone. In the valley between this ridge and Shawangunk Mountain to the east is found the limestones of the Helderberg Group (Pl. 5, Fig. 2).

STOP 2. Martinsurg / Shawangunk contact
Unconformable contact between Martinsburg Shale and Shawanqunk Conglomerate (walk approx. 300 feet east along railroad tracks).
In this railroad cut is exposed an angular unconformity between the Martinsburg and Shawangunk Formations. The Martinsburg dips 37°NW and the overlying Shawangunk dips 28°NW. The Martinsburg is made of interbedded graywacke shales and sandstones. The Shawangunk is a massive quartz sandstone with a 40-50 foot basal quartz conglomerate. The high percentage of quartz, the well rounded grains, the high index of sorting, and the great thickness, all characterize a beach deposit developed over a long period of time. In an old quarry above the road, Schuchert (1916) found Eurypterids in the shale beds found within the Shawangunk. In places the Shawangunk is cut by quartz-filled veins that are mineralized with pyrite, chalcopyrite, galena and sphalerite. These veins near Guymard (3.5 miles southwest of this locality) were the site of a small lead-zinc industry approximately 75 years ago.

STOP 3: Small quarry in New Scotland Formation.
The beds exposed in this cut are those of the Lower Devonian New Scotland Formation. Most of the formation consists of dark blue black shaly limestones. Toward the base of the formation abundant chert is found. The chert layers represent the Kalkberg Member of the New Scotland. The non-cherty beds are characterized by the following fauna:
Spirifer maclopleura
Leptaena rhomboidalis

STOP 4. Recumbent fold in Martinsburg
Recumbent fold in Martinsburg (east side of Erie Railroad tunnel) - walk approx. 500 feet along railroad track.
On the north side of the track, the Martinsburg has been folded into a recumbent fold. In the same locality other signs of deformation are seen, (1) overturned beds, (2)small scale fault east of the recumbent fold. Although folding and faulting are seen in the area, metamorphism of the shales is not evident. It is interesting to note that the Shawangunk-Martinsburg contact is found near the crest of Shawangunk Mountain and not near the base. This is due to the predominance of sandstone beds that are quite massive in the upper part of the Martinsburg. The valley east of Shawangunk Mountain is part of the Great Valley and is underlain in this area by the Martinsburg Formation.

Martinsburg on right (W).

Exposure of Martinsburg on right (W).

STOP 5. Martinsburg Formation.
Cyclic repetition of graywacke sandstone (with some layers becoming quite heavily bedded) and black, fissile shale characterizes the lithology of the upper portion of the Martinsburg, the oldest formation in this area (Upper Ordovician). Massive graywacke, several feet in thickness, quite prevalent near the top of the Martinsburg section (striking northeast and dipping on the average of 30 northwest), partially supports Kittatinny Mountain. The contact between this formation and the overlying Shawangunk Conglomerate, nowhere exposed in this area, lies just below the topographic crest of this ridge. Irregularities in sedimentation (seen readily in other exposures along the strike) are represented by irregularly-shaped fragments of shale within the massive graywacke layers. These isolated pieces are lenticular and the subjacent beds show no gaps, into which they might fit. Other fragments are concave and sharply angular at their ends and appear torn from their position by slight tectonic movements. Undoubtedly, irregularities in primary sedimentation or slumping or other settling movements, incidental to primary deposition but taking place after sufficient hardening of the deformed layers, permitted them to act as competent units. Van Houten (1954) proposed that Martinsburg mud accumulated slowly in a marine environment. Sand, periodically stirred up in the shallow sea was carried to deeper water environments by spasmodic turbidity currents, and as the velocity decreased, the unsorted sediments settled in graded' beds (not a prominent feature in the sandstone because no great range in grain size is involved in vertical sorting). These deposits may represent a "poured in" type of sediment, derived from the rapid erosion of tectonic source areas.

STOP 6: Exposure of Shawangunk Conglomerate.
This is near the nose of a doubly plunging syncline of this formation. (See Pl. 6 and accompanying discussion.)
Lake Marcia on left (W) underlain by strongly sheared Martinsburg Shale. The "scenic drive" parallels the strike of the western limb of the syncline; dips range from, 30° to 70° southeast.

STOP 7. Highest elevation in New Jersey. 1,803 feet a.s.l.
This is the highest point in New Jersey. We are still on the western limb of the plunging syncline. Note the steep south-east dips (60°SE). Lake Marcia is located in the Martinsburg Shale as a result of breaching of the anticline immediately to the west and erosion along a thrust fault. The anticlinal, unbreached structure continues southwest (southwest of the A.T.&T. tower) until it ultimately dies out (in the southwestern portion of the Port Jervis South Quadrangle). All structures are doubly plunging. Toward the west lies the Pocono Plateau and along the east, the Great Valley underlain by the Martinsburg Formation.

D: STRATIGRAPHY AND STRUCTURE OF THE "CATSKILL GROUP" IN SOUTHEASTERN NEW YORK
Frank W. Fletcher
The University of Rochester
"A blackboard drawing or a textbook illustration of a sedimentary facies has quite a different appearance from a sedimentary facies when one encounters it in the field. In the field, facies changes seem baffling and bewildering, especially in an area of new and unknown stratigraphy. It is as if stratigraphy, hitherto subject to natural laws and capable of rational analysis, had suddenly gone lawless and planless." P. B. King
THE CATSKILL PROBLEM
Within the Devonian rocks of southeastern New York there are approximately 5000 feet of interbedded red and gray sandstones, shales and conglomerates known collectively as "Catskill." After more than a century of investigation, virtually the only conclusions agreed upon by the various workers in the area are that the facies changes are complex, the location of formation boundaries is difficult, few fossils are present, correlation is uncertain, and the sedimentary environment is either subaerial or subaqueous.

D: STRATIGRAPHY AND STRUCTURE OF THE "CATSKILL GROUP" IN SOUTHEASTERN NEW YORK

Point Peter, Port Jervis, N. Y.
Outcrop of dark gray shales and sandstones called Portage by Willard (1936) and marine Devonian beds on the Geologic Map of Pennsylvania. These rocks contain many of the same fauna as the Mount Marion Formation along the Catskill Front.

Hawks Nest formation
Beginning of outcrop which shows the type section of the Hawks Nest Formation.

STOP 1. Type section of Hawks Nest Formation.
The name "Delaware River Flags" was first applied by I.C. White in 1882 to the rocks which overlie the marine Hamilton (?) beds just north of Port Jervis, New York. He reported a thickness of approximately 1400 feet. Willard(1936) redefined the formation as 1500 feet of greenish flags without red beds. He states that the formation is correlative with the Onteora Formation of the Catskill front. However, he fails to give an adequate reason for the disappearance of almost 3000 feet of red strata (the combined thickness of the Onteora and pre-Onteora red beds) which is necessary to support such a correlation. Examination of rock samples from exploratory oil and gas wells in the area has shown that a thick sequence of red strata occurs in the upper 700 feet of Willard's Delaware River Flags. This sequence of red beds can be traced, in a series of wells, north along the Delaware River and into the region of Oneonta, New York, where it is called the Oneonta Formation. This has prompted Fletcher to discard the name Delaware River Flags. The section of gray sandstones and shales which, in southeastern New York, lie beneath the Oneonta Formation, are defined as the Hawks Nest Formation after the excellent exposures on the high cliffs at Hawks Nest, N.Y. This 800 foot sequence of strata is probably correlative with the Unadilla Sandstone of the Oneonta region. The dominant lithology is a fine- to medium-grained, light to medium bluish gray subgraywacke. The fine-grained sandstones are finely laminated and flow rolls are common. The medium-grained sandstones exhibit low angle cross-bedding. A limonite stain is present on the weathered rock surface. Interbedded with the sandstones are medium dark gray to grayish blue siltstones which are brownish gray on weathered surface and lack fissility. The formation is generally unfossiliferous.

3.1 miles from Point Eddy bridge
4.56 miles between Point Eddy bridge and Mongaup bridge

Outcrop at left along the river.
Outcrop at left along the river. A clear expression of the regional dip, cross-bedding, and joint pattern.

Large quarry at the right.

STOP 2. Outcrop of the Oneonta Formation.
In the same report in which Mather defined the Catskill Mountain Group, L. Vanuxem (1840) proposed the name "Montrose sandstone or sandstone of Oneonta" for the red and gray rocks found in Otega, Broome and Chenango counties, New York. The Geologic Map of New York shows these 700 feet of strata correlated with the Onteora Formation. Fletcher, however, has suggested an alternative correlation (see Plate IV). Stratigraphic columns constructed from samples from gas wells located in the northeastern Catskill Mountains show that only the lower 800 feet of Chadwick's Kiskatom red beds "drop out" before they reach'the type section of the Oneonta Formation. Beneath the Twilight Park Conglomerate is a 900- foot zone of predominantly red strata, 250 feet of dark gray shale and sandstone with two thin beds of coarse-grained, white quartzose sandstone,and about 800 feet of intercalated red and dark bluish gray sandstone and shale. The 250 feet of rock containing the two thin white sandstone beds forms a distinctive and persistent marker horizon in subsurface samples. This zone has been traced to the Durham quadrangle where it was called by G.A. Cooper (1934) the eastern equivalent of the Portland Point Member of the Moscow Formation. In the Durham quadrangle the zone is underlain by 350 feet of red beds. In the Margaretville quadrangle, west of the Catskill front, only 100 feet of red beds underlie the white sandstone units. At the type locality of the Oneonta Formation this zone is located approximately 900 feet beneath the lowest red bed. As a result of these findings the strata Chadwick called Kiskatom have been 'divided into three units. The lower red zone, which loses its red beds rapidly to the west and south, is designated the Plattekill Formation and its type section is taken as Plattekill Clove. The middle zone is called the Potter Hollow Formation after Potter Hollow, Greene County, New York. The upper red zone is the Oneonta Formation. The Oneonta contains micaceous, pale red purple and grayish purple siltstones and mudstones. The red mudstones exhibit slickensides formed by slumping of unconsolidated mud before induration. The sandstones are medium grained, red purple and light gray to greenish gray subgraywackes. They weather light greenish gray. The flaggy sandstones have primary current lineations on bedding surfaces and, with the exception of one type of freshwater (?) pelecypod and plant fragments, are unfossiliferous.

Sandstone outcrop along railroad on Pa. side of river.

Sandstone outcrop
Sandstone outcrop on right side of highway. Notice well-expressed joint sets. Red siltstone at top of hill.

Outcrop along railroad on Pa. side.

Outcrop of sandstone
Outcrop of sandstone on right side of highway. Cross-stratification is absent. Red siltstone near bottom of hill.

Red mudstone indicates regional dip
Outcrop on right. Watch for appearance of red mudstone which indicates the regional dip.

Large outcrop of the sandstone on the right.

Cross-stratification.
Outcrop showing well-developed cross-stratification.

Red siltstone and dark gray shale
Outcrop on both sides of the highway. Red siltstone and a dark gray shale are exposed.

Barryville member of the Shohola Fm.
Outcrop of the Barryville member of the Shohola Formation (see Willard, 1936). Notice the distinctive weathering "holes."

Cross ten mile river

Cross-stratification.
Sandstone outcrop at left showing well-developed cross-stratification.

Outcrop near the top of the sandstone on the right side of the highway.

Outcrop at right. Notice the abundance of red soil.

Red siltstone exposure at right.

Red siltstone with anticlinal structure
Outcrop of red siltstone and mudstone on right side of highway. Notice anticlinal structure.

STOP 3. Type locality of the Damascus Formation.
Above the Stony Clove Formation in the Delaware River region are about 400 feet of strata composed almost entirely of red sandstone, siltstone, mudstone and shale. Willard (1936) gave the name Damascus Formation to these rocks after Damascus, Pennsylvania where this sequence is well exposed. These strata were originally named "Montrose" by White (1882) who believed they were the same red beds which crop out around Montrose, Pennsylvania. Fletcher has correlated the Damascus with the basal portion of the Katsberg formation, called Lower Katsberg on the Geologic Map of New York State. At the type locality the formation lies in the center of a large syncline (see section on structure), so that along the Delaware River older beds occur both to the south and north of the outcrop of the Damascus Formation. The sandstones are fine- to medium-grained and are grayish red purple. The few interstratified greenish gray sandstones range from medium- to coarse-grained. Both red and gray sandstones exhibit cross-stratification. The red mudstones and siltstones strongly resemble the same in the two previously described red formations; however, more of the fissile red shale is found in the Damascus Formation.

Red shale and mudstone exposed on both sides of highway.

Outcrop of gray sandstone in Damascus Fm at right.

Red sandstone exposure at right.

STOP 4. Outcrop of the Lower Katsberg Formation.

E: THE FRANKLIN STERLING MINERAL AREA
by
Helen A. Biren, Brooklyn College
The area which we shall visit is a limestone region lying in the New Jersey Highlands, which is part of the Reading Prong. It extends in a northeasterly direction across the northern part of the state. The rocks are Precambrian "crystallines" with narrow belts of infolded and infaulted Paleozoic sedimentary rocks. Major' longitudinal faults slice the fold structures, so that the area has been described as 'a series of fault blocks extending from south of the Sterling Mine to Big Island, N. Y."
For many years the Franklin Limestone yielded enough zinc to make New Jersey a leading producer of this commodity. Mining has steadily decreased in thisa rea, and in 1955 the Franklin Mine was shut down permanently, so that mineral specimens are derived mainly from surface dumps and quarries. Some twenty million tons of ore were removed from Franklin before it was shut down.

STOP 1. Sterling Hill
The Lord Sterling Pits, the earliest known workings (1770) outcropped in the legs of a syncline in the Franklin Limestone, which pitches northeast at an angle of about 50° from the horizontal. Details of the structure are quite complex. About 1913 a shaft was sunk and extensive underground development started. The ore appears to have followed definite stratigraphic horizons in the folded structure, since the banding of the Franklin Limestone and the complex folding of the ore veins appear to conform. Pegmatites are not present with the ore, so fare minerals are fewer than at Franklin. Minerals reported from this area (other than the common species listed on the chart) include: Chalcophanite, McGovernite, Mooreite, and Roepperite.

STOP 2. Farber Quarry
The Farber Quarry (formerly the Bigelow Quarry) on Cork Hill road at the Franklin-Ogdensburg line is the only active quarry. In this white limestone may be found tremolite in fluorescent crystals, pyrite crystals and calcite, chrondrodite, norbergite, magnetite, dolomite, edenite, fluorite, graphite, hematite, phlogopite and scapolite.

STOP 3. Slag boulders from Franklin Furnace
Along the east side of Cork Hill Road are large, dark boulders which represent slag from the old Franklin Furnace. Many minerals are present in some of the boulders, and the "vesicles" in the slag show a variety of fillings representing secondary mineralization.

STOP 4. B. Nicol Quarry (Formerly the Fowler Quarry)
This was the largest quarry in the area, and was active at the turn of the century as a source of flue for the blast furnace.
It is requested that visitors stay clear of the buildings of the Cellate Corporation, and do not smoke in the vicinity of the buildings or drums.
Recent visits to this quarry have yielded specimens of amphibole, apatite, arsenopyrite, chondrodite, diopside, edenite, fluorite, graphlte, magnetite, phlogopite, pyrite, pyrrhotite, pyroxene, quartz, scapolite, spinel and green and brown tourmaline.

STOP 5. Furnace Quarry
This is an abandoned quarry in the white limestone which has yielded many metamorphic minerals, including arsenopyrite, edenite, fluorite, graphite, norbergite, pyrite, pyrrhotite, rose quartz, sphene, spinel and tourmaline.

STOP 6. Buckwheat Dump
In 1852 the eastern leg of the syncline was discovered, and was stripped to form the Buckwheat open cut. Much of the overburden was removed to the dump. The accompanying key lists 50 minerals which are likely to be found there. Since the town of Franklin turns the dumps over at intervals, fresh materials are exposed, so that there is a likelihood that a variety of species will be available. In the sheds at the foot of the dumps some long and short wave ultraviolet lamps will be available for determining fluorescent phenomena. Accompanying this paper is a chart describing the fluorescence of Franklin minerals, as observed and as reported in the literature. Not all samples of a given mineral will display the described fluorescence, but it is certain that Buckwheat will yield some fluorescent material.

STOP 7. Mine Replica
The mine replica is an authentic duplicate of a typical working space in the abondoned Franklin Mine, and a display of fluorescent minerals under ultra-violet light. This is an optional trip and involves a 50-cent admission charge. Since only a limited number can be accommodated at one time, arrangements for this visit will be made while the rest of the group is collecting at the vaqrious quarries.
This trip also offers a good view of the Buckwheat open cut.
2010: This is now operated as part of the Franklin Mineral Museum:
http://www.franklinmineralmuseum.com/

Geology of South-Central New York
a guidebook
with articles and field trip logs
prepared for the
Binghamton, New York
May 3-4, 1963
Donald R. Coates, Editor
HOST
Department of Geology
Harpur College
of the
State University of New York

A: UPPER DEVONIAN STRATIGRAPHY AND SEDIMENTOLOGY IN THE BINGHAMTON AREA
James E. Sorauf and Herman E. Roberson
Harpur College
No Road Log

STOP 1 Twist Run
The road cuts in Twist Run (Fig.2), expose beds of the Rhinestreet Formation. Near the top of the hill is a 7-foot interval of dark gray, fissile shale, the Dunn Hill Member of the Rhinestreet Formation. Above the Dunn Hill shales are the basal beds of the overlying Beers Hill Member of the Rhinestreet. Approximately 12 to 15 feet of strata of the Beers Hill Member are composed of siltstones, generally quite massive where fresh, but weather into thin and irregular units. The basal 4-foot unit exhibits minute crosslamination.
Below the Dunn Hill Member is the Millport Member of the Rhinestreet, comprising the largest amount of the exposed beds. It is composed of a series of units which are somewhat cyclic in nature. Ideally the unit grades from massive, very fine-grained sandstone at the base, through massive siltstones into siltstones progressively thinner bedded and more argillaceous upwards, with a thin bed of dark shale at the top. At the base of each massive unit are flow rolls. Few if any of the units show the complete range of lithologies listed above, and each unit is extremely lenticular. Thus the measured thicknesses of each bed shown on Figure 2 must be regarded as true only for the exact place of measurement. Several of the massive beds of very fine-grained sandstone can be seen pinching out laterally within the confines of the outcrop.
Faunal elements are present within the sequence, either interspersed along bedding planes within the siltstone layers, or in definite beds of coquina. Both brachiopods (orthids, productids, and spiriferids) and pelecypods are abundant at several levels. At least three thin beds of coquina are present within this sequence. At this locality, each bed is very thin; the thickest observed being less than 6 inches.
The lowest outcrops in Twist Run are still within the Millport Member, which is underlain by the basal or Moreland Member of the Rhinestreet Formation. The Moreland is a dark shale unit similar in lithology and thickness to the Dunn Hill Member seen at this locality.

STOP 2 Binghamton Brick Co. Quarry
The quarry of the Binghamton Brick Company is developed in the Millport Member of the Rhinestreet Formation. The Moreland Member is exposed at the entrance to the quarry below the level of the main floor. The quarry floor and walls, developed as a series of steps carved from the hill, are composed of beds of the Millport Member.
As in Figure 3, the Millport Member in this locality consists of a series of alternating gray to green siltstone and shale. The shale units range from 10 to 15 feet in thickness, and are generally thin-bedded and fissile, especially where weathering has occurred. Medium-bedded siltstones occur in a somewhat cyclic pattern throughout the section. In the upper part of the sequence, the siltstones are more thickly bedded, and correspondingly the cyclical pattern is not as regular.
Smooth, continuous bedding planes between shale beds and also between shale and siltstone beds predominate; there appears to be little lensing. Small-scale cross-laminations may be observed in the siltstones.
Two prominent flow roll zones may be observed. The first occurs about 100 feet above the floor of the quarry, and the next about 20 feet higher. The flow rolls of the latter unit are numerous, and range greatly in size, shape, and degree of development. Beds of coquina are seen in place and in slump in the upper part of the section.

STOP 3 Corbisello Quarry
The Corning Member of the Gardeau Formation and the overlying New Milford Formation are exposed in this quarry. The Corning Member at this localtiy is a gray, fissile shale, of which approximately 5 feet are exposed.
The New Milford Formation contains a tongue of the Catskill facies at the base. This tongue is composed of massive, interbedded, thick lenses of sandstone. Lenticular cross-lamination is present in the thick lenses. There is a thin disrupted coal seam in the middle part of this sandstone unit. Ripple marking has been preserved on the upper surface of this sandstone tongue. This is probably a fluviatile deposit deposited near the strand line of the Upper Devonian sea.
Overlying the massive sandstone is a thick sequence of shale and interbedded siltstone. These fine-grained rocks are thought to be near-shore deposits, possibly lagoonal muds. Above the unit of shale and interbedded siltstone is another sequence of massive lenses of sandstone with interbedded siltstone and shale. These beds are similar to the basal sandstone in lithology, but are extremely lenticular.
This is the only stop on this trip, or on the trip led by Woodrow and Nugent, where the Catskill non-marine facies may be observed. Several miles to the south the New Milford is entirely composed of beds belonging to the Catskill facies.

B: GEOMORPHOLOGY OF THE BINGHAMTON AREA
Donald R. Coates
54.6 miles

B: GEOMORPHOLOGY OF THE BINGHAMTON AREA

Binghamton Brick Company.
From Stop A-2 description: The quarry of the Binghamton Brick Company is developed in the Millport Member of the Rhinestreet Formation. The Moreland Member is exposed at the entrance to the quarry below the level of the main floor. The quarry floor and walls, developed as a series of steps carved from the hill, are composed of beds of the Millport Member.
As in Figure 3, the Millport Member in this locality consists of a series of alternating gray to green siltstone and shale. The shale units range from 10 to 15 feet in thickness, and are generally thin-bedded and fissile, especially where weathering has occurred. Medium-bedded siltstones occur in a somewhat cyclic pattern throughout the section. In the upper part of the sequence, the siltstones are more thickly bedded, and correspondingly the cyclical pattern is not as regular.
Smooth, continuous bedding planes between shale beds and also between shale and siltstone beds predominate; there appears to be little lensing. Small-scale cross-laminations may be observed in the siltstones.
Two prominent flow roll zones may be observed. The first occurs about 100 feet above the floor of the quarry, and the next about 20 feet higher. The flow rolls of the latter unit are numerous, and range greatly in size, shape, and degree of development. Beds of coquina are seen in place and in slump in the upper part of the section.

Phelps Creek and south side of Hillcrest.
Phelps Creek and south side of Hillcrest. Cemented gravels attest to high lime content of sediments. This kame terrace with 900' level extends along east side of road 1.5 miles

STOP 1
Valley train outwash plastered on bedrock of shale and siltstone to height of 140'. Strata are in contact between Upper Sonyea Group at the base and Lower West Falls Group (Rhinestreet Formation) on top.

Sonyea Group
Bedrock is Upper Sonyea Group. This marks site of the post-glacial Chenango River channel that was incised owing to ice and sediment blockage in old channel to the west. Northward the valley contains a wide range of outwash deposits, terrace and plain levels, and alluvial fans. The original outwash plain slopes north from 880' to more than 1,000' at Chenango Forks and has been trenched by the Chenango River and Page Brook tributaries.

Turn left
Turn left (west) into Park area. Pass over Page Brook.

Chenango Valley State Park
Chenango Valley State Park entrance. Continue straight and make counterclockwise circuit of Park.

STOP 2
Park in parking area near pavilion. Elevation of sharp ridge is 950' which is 60' above Lily Lake on the north and Chenango Lake on the south, both are kettle hole lakes. The ridge is composed of unconsolidated materials and is probably the finest example of a crevasse filling in this part of the State. The Park contains numerous kettles and plains; however, this is not kame and kettle topography. Instead the stratified materials are largely horizontally bedded (stop 3) indicating transport from the north that engulfed stagnant ice blocks.

STOP 3. Sand and gravel quarries
Sand and gravel quarries in horizontally-bedded glaciofluviatile materials. A characteristic of quarries in the Binghamton area is coarse material on top with finer material at the bottom which are commonly sands showing cross bedding and deltaic bedding. Continue north and notice many excellent kettles along route, some more than 60' deep.

STOP A-2 Binghamton Brick Co. Quarry
The quarry of the Binghamton Brick Company is developed in the Millport Member of the Rhinestreet Formation. The Moreland Member is exposed at the entrance to the quarry below the level of the main floor. The quarry floor and walls, developed as a series of steps carved from the hill, are composed of beds of the Millport Member.
As in Figure 3, the Millport Member in this locality consists of a series of alternating gray to green siltstone and shale. The shale units range from 10 to 15 feet in thickness, and are generally thin-bedded and fissile, especially where weathering has occurred. Medium-bedded siltstones occur in a somewhat cyclic pattern throughout the section. In the upper part of the sequence, the siltstones are more thickly bedded, and correspondingly the cyclical pattern is not as regular.
Smooth, continuous bedding planes between shale beds and also between shale and siltstone beds predominate; there appears to be little lensing. Small-scale cross-laminations may be observed in the siltstones.
Two prominent flow roll zones may be observed. The first occurs about 100 feet above the floor of the quarry, and the next about 20 feet higher. The flow rolls of the latter unit are numerous, and range greatly in size, shape, and degree of development. Beds of coquina are seen in place and in slump in the upper part of the section.

Tioughnioga River
Keep left, pass over Chenango River bridge to Chenango Forks and intersection with Rt. 12. This area is junction with Tioughnioga River. Excellent exposures of bedrock, till, and lacustrine beds occur 1.2-1.7 mi. upstream in Tioughnioga River. Here it is flowing in post-glacial gorge with bedrock walls. The pre-glacial channel is 2 mi. northeast and parallel to same direction and part of the old stream bed is occupied by Ockerman Brook. (Fig.4)

Post-glacial channel
Along this part of route the Chenango River flows in post-glacial channel, the older channel was east and is now filled. Stratified outwash occurs along west side of route and at high levels above the valley walls are several small 'through-valleys'. These saddles and cols are a type of wind-gap created by high-level meltwater streams when the valley was ice filled and the uplands had become ice-free.

High level saddle
Ascending a high-level saddle, 1070', one of the overflow passes.

STOP 4. Pre-glacial channel
The railroad marks the axis of the pre-glacial Chenango River channel. This area contains many quarries in outwash sand and gravel. A recently drilled well, April 1, 1963, produced 120 gpm from sand and gravel 98' below ground surface.

Terraces and till
Chenango Bridge red light. Turn right and continue west to red light and intersection with Rt. 12, then turn left and continue on Rt. 12 to Prospect Street. Good exposures of outwash and terrace levels in main part of valley floor. On the valley walls are exposures of Binghamton till at Rappaport's and Grand Union.

STOP 5. Borrow pit in Olean till
Old borrow pit on right side of road is in Olean till. Elevation 940'. See text for characteristics of valley fill across the Chenango and Susquehanna valleys. S 300W is well field for ANSCO. Yield of wells range from 150- 1,800 gpm. ANSCO has a recharge program in which water is recycled back into the aquifers. Continue west to the next stop by taking Prospect Street, Harry L. Drive, and just west of Calvary Cemetery.

STOP 6. Borrow pit in Olean till
Borrow pit on right side of road in Olean till. Used as fill in flood wall construction. Return to Rt. 17 on south side of Susquehanna River through Oakdale, Rt. 17H and Riverside Drive, and across Johnson City-Vestal Bridge.

Kettle Hole
Star-Victory marketing area is located in kettle hole. This is one feature in a morainic complex that extends 0.8 mi. west and was the former site of Susquehanna River prior to blockage.

View of terrace
Good view of 860' level terrace, one part of a vast outwash plain that continues west past Tracy Creek.

Binghamton-lithology till in borrow pit on left side of road (stop 9).

Deltaic outwash
Deltaic outwash on south in area of Federal Electronics.

Outcrop of Lower West Falls Group
Bedrock, claystone and shale. Lower West Falls Group (Rhinestreet Formation). Used for bricks and fill.

Choconut Creek
Choconut Creek. Flood walls built by Army Corps of Engineers as part of flood-control project in the Triple Cities area. This area is site of Town of Vestal well field. Wells did not encounter bedrock at 170' and yield 70,000 gallons per day per foot of drawdown. West of this area at Castle Gardens are large quarries in sand and gravel outwash.

Unconsolidated glacial materials on left side of road (Stop 8).

STOP 7. Bedrock walls of Tracy Creek
Bedrock walls of Tracy Creek. (Rhinestreet Formation) This is post-glacial gorge and typical of the many drainage diversions in the Binghamton area. It is common for these derangements to occur near the junction with major streams. This is similar to the Tioughnioga junction diversion. The pre-glacial Tracy Creek channel is east and became choked with morainic debris. The stream, unable to locate its clogged former channel with disappearance of the ice, incised a new channel as a superimposed stream, even though in bedrock.

West side of Tracy Creek
Bus stop only to show the west side of Tracy Creek. Olean till occurs in stream cut but varve clays are at the top of the sequence. This exposure completes the history of this local area for the morainic dam impounded waters flowing north and formed a lake, the outlet of which overflowed and started incisement of the bedrock gorge. The lake may have been in existence more than 200 years. Olean-Binghamton transitional facies also occurs.

Pre-glacial Tracy Creek
Turn sharp left on Ross Hill Road. Outcrops of Olean till occur on the right side of road. This area is site of pre-glacial Tracy Creek.

STOP 8 Borrow pit
Triple Cities Construction Co. equipment area and borrow pit. The glacial deposits are lacustrine sands, silts, and clays at 840' with Binghamton till on top. The till has the appearance of being in part ice-rafted.

STOP 9. Borrow pit
Large borrow pit near African Road. This material was used in construction of flood walls for the containment of the Susquehanna River. This is typical Binghamton till. The oxidized and leached upper 12' are characteristically brown and below is gray unleached till'with high limestone content. The pebbles have bi-modal roundness parameters indicating a dual source, one of local derivation, and the other of longer transport that initially were river-worn. The small butte-like remnant is composed of glacial-lacustrine beds at 850'. Recent excavation (April 6, 1963) reveal the locality from African Road to Federal Electronics to be a complexly developed till-lacustrine-deltaic-ice contact area capped by alluvial fan materials.

Outwash terrace
Turn left at African Road and in .2 mi. turn right on Vestal Road. This is outwash terrace with quarries occurring .6 mi. on left side of Vestal Road.

STOP 10. Barney Dickenson Company quarry
This is the second stop called STOP 9 in the guidebook...
STOP 9. The materials originated as valley train outwash in the Susquehanna valley glacial sluiceway. The coarse materials are horizontally-bedded and underlain by sands that are commonly crossbedded. Cemented conglomerates in the southeast part of the quarry show the results of the high limestone content in the lithology. In materials larger than gravel size the limestone is more than 25% and the igneous-metamorphic crystallines are more than 15%. Heavy mineral composition of the sands show more than 40% magnetite, 18% garnet, 10% ilmenite, and also containing kyanite, zircon, tourmaline, hematite, rutile, and hornblende. A mastadon tusk was found in the higher outwash gravels immediately south of the washing-sieving equipment in 1953. It is reported that the skull, jawbone, and teeth of a "horse-like animal" were found in 1956 in the same horizon 700 feet east of the mastadon location. These materials presently reside at Yale University, waiting for final identification.
1962 Annual Report of Barney & Dickenson, Inc.
(sent to U. S. Dept. of Interior, Bureau of Mines)
Type of Material | Quantity (Tons) | Value
2. Gravel | |

C: FACIES AND THE RHINESTREET FORMATION IN SOUTH CENTRAL NEW YORK
Donald L. Woodrow, Department of Geology, University of Rochester
Robert C. Nugent, Department of Geology, Northwestern University
174.8 miles

C: FACIES AND THE RHINESTREET FORMATION IN SOUTH CENTRAL NEW YORK

STOP 1. Doubleday Glen
Exposures of the Dunn Hill and Beers Hill Members of the Rhinestreet Formation. Elevation of exposure: 975'.
After leaving the busses, walk up the hill to the terraced exposure where the dark gray shales of the Dunn Hill Member may be seen. Small flow rolls are exposed here and many additional flow roll zones are visible in the stream bed of the Glen. Excellent view to the southwest, across the Susquehanna River. Red sandstones and shales of the "New Milford Formation" cap the hills visible across the river.

STOP 2. Binghamton Brick Company Quarry
Exposures of Moreland and Millport Members of the Rhinestreet.
Elevation of the quarry floor: 900'.
The very dark gray shales exposed at the base of the quarry are the easterly equivalent of the Moreland Member. No other dark gray shales such as these have been found at higher elevations in the quarry.

STOP 3. East Beecher Hill Road
Exposures of Beers Hill and Roricks Glen Members of the Rhinestreet. Elevation at bottom of exposure: 950'.
The Roricks Glen is represented by scattered, very dark gray shales at the upper end of the exposure. Flow rolls are well developed here. Cyrtospirifer sp. have been reported from strata at bottom and top of exposure.

STOP 4. Smithboro Section.
Smithboro Section. Exposure in Beers Hill Member of Rhinestreet. Elevation: 1000'.
This is an excellent, although small, exposure of Chemung lithofacies and biofacies. Massive sandstones and underlying mudstones are highly contorted in large flow rolls. Numerous brachiopods, pelecypods, and rugose corals may be collected.

Beers Hill Member
Exposure in Beers Hill Member, approximately 75 feet above the Dunn Hill member: lithologies Portage-like with rare, diminutive forms of
Cyrtospirifersp. reported.

STOP 5. Chemung Narrows. (0.4 mile stretch)
Exposure in the Gardeau Formation. Elevation: 800'.
This exposure is one of the most famous Upper Devonian sections in North America. Here, the typical features of the Chemung magnafacies are developed and well exposed. Notice the well formed flow rolls and prolific fauna. The proximity of this exposure to the highway makes it unsuitable as a place for discussion; therefore, we will move a short distance west and cross the Chemung River to a similar exposure, stratigraphically higher.

STOP 6. Wellsburg Section.
Exposure in the Gardeau Formation. Elevation: 840'.
This is a fresh (1962) exposure of lithologies similar to those seen at stop 5. Flow rolls are rare, but fossils may be collected readily. This road-cut and the section exposed along the railroad below the road served as the type section of Williams, Tarr, and Kindles "Wellsburg Sandstone Member of the Chemung Formation" (1909).

Gardeau Formation
Sandstones of the Gardeau Formation exposed on north side of road.

Millport Member of Rhinestreet Fm
Leave 17 for Elmira via East Church exit (extensive cuts in the Millport Member of the Rhinestreet Formation on the north side of the exit ramp.)

STOP 7. East Church Street Quarries
Leave busses at first dirt road to right after crossing bridge. Walk to quarries.
Exposure of the .Millport and Dunn Hill Members of the Rhinestreet. Elevation 910".
A comparison of the lithologies displayed here with the Iithologies seen in the Millport of the Binghamton region illustrates the facies changes that have occurred. At the top of this quarry may be seen the heavier-bedded siltstones and fine-grained sandstones of the upper Millport. The quarry floor and lower faces are cut into the black and very dark gray shales of the Dunn Hill Member.

STOP 8. Type Section of Dunn Hill Member.
Leave busses at first dirt road to the right (north); walk to stream exposure.
Elevation: 1010'.
In this stream, the Dunn Hill Member is 22 feet thick and is composed of gray, silty shales and mudstones with nearly eight feet of black and very dark gray shales of which the majority is concentrated in the basal ten feet of the member. A tributary of this stream draining the hill to the south is the type section of the overlying Beers Hill Member of the Rhinestreet.

STOP 9. Reference Section for Moreland Member
Black shales of the basal Moreland are exposed. Elevation: 1380'.
Owing to time limitations, the type section of the Moreland Member (in Hamilton Creek, one mile north of this stop, elevation: 1370') will not be visited, however, the black shales may be observed here. In addition, the limey mudstones and shales of the underlying Rye Point Member of the Sonyea Formation are well exposed in this stream.

Ithaca Formation
On the right (west) side of 14, exposures of the evenly bedded siltstones and shales of the Ithaca Formation are continuous from Watkins Glen to Montour Falls.

Ithaca Formation
Road cuts on north side of road; excellent exposure of siltstones in upper part of the Ithaca Formation.

Montour Member (Middlesex Formation)
Exposure of Montour Member (Middlesex Formation) under bridge in center of town.

Millport Member
Exposures of Millport Member on right (south) side of road.

Langsford Creek occupies valley on the left (north).

Beers Hill Member
Excellent exposures of the Beers Hill Member of the Rhinestreet in the hillside directly across the intersection from the bridge. Other exposures may be seen along 38 to the left (north).

D: GENERAL GEOLOGY OF THE WESTERN CATSKILLS
Donald R. Coates
132.5 miles

D: GENERAL GEOLOGY OF THE WESTERN CATSKILLS

STOP 1 Glacio-fluviatile and glacio-lacustrine beds
Outcrop of glacio-fluviatile and glacio-lacustrine beds intermixed with till and a deltaic complex. Lithology of the larger rocks includes red sandstone, local siltstone, and coquinite, and some igneous-metamorphic crystallines. Limestone is rare. The Susquehanna River is 810' and adjacent hills are 1500'-1600'.

Glacial Channels
Stay on Rt. 17 as Rt. 11 turns south. The wide area of unconsolidated materials was produced by junction of the west-flowing Park Creek and south-flowing Stanley Hollow. The latter stream was a major overflow channel of glacial waters when the ice front was north of the area.

Climbing out of the Susquehanna valley
Stay on Rt. 17 at Penn-Can turnoff. Climbing out of the Susquehanna valley. Will see Susquehanna again at Windsor.

STOP 2. West Falls Group
Lithology is largely shale and siltstone with some fine-grained sandstone. A few thin coquinite beds are present containing brachiopods and crinoid columnals. The original limestone has been removed. Several excellent horizons of flow rolls occur. The lack of parallelism of flow rolls and bedding planes is seen in the easternmost part of the outcrop. Radiographs done at Harpur (Greene and Coates, 1963) of sections cut at different orientation of the flow rolls indicate some interior structures of small-scale folding and gravity faulting. An angular unconformity occurs at this stop. Rocks also contain many other structures, both primary and secondary in origin. Next to the bedding characteristics in rock importance is the universality of the joint patterns. Two sets are well-developed throughout the Catskill region.

West Falls Group
West Falls Group on south side of road. Similar to stop 2. Throughout this area the hills are capped by sandstones of the continental facies of the Catskill delta-alluvial plain complex, but only marine facies rocks are visible along the road at the lower elevations.

Walk on the west side of house down to flood plain of Occanum creek about 500 feet. On south side of creek is 50' high outcrop of Olean till (Catskill phase). The bedrock that occurs upstream indicates that in places Occanum Creek occupies a post-glacial channel.

Terrace development
Excellent terrace development at the community of Occanum. The origin of this type feature will be discussed later.

Choker Moraine
Thick till "choker moraine". This feature is also common along the route that will be travelled and it will be discussed later.

Susquehanna River
The Susquehanna River, elevation 920', flows south. The hills are 1700'- 1900'. Occanum Creek forms an alluvial fan and the village of Windsor is built on the junction of the alluvial fan and the 980' level of outwash developed by the Susquehanna River in glacial times during ice recession. This terrace extends to Sage Brook and Rt. 79 utilizes it. Well-developed flood plain occurs in the present Susquehanna channel area.

Sage Brook.
Top of alluvial fan is 1000'. Olean till (Catskill phase) is exposed on north side of stream. This is the southern edge of the morainic barrier that extends northward around the river meander.

Channel, terraces, etc.
Turn right (east) at Ouaquaga over Susquehanna River and keep left at road Y .2 mi. Good view of present channel, plains and terraces on this west-flowing stretch of river.

STOP 4. Gravel Quarry
This is a .25 sq. mi. area of stratified glacial deposits. Materials have a wide range of size, composition, and structural forms. The history of this area originated with blockage of the river by ice and morainic deposits in the channel to the west. The glacial meltwaters were diverted to a low pass east of the former valley, causing incisement of the former divide. Further recession of the ice front occurred with the abandonment of stagnant blocks that melted more slowly owing to favorable positions of insulation. These conditions account for the complex bedding, size, and sorting of material relations. Much evidence of ice-contact deposits, lacustrine conditions, deltaic sedimentation,and valley train outwash is visible. Disconformities occur indicating an erosional interval separating deposition of older and coarser materials from younger sands. In some of the outwash sands there are veinlike structures composed of "bridged" grains. Norma] faulting is also present. Travel in and out of quarry is .6 mi.

Overflow Channel
From the quarry take the road south to East Windsor, pass under the tracks and turn right (south) at the T. This valley is the former overflow channel of the Susquehanna that was in turn abandoned when the drift dam was breached in the older channel to the west. Elevation of the pass is 1000'

Damascus - Marine / Non-Marine interfingerings
Damascus. To this point the route elevation has been 900'_1050' and at this level all bedrock is marine. Rock exposures in the new Rt. 17 roadcuts at Damascus indicate this is the strand line at road level. There are many interfingerings of marine and non-marine beds at this locality. Eastward the rocks are mostly non-marine. Damascus is on an incised alluvial fan of Tuscarora Creek. The road now climbs what is locally called "Tuscarora Mountain", and hill elevations are over 1900'.

Non-marine strata
South of the road is the first visible exposure of the non-marine strata of the Catskill delta-alluvial plain complex. Formations are still in the West Falls Group and are continuous for more than one mile.

Deer Lake.
Deer Lake. This lake along with Sky Lake one mile north and Fly Lake one mile south occur in the drainage of Fly Creek. The amphitheater-like basins all contain constrictions on the south suggesting their glacial origin of impoundment of south-flowing Fly Creek behind morainic loop dams. This pattern is repeated throughout the Catskill area.

Turn right (south) to Gulf Summit. This area contains a great variety of glacial deposits, many are stratified. This is a topographic hollow with slopes rising on all sides, and thus was the locus for a large stagnant ice mass. The meltwater drainage was southwest and a deep notch was incised southwest of the village. This is now the divide, elevation 1375', between Cascade Creek flowing west to the Susquehanna River and a tributary of Fly Creek flowing east to the West Branch Delaware River. (see Fig.7 and 8) Cascade Creek with greater gradient is capturing drainage that formerly went eastward. 2.2 mi. round trip to Gulf Summit and return to Rt. 17.

Sand and Gravel Quarry
North of road is sand and gravel quarry developed in materials that indicate deltaic and glacio-fluviatile origin. These deposits are typical of the Otisville gravelly loam that occurs as a terrace-band through this area at elevations that reach 1410'. Thus, at a minimum there has been more than 36' of post-glacial incisement through the pass at Gulf Summit.

Former location of an esker
Junction of Rts. 17 and 41. At this location on north side of road was a well-developed esker, recently demolished during construction of the new road. From this point to Deposit in the Oquaga Creek valley are many glacial deposits, including high-level hanging deltas. See text for data on Oquaga Creek.

Deposit - Lunch Stop
LUNCH STOP at the Jordan House. This town is often given as the western boundary of the Catskill Mountains. Eastward the rocks are all continental, (Fig.4) and the stratigraphy for the general area is the Sonyea Group, with the Stony Clove and Lower Katsberg formation in the valley and lower slopes and the Upper Katsberg formation of the West Falls Group on the higher slopes and capping the mountains.

Upper Katsberg beds
Turn on Rt. 10 left (east) at stop light. stay on Rt. 10 to Cannonsville, 9.2 mi. The route parallels the west-flowing West Branch Delaware River. Upper Katsberg beds will be seen on left, with cross bedding, typical of many non-marine sandstones. Large outwash area is present on south side of river.

Temporary end of Route 10
Old Rt. 10 has been abandoned east of intersection of Rt. 8 and Cold Spring Creek. This is new bridge over the river and all the new construction was necessitated by development of Cannonsville dam and area as a reservoir for New York City. Work is done through the office of the Board of Water Supply.

Massive continental sandstones.
Massive continental sandstones. This is near contact of Upper Katsberg and Slide Mountain formations. Good exposures for .8 mi.
From one page handout (1963): Spectacular rock cut in diversion channel showing more than 100' of non-marine Catskill-type beds. Channel filling, faults, variations in color and lithology.
2010: Reservoir filled in 1964-5, so much may now be inundated.
DEC Unique Geologic Landforms 180: Deposit State Hwy 10

STOP 6. Cannonsville Dam
Picture stop for Cannonsville dam area. The Board of Water Supply, City of New York was created in 1905. Since that time water use in New York City has risen from 400,000,000 gallons per day to 1,200,000,000 gpd in 1955. Estimated usage for the year 2000 is more than 1,900,000,000 gpd. The Catskill system of reservoirs was started in 1907 for eastern drainages. When these supplies appeared inadequate for continued growth of the City, enabling interstate legislation was undertaken to use Catskill drainages of the west-draining Delaware River. In 1931 by court action 440,000,000 gpd could be used by the City and this was increased to total usage of 800,000,000 gpd in 1954. Total cost for the present Catskill reservoir system is well over $1 billion. The Cannonsville Reservoir will impound 97.4 billion gallons in the 450 square mile drainage area of the West Branch Delaware River. The dam is an earth embankment about 1,500' long and 175' high. The water supply will move by gravity through the West Branch Tunnel to the collecting Rondout Reservoir. The tunnel will be 44 miles long and 11.3 feet in diameter. Estimated cost of the dam and reservoir construction is about $60 million and the tunnel at $81 million. (Source: 50th Anniversary Report of the Board of Water Supply).

STOP 7. Catskill-type red beds.
Catskill-type red beds. View of the village of Cannonsville that will be inundated when construction of area has been completed. (see Cover page for picture taken prior to construction). 2010: Location is about as close as the dry land gets to where Cannonsville was.

Ascent of Trout Creek
Pass over West Branch Delaware River and at Cannonsville turn right .2 mi. then left (north) up Trout Creek. (see text for Trout Creek data) Cannonsville was built on materials that developed a small alluvial fan and terrace. Soil classification is Tunkhannock gravelly loam. It is 114' to bedrock. A variety of phenomena can be seen during ascent of Trout Creek. The valley slopes are in places bedrock (lower Katsberg Formation), and in others show unconsolidated materials some till, some stratified outwash and kame terrace deposits, and probably some of the large blocky rocks are in the range of congeliturbites. In places the road is on a terrace and there are constructional hills, mostly kames, developed in a valley-choker type of morainic complex. North of the kame and terrace area are flat plains of lake deposits impounded by the stagnant ice.

Lacustrine Sands
Lacustrine sands were uncovered during construction of the new bridge and another well-developed lake plain occurs upstream from this locality.

Alluvial fan
Rock Royal. Sherruck Brook has developed an alluvial fan and associated with it is glacial outwash. On east side of Trout Creek are more exposures of stratified outwash. Lake plain occurs north of this area.

Trout Creek
Village of Trout Creek and intersection of Rt. 206. Continue north. Valley fill is 60' thick.

Glacial topography
Glacial constructional topography of knobby-morainic hills, incised by a post-glacial, V-shaped gorge. This pattern will be seen many times on the trip.

Bedrock and morainic loop.

STOP 8. Stone net
Stone net in lower Katsberg Formation. This was first noticed by E.H. Muller. Open meadows such as this, throughout the Catskills, often show similar features. The slabs develop polygonal shapes, and constantly change in attitude from the center of a net. There is also some tendency for size-sorting of slabs. The original spacing of joints seems to influence the location and development of the nets. Frost heaving and ice wedging aid in deterioration and movement of the slabs.

Drainage divide.
Drainage divide for Susquehanna and Delaware systems.

Morainic loop.
Morainic loop on left side of road with post-glacial gorge.

Man-made lake.

Gulf Oil Company test well
This is site on right side of road of Gulf Oil Company test well drilled by Delta 29. On March 16, 1963, 3800' of rock had been drilled in about a month. Apparently the hope is that Oriskany sandstone when encountered will contain oil or gas of commercial value. From this position the road descends to Ouleout Creek drainage area.

STOP 9. East Sidney Dam
East Sidney Dam and Ouleout Creek drainage area. See manuscript for data on Ouleout Creek and Figure 9. Turn right .3 mi. to dam. Oneonta formation red beds occur at base of dam. East Sidney Dam built by Department of Army, Corps of Engineers. Completed 1950.
Dam characteristics: |
Quantity of concrete: | 156,000 cu. yd.
Height above Ouleout Ck.: | 130'
Length of Spillway crest: | 240'
Total length of concrete dam: | 750'
Embankment: |
Rock Fill: | 113,000 cu. yd.
Earth Fill: | 194,000 cu. yd.
Excavation: |
Take Rt. 7B from the dam going east WEST until intersection with Rt. 7. This part of road traverses excellent kame and kettle topography. There are two well-developed lower terraces before Ouleout Creek unites with the Susquehanna River. Sands and gravels are Tunkhannock gravelly loam, the upper terrace is Tioga silt loam and lower terrace is Chenango silt loam.

Oneonta formation
Rt. 7 turn left (south) to Unadilla. Oneonta formation crops out along railway cut. Susquehanna River flows south, elevation 1000'. Hills rise to 1900'.

STOP 10. Quarry
STOP 10. Quarry southwest side of Unadilla. This area is kame and kettle topography within a morainic complex that impounded meltwaters during glacial recession. Extensive lake plains and terraces levels and remnants of levels occur from this position upstream several miles. This pattern is repeated several times downstream in the Susquehanna valley. See text for description of lithology.

STOP 11. Masonville Quarry
Owned and operated by The American Blue Stone Company, New York, N.Y.: has been in operation since 1945. (See Fig.6) Current level working area is about 250' x 100' and production is confined to mill blocks. The processing plant is in South Unadilla. The quarry is flooded during the winter months to a height five feet above the lower bench to protect the stone from ice and frost damage. Mr. James J. Newberry has kindly qiven information about the quarry and has given permission to visit it. The mill processes 16,000 cu. ft. of stone from this quarry.
DEC links 1 2 3

River confluence
This is near the confluence of the Susquehanna and Unadilla Rivers. Streamflow of these rivers in this area are: Susquehanna River at Unadilla, N.Y., 1,626 cfs for 984 sq. mi. drainage area, and Unadilla River at Rockdale, N.Y., 842 cfs for 518 sq. mi. drainage area. Although the Susquehanna has two times the flow today owing to the larger drainage area, it is probable that the Unadilla carried more water during the ice ages. The headwaters of the Unadilla are at lower elevations than most Susquehanna tributaries and the major tributaries of the Unadilla occur in through-valleys. Overflow of the glacial lakes in the Mohawk Valley Region therefore found ready-made outlets in such rivers as the Unadilla and Chenango, and turned these valleys into giant sluiceways for the impounded glacial waters. There is a high-level drainage channel of the Unadilla in the saddle that occurs just east of Mt. Moses, the hill that rises north of the intersection of Rts. 7 and 8. Throughout the Sidney area are outwash sand and gravel quarries. Terrace development is common and a good view of the 1010' level occurs on the south side of river.

Outwash materials
Quarry outwash materials, coarse and rubbly at the bottom and finer sands and gravels at the top. The road is built on the 1010' terrace level. 2010: GE says 990'.

Bainbridge
Bainbridge is built on the 1010' terrace. Susquehanna River is 975! 2010: GE says 990' and 962'.

Olean till
Olean till on right side of road. (See text for description).

Ice contact features.
Sand and gravel area. Ice contact features are present. The Susquehanna is incised through the outwash plain.

Kettle hole lake
Afton Lake, a kettle hole lake. This is kame and kettle topography, created in part by a morainic complex. The locale is characteristic of many others in the Susquehanna valley, in which the constructional topography occurs near the junction of the Susquehanna and a tributary. The south-flowing Kelsey Brook is an underfit stream and the morainic areas are upstream in the Susquehanna valley.

Kame and kettle
More kame and kettle topography near the mouth of the north-flowing Cornell Creek on the south side of the Susquehanna valley.

STOP 12. The Plains
The Susquehanna River 950' elevation has incised more than 100' through a broad and exceptionally well-preserved 1060' terrace level, called "The Plains". Remnants of this level can be found several miles along the Susquehanna.

Leaving Susquehanna River
We are now leaving the Susquehanna River which turns south. The road ascends Belden Brook up to Belden Hill.

STOP 13. Parking area
Elevation 1650'. Near the Chenango-Susquehanna drainage divide. View to the south provides appearance of accordant summit levels. The summits actually range between 1600' and 1850'. Westward the road follows a tributary of Osborne Creek, an underfit stream. There are a series of at least four different morainic loops in this tributary system of the Chenango. These choker moraines occur at intervals from the parking area of 1.6 mi., 1.6 mi., .5 mi., and .9 mi. Notice the flat topography that is always upstream of these constructional areas.
2010: This is the last stop from the 1963 Field Trip. They returned to Harpur by older roads, we go back to SUNY Binghamton by expressways...

New York State
Geological Association
Guidebook
John James Prucha, Editor
Department of Geology, Syracuse University, Syracuse, N.Y.

A: GEOLOGY OF THE SOUTH-CENTRAL ADIRONDACK HIGHLANDS
Cedar River - Blue Mountain section (CR)
by Dirk de Waard
Snowy Mountain Section (SM)
by William D. Romey

STOP CR 1. View to SW from Cedar Bend Lodge
View towards the southwest from hill opposite Cedar Bend Lodge (ask permission). In the Cedar River valley marble and other supracrustal rocks are exposed which are folded in a syncl inal keel wedged in between the Snowy Mountain dome towards the south (left) and the Wakely Mountain nappe towards the west (right). Dip of foliation and bedding in the structure is to the northwest (right), and the fold axis plunges west. Dip slopes of the Snowy Mountain dome are visible towards the south. Gneisses of the Wakely Mountain nappe are exposed in Wakely Mountain, Round Top, and Blue Ridge to the west. Sugarloaf Mountain in the center is the gneissic core of the syncline.

STOP CR 2. Charnockitic gneisses
Ledges in bushes on right are charnockitic gneisses which form the uppermost overturned portion of the core of Wakely Mountain nappe. Stratigraphically overlying amphibolite and marble are exposed in several places along the road.

STOP CR 3. Supracrustal strata
Stop 3. Short walk up hill to the right to the first ledges of Sugarloaf Mountain. Traverse across supracrustal strata of diverse composition (marble, amphibolite, layered gneisses, diopsidic quartzite and gneiss, diopsidite) towards the core of the syncline which consists of gneiss.

STOP CR 4. Trail to Cedar River falls
Small trail to the left down to the Cedar River. Gorge and falls in marble. Walls demonstrate intense plastic deformation and flow folding in the marble, distortion and rotation of amphibolite pieces. Exposures of amphibolite, quartzite, and sillimanitic garnet-biotite gneiss.

STOP CR 5. Large garnets
On the left, about 30 meters in the bushes, is a small outcrop of amphibolitized metadolerite (sill in charnockitic gneiss of Stop 6). The amphibolite consists of andesine, hornblende, and orthopyroxene. The exposure shows some large garnet porphyroblasts (15 cm diameter) similar to those of the famous Gore Mountain occurrence. PLEASE DON'T SAMPLE THE GARNET HERE. Others may like to see this outcrop after you.

STOP CR 6. Core of Wakely Mountain nappe
Road cut on the left shows typical grey-green, hornblende-bearing, perthitic charnockite of the basement core of the Wakely Mountain nappe.

STOP CR 7. Large road cut
Large road cut on the north shore of Lake Durant. The section of diverse, layered metamorphic rocks includes pink and greenish leucocratic gneisses with thin metabasic layers, marble, and calc-silicate rocks. The section forms part of the supracrustal sequence which overlies the leptites of the Wakely nappe exposed in the hills visible towards the south across the lake, and which underlies the Blue Mountain charnockite sequence towards the north. Lineations on foliation planes indicate a 30° NE plunging fold axis. The intrusive nature of marble into boudinaged layered gneiss is shown on the west end of the north side of the road cut.

STOP CR 8. Supracrustal charnockite
Road cut on the right just downhill from diner, in charnockite of the supracrustal sequence. The grey-green charnockite, interlayered with metabasic rocks and tremolite schist (in the brook), is part of a series of charnockitic rocks which presumably forms an isoclinally folded, complex syncline (Blue Mountain). The charnockite layers, which overlie the marble exposed in the lake and the rocks of stop 7 north of Lake Durant, form part of the supracrustal envelope of the Wakely-Mountain nappe. The Blue Mountain charnockite sequence is considered to be equivalent to the Little Moose Mountain sequence of charnockites. They are stratigraphically the youngest supracrustal rocks known in this area. The composition of the charnockite at this stop is predominantly:

STOP CR 9. Large migmatite exposure
Large exposure in the brook on the right shows pattern of typical migmatite (crocydite) in quartzofeldspathic metamorphic rocks of the Adirondack highlands. The metatect is anatectically generated granite in hornblende-biotite-quartz microcline microperthite oligoclase gneiss. The gneiss grades into charnockite and belongs to the Blue Mountain charnockite sequence.

STOP SM 1. Augen gneiss of Snowy Mtn dome
Stop 1. Roadcuts O.1 miles west southwest of trail leading to the top of Snowy Mountain. K feldspar-plagioclase-quartz-andesine-pyroxene-hornblende augen gneiss (charnockitic "Keene"-type gneiss) of the type which is widespread in Snowy Mountain dome. Foliation about horizontal.

STOP SM 2. Leuco metanorite
Stop 2. From the highway walk west a few yards along a narrow dirt road to flat outcrops. Andesine-pyroxene-hornblende gneiss with relict ophitic to hypidiomorphic granular texture preserved. Note relict cores of dark gray plagioclase (An42) surrounded by recrystallized plagioclase (approximately An34). Square masses of plagioclase are outlined by partially recrystallized mafic minerals. This rock is similar to some of Buddington's gabbroic anorthosites, but we have preferred to call it a (leuco) metanorite. Foliation dips west southwest at a low angle.

STOP SM 3. Anorthosite
Stop 3. Large roadcut on the hill 0.4 miles southwest of the intersection of highway 30 with the lake shore road through Sabael. Anorthosite at the lower end of the outcrop is overlain by metanorite (unfoliated andesine-pyroxene-hornblende gneiss) which is in turn overlain by streaky andesine-pyroxene-hornblende augen gneiss. Both "Marcy-" and "Whiteface-" type anorthosites are present. The grain size of metanorites ranges from coarse to fine, and the original texture of the rock is preserved to various degrees in different parts of the exposure. Several small amphibolite (metadolerite) lenses may be observed in the streaky gneiss. Foliation is nearly horizontal. Walk up the steep hillside above the road to see massive ledges of anorthosite, metanorite, and a rock which is texturally and compositionally intermediate between these two types.

STOP SM 4. Well foliated gneiss
From the intersection of highway 30 with the lake shore road through Sabael walk east about 100 yards on a private road (get permission) leading to a house on a small peninsula. Outcrops are on the lake shore east of the house. Well-foliated K gneiss (charnockite). Domal structure of the complex on the east side of Indian Lake can be observed from the point east of the intersection.

STOP SM 5. Charnockitic augen gneiss
Roadcuts on the main road 0.1 miles northeast of Squaw Brook. Charnockitic augen gneiss similar to the rock seen at stop number 1 (K gneiss).

Banded gneisses in roadcut
No stop. From the bus observe banded gneisses in roadcut. K feldspar-quartz-plagioclase-amphibole gneiss is interlayered with plagioclase-hornblende-biotite amphibolite.

STOP SM 6. Last of the anticlinal core rocks
Stop 6. Roadcuts consisting of well-foliated, homogeneous, leucocratic charnockite (K feldspar-quartz-plagioclase-pyroxene-hornblende-garnet gneiss). A few amphibolite layers are present. This is the granitic end-member of the "syenite" series of Buddington. This is the last stop in what we have called "anticlinal core rocks".

STOP SM 7. Supracrustal rocks
Roadcuts consisting of banded microcline-quartz-plagioclase-hornblende-pyroxene gneisses. These are the first clearly supracrustal mantle rocks overlying the anticlinal core rocks. Note intense folding of the gneisses.

Extra STOP SM 1. Gneiss with large diopside clots
Roadcuts of feldspathic gneisses containing large diopside clots. About 0.2 miles west of the road are spectacular exposures of the same gneiss in a newly reopened quarry (get permission to visit).

Extra STOP SM 2. Amphibolite and marble
East of Indian Lake village on highway 28 there are flat outcrops of amphibolite and very coarse-grained white marble at the outlet to Adirondack Lake. At times of high water these cannot be easily seen.

B: GEOMORPHOLOGY OF ONEIDA BASIN AND SOUTH SLOPE OF THE TUG HILL PLATEAU
by Ernest H. Muller, James S. Street and Jesse L. Craft

B: GEOMORPHOLOGY OF ONEIDA BASIN AND SOUTH SLOPE OF THE TUG HILL PLATEAU

Rise onto drumlinoid with veneer of red till.

Iroquois lake plain at 410 ft. msl.
Continuing on N.Y. Rte. 290, cross overpass and descend to level of Iroquois lake plain at 410 ft. msl.

Fremont Hill drumlinoid
Continuing on N.Y. Rte. 290, rise onto Fremont Hill, a drumlinoid that was an island in Iroquois Lake. Strand features are mapped at the 435 and 420 ft. levels.

Cemetery at 430 ft
Cemetery on right (S) as road returns to lake plain is at the 430 ft. level. Cross alluvial flats of Limestone Creek.

Abandoned feeder of Erie Barge Canal
Cross abandoned feeder of Erie Barge Canal and rise from Iroquois lake plain onto intensely scoured scarp developed on Syracuse fm. Excellent exposures of Syracuse fm in railroad cut, off route .4 miles SW.

Route parallels Erie Canal
At "t-intersection", turn left (E) to continue on N.Y. Rte. 290. Route parallels Erie Canal, with Iroquois lake plain on left and scoured, thinly veneered slopes on right.

STOP 1. Green Lakes State Park
Examination of notched Green Lake channel and Round Lake plunge pool. Discussion of meltwater channels, plunge pool development, interrupted plunge pool migration and limnology of Green Lake. See text, p.31.

Mouth of Green Lake channel
Turn right (E) onto N.Y. Rte 290. Embayed mouth of Green Lake channel debouched into Lake Iroquois at right.

Descend across weak 435 ft. strand
Descend across weak 435 ft. strand at curve in road. Cross abandoned Erie Canal and continue north through Kirkville on littoral sand and gravel.

Iroquois lake plain
Cross N.Y. Thruway overpass affording broad view of nearly level Iroquois lake plain. Pine Plains lie ahead right.

Dune and blow-out complex
East of first cross-road note yellow-brown sandy soil and irregular low relief of dune and blow-out complex related to strandline of late phase of Lake Iroquois which lies parallel and just north of the route for the next 3 miles. Dune configuration suggests dominant effective winds from the west-northwest.

Sand dune complex
Follow road in 90° curve to the right (S), then turn left (E) immediately at "T-intersection" to continue east on Chestnut Ridge Rd. through sand dune complex that borders Pine Plains on the south and Canastota mucklands on the north.

Cicero stage of Lake Iroquois
Turn left (N) onto Chittenango-Lakeport Plank Rd., In .2 mi. descend about 20 ft. across strand that marks Cicero stage of Lake Iroquois (Coon, 1960). Surface of Canastota muckland is approximately at 385 ft. msl.

STOP 2. Sky-High Farms
STOP TWO. SKY-HIGH FARMS (Smith-Coulter Co., Inc.) Peat, marl and bottom sediments of Cicero stage of Lake Iroquois, illustrating succession in filling of post-glacial embayment. Pulmonate gastropods in marl.

Eastward extension of the Lockport cuesta
Turn right (E) onto Lake Rd. in Lakeport. For next 7 miles, Oneida Lake is on left at 369 ft. msl, while a broad swell, elongate east-west, rises to the south of the route. Although it is virtually without bedrock exposure, this rise is considered to be an eastward extension of the Lockport cuesta.

Beach ridge
Turn left (N) onto N.Y. Rte. 13 across Oneida Lake plain. Cross Oneida Creek and continue on minor beach ridge, one of several at 375 ft. msl. that indicate steadily prograding east shore of Oneida Lake.

STOP 3. Verona Beach State Park
Rest stop. Summary of Iroquois lake history and Oneida basin geomorphology as encountered en route and at previous stops.

Oneida lake plain
Turn left (N) onto N.Y. Rte 13. Proceed across Oneida lake plain. Relief is less than 15 ft. for several miles to the east and the deepest part of the lake is only 55 ft. deep. This plain and basin occupy the structurally controlled lowland on the Clinton Group.

Erie Canal
Cross Erie Canal at Fish creek between Verona Beach and Sylvan Beach. In April, 1963, wind-driven shore ice rammed across the beach and against roller-coaster in amusement park at canal outlet into Oneida Lake.

Rise from Oneida Lake plain
Begin rise from Oneida lake plain across Iroquois nearshore and strand deposits. Medina-Clinton contact concealed and not established as having any relation to the shore scarp. At the "Sand Bar" on right, a low cut exposes 3 ft. of red-brown sand and silt over 8 ft. (base concealed) of red to red-brown rhythmically-laminated, but not varved, clay and silt. A well 1.5 miles southeast was drilled through 250 ft. of unconsolidated sediment reported to be dominantly lacustrine. The hole bottomed at 125 ft. msl without reaching bedrock.

Minor drift bench.
Turn right (E) on N.Y. Rtes 13 and 49 along a minor drift bench. Borrow pits dominantly expose ablation drift. Iroquois lake plain extends many miles east-west on right along trend of non-resistant Clinton Group.

Moraine divide
Turn left (N) in Vienna, following N.Y. Rte 13. Cross moraine divide between Oneida and Fish Creek basins.

West Branch Fish Creek
Cross West Branch Fish Creek. Pass Harden furniture plant and proceed north across remnant of Williamstown outwash plain.

STOP 4. G. W. Bryant Sand Pit
Examination of structures in stagnant ice deposits; discussion of aspects of sand and gravel industry.

Shallow meltwater channel
Proceed north following shallow meltwater channel incised into stratified drift of kame and kettle complex.

LUNCH STOP.
LUNCH STOP. Camden Methodist Church, served in Walker Memorial by Women's Guild.

STOP 5. Camden Wire Company Esker
STOP FIVE. CAMDEN WIRE COMPANY ESKER Examination of composition and structure as exposed in transverse and longitudinal sections of a small esker. Significance of "pseudo-anticlinal" structure in transverse section.

Stagnation features
Turn right (E) onto Pond Hill Rd. Continue across stagnation features marking progressive decay and wastage of the late Cary Oneida ice lobe.

Boulder gravel
At top of rise note boulder gravel exposed in road cut. Poorly sorted glacial drift is thick and bedrock is unimportant as a control of local relief in this area.

Climb sharply to higher bench.

STOP 6. Mack Pond Kettle Cluster
Examination of topographic and hydrographic relationships in a compact cluster of kettles and crevasse ridges at edge of the Pond Hill terrace.

Shallow marginal drainage line
Proceed east on Pond Hill Rd. Cross shallow marginal meltwater drainage line before rising sharply.

Head of meltwater channel
In one mile note swampy area on left which is at head of one of a series of eastward draining meltwater channels.

Cemented cobble gravel
Just before road enters shallow cut, cemented cobble gravel can be seen in overgrown cut 200 yds south of road. Leaving roadcut, descend on Rte. 69 over 30 ft. scarp which appears to be wave-cut.

Meltwater channels
Turn left in Lee, onto Lee Valley Rd. Cross Sash Factory Creek in swampy swale, the downslope continuation of meltwater channel seen on left 2.5 miles earlier. The right angle bend between channel segments suggests a subglacial meltwater escape-way. On right (S), shallow meltwater channel-way parallels road, curving eastward at about 520 ft. msl.

Cemented cobble gravels exposed on left (W)

Meltwater channels
Entering Lee Center, cross swampy meltwater channel with small pond on left and cannery on right. Channel alignment continues east from Lee Center as an obvious meltwater channel segment, but at slightly higher elevation than floor of the swampy channel segment that enters Lee Center from the west. Apparently segmentation of marginal drainage-way resulted from development of a subglacial escape-way downslope, now occupied by Canada Creek and Mill Road south of Lee Center.

Pass Sulphur Springs Rd
Exposures of Whetstone Gulf shale on left indicate probable of source of sulfur as being from decomposition of pyrite.

Outwash bench
Rise sharply and proceed east across outwash bench. Pass between Rome Reservoirs and angle across bench to Stokes.

Edge of Tug Hill Plateau
Begin rise across Quaker Hill, the southeastern tip of the Tug Hill Plateau developed on rocks of the Lorraine Group.

Ice walled meltwater channel
Minor bench and northward rise are remnants of former ice walled meltwater channel that is better developed about a mile west, and trends eastward toward Mohawk Valley.

West Branch Mohawk River
Cross West Branch Mohawk River at village of West Branch.

Diffuse moraine runs N-S
Continuing north on N.Y. Rte. 26, rise onto diffuse moraine that trends north-south, with best development of constructional topography west of the route between Ava and West Leyden. This is the first moraine of the Black River lobe encountered on this trip. The larger Oneida glacial lobe dominated and outlasted the Black River ice in this interlobate area in the lee of the Tug Hill nunatak.

East Branch of Mohawk River
In West Leyden, jog right with N.Y. Rte 26 to cross East Branch Mohawk River.

Increase in field boulders
At Redmond Corner, intersection with Webster Hill Road, continue eastward and begin to descend toward Boonville. Note increase in abundance of field boulders. In about a mile pass through area of minor stagnant ice features.

Black River Canal
Rte. 12 parallels the Black River Canal, built in 1855 to link navigable reaches of the Black River north of Lyons Falls with the Erie Canal at Rome. With a total of 109 locks in 35 miles the canal crossed a divide 700 feet above the Erie Canal. The substantial remains of a dozen or so locks are seen between Boonville and Sugar River which was crossed by aqueduct.

STOP 7. Sugar River at Boonville quarry
E. G. DeLia and Sons, Inc. Examination of stratigraphic section in quarry and of solution features along Sugar River.

Descend into channel
Continuing on N.Y. Rte. 46, descend 30-ft into broad flat-bottomed, rock-floored channel across ledge that controlled outflow from proglacial Port Leyden Lake through the Lansing Kill or Boonville Gorge. Continue south in channel, crossing diagonally to east side, thence back to west side to parallel the old Black River Canal.

Booneville Gorge
Shale bluff in roadcut on right indicates erosivity of rock into which the Boonville Gorge is cut. From Boonville to this point the gorge has become progressively more constricted. At left where Lansing Kill enters from the east side of the valley, post-glacial notching accounts for abrupt deepening of the gorge.

STOP 8. Boonville Gorge State Park. Pixley Falls
Rest stop. Consideration of significance of Lansing Kill Gorge.

Five adjacent locks
Five combines -- a flight of 5 adjacent locks on Black River Canal.

Mohawk River
Mohawk River enters Boonville Gorge from west with development of multiple terraces now incised by both Lansing Kill and Mohawk River.

Apex of meltwater delta
Village of Westernville, on right, near apex of delta built by meltwater stream through Boonville Gorge as it debouched into small lake impounded on southwest by the moraine at Rome. The Mohawk River subsequently incised a channel that swung diagonally across the valley from Westernville leaving the terrace remnants at 550-560 ft. msl., slightly above the level of Delta Reservoir.

Delta Reservoir Dam
Delta Reservoir Dam on right (W) of route. Mohawk River, incising its channel into delta and outwash deposits swung diagonally across valley from site of former village of Delta, to intrench itself at this point into Utica shale that walled the inherited bedrock valley. The steep-walled, 80-ft. deep gorge, known as The Palisade, provides a suitable dam-site for the broad, deep bedrock valley directly to the northwest is blocked by the late Cary recessional moraine at Rome. Construction of the dam in 1911 and impounding of the reservoir inundated the village of Delta, which survives only in the name of the reservoir. Through this gorge also passed the Black River Canal, traces of which can be seen beside the road directly up-valley from the dam.

State Fish Hatchery on right (W) side of road.

Griffiss Air Force Base
Bear left, continuing on N.Y. Rte. 46 at juncture with Elmer Hill Rd. Proceed south into Rome. Griffiss Air Force Base is at left (E) across Mohawk River, after Rte. 46 has become Black River Boulevard.

Narrowing Iroquois Lake Plain
Cross overpass over N.Y. Central R.R. and Erie Canal in middle of narrowing Iroquois lake plain. Less than 2 miles east is the highest elevation on the Erie Canal east of the Finger Lakes and the eastern end of the Iroquois plain. The Mohawk River having strayed from its westward-leading ancestral valley at The Palisade, has built an alluvial fan into the plain at this narrowest point. Flowing across this fan the Mohawk might as easily have drained westward, instead of eastward following the abandoned Iroquois outlet channel.

Iroquois strand
Pass entrance to Rome State School and rise obliquely across low slope of Iroquois strand.

Shallow meltwater channel
Shallow meltwater channel with threshold about 20 ft. above Iroquois strand is parallel to N.Y. Rte 365 for about 1 mile on right (NW).

Cowaselon Creek
Continue west on N.Y. Rte. 5, through Five Corners. Cross Cowaselon Creek which has cut a narrow flood plain into valley-choking glacial drift. Borrow pits at left (S), west of Cowaselon Creek, are opened in kame delta complex.

Wampsville
Village of Wampsville, location of Madison County Court House.

Canastota
Continue west on N.Y. Rte 5, following juncture with N.Y. Rte 13 in outskirts of Canastota. Samuel Champlain, French explorer fought a skirmish with Oneida Indians at village site, 6 miles south, during penetration southward from St. Lawrence settlements in 1615.

Iroquois Lake Plain.
Cross Chittenango Creek at level of Iroquois Lake Plain.

Pools Brook meltwater channel
In Mycenae, enter Pools Brook meltwater channel. For 3 miles, N.Y. Rte. 5 utilizes the low grade of this deep, transverse gorge cut by impounded pro-glacial meltwaters escaping east from Limestone Valley. Constructional topography extending into the west end of this channel indicates that principal erosion by meltwater preceded final melting of stagnant ice at channel-head near Fayetteville.

Floodplain of Limestone Creek
Continue west on N.Y. Rte. 5, through Fayetteville. Descend to floodplain of Limestone Creek at level of Iroquois Lake Plain.

Continue west
At juncture with High Bridge Rd. continue west on Rte. 5.

Descend to cross floodplain of Butternut Creek.

Syracuse Formation
Turn right (N) onto Erie Blvd. In about a mile, new construction has opened exposures in Syracuse formation on left.

C: STRATIGRAPHY AND STRUCTURE OF SILURIAN AND DEVONIAN STRATA IN THE SYRACUSE AREA
Newton E. Chute and James C. Brower

C: STRATIGRAPHY AND STRUCTURE OF SILURIAN AND DEVONIAN STRATA IN THE SYRACUSE AREA

STOP 1. Upper part of the Syracuse formation.
The contact of the Syracuse formation with the overlying Camillus shale is near the highest part of the excavation. The members exposed are as follows:
Upper dolomite member | Most of this member is exposed in the face above the bench. A distinctive porous dolomite bed, referred to in the literature as "vermicular" dolomite, is exposed in the lower part of the member. The holes of the vermicular dolomite probably were filled originally by salt or anhydrite.
Upper clay member | This member is about 10 feet thick here according to Leutze (1955, M.S. thesis, Syr. U.). It is mostly concealed under the floor of the bench and the talus debris.
Middle dolomite member | Thin- to medium-bedded dolomite. A few exposures of the upper part of this member may be seen below the bench.

STOP 2. Syracuse formation
A bed of gypsum 2 to 4 feet thick in the Lower Clay member is exposed near the bottom of the excavation behind the Victory Market and the Towne Mart. This gypsum bed is overlain by the Middle Dolomite member composed of impure thin- to medium-bedded dolomite and gypsiferous shale to the top of the excavation.

Meadowbrook cross channel
Meadowbrook Drive follows a well-defined glacial cross-channel that carried meltwater drainage eastward

STOP 3. Camillus shale.
Some of the upper part of the Camillus shale formation is exposed in small gulleys on the hillside. The rock units visible are as follows:
1.5' | Greenish gray thin-bedded dolomitic shale
6.5' | Massive greenish gray dolomitic shale with scattered quartz sand grains. This rock weathers rapidly into small angular fragments.
2' | Dolomitic thin-bedded shale that breaks into thin slabs and resists weathering better than the greenish shale above.
5' | Gypsiferous shale and gypsum? now partly leached to clay.
8'1" | Covered
2'
Massive greenish gray dolomitic shale with scattered quartz sand grains similar to the greenish shale above. This exposure is in the ditch on the east side of the macadam roadway.
Downhill, about 50 feet lower stratigraphically, 4.5 to 5 feet of greenish shale with thin beds of brownish dolomite are exposed in the bank at the uphill side of the playground behind the Washington School. These exposures probably are near the middle of the Camillus.
The Camillus of the Syracuse area seems to be unfossiliferous.

Drumlins
For the next 2 miles the route passes through a group of drumlins and bedrock exposures are scarce

Northern end of a drumlin
Between Randall Road and Guintard Road (McGee Road) the route swings west around the end of a drumlin.

Rock Cut gorge
Entering Rock Cut gorge, the largest of the cross channels, eroded by the outflow from glacial lakes in Onondaga Valley to the west. The floor of this channel is the Fiddlers Green dolomite member of the Bertie formation. It "hangs" about 140 feet above the Onondaga Valley on the west and about 50 feet above the Butternut Creek Valley on the east.
2010: What is now called "Old Stonehouse Road" used to be the continuation of Nottingham Road. It continues, on the far side of I 481, as "Rams Gulch Road" where the bridge beneath the railroad still exists. This ends at Rock Cut Road, which used to be called "The Jamesville Toll Road." The route here will get you there...

STOP 4. Rondout, Thacher, and Olney in quarry.
The quarry section is as follows:
33.5' | Olney limestone
9'
Thacher limestone
14.5' | Rondout dolomite
The Rondout and part of the Thacher are exposed in the old lower part of the quarry near the primary crusher. The main operating face is in the Olney limestone.
The Thacher here has the lithologic characteristics of the lower part of the member farther east. The contact with the overlying Olney is placed at the top of the highest zone of algal colonies and at the bottom of the lowest "drab and blue" limestone unit characteristic of the Olney.
As elsewhere in central New York, the lower Thacher exposed in this quarry is characterized by two or three zones of algal colonies and a yellow dolomite bed from about 6 inches to 3 feet in thickness. This variation in thickness appears to be due to a diastem at the top of the dolomite bed.
Subsidence structures are well exhibited in plan and section in this quarry.

STOP 5. Type section of Fiddlers Green
Turn left on the road into the Solvay Process Division's quarry property and stop at the bridge over Butternut Creek.
The Fiddlers Green dolomite has a total thickness of about 27 feet in this area. The bottom contact with the Camillus shale is exposed on the east side of the gorge several hundred feet down stream from the bridge. The top contact is not exposed, but the mudcracked beds near the bridge probably are close to the top of the member.
Ostracodes are numerous in a few thin layers, other fossils are rare.
Eurypterids have been found in the top beds in other local ities.

STOP 6. Old gypsum quarries
Park at bend in road and walk 250 feet south to the roadway into the north quarry. This quarry exposes the upper part of the Scajaquada (Forge Hollow) gypsum member overlain by the Williamsville (Oxbow) impure dolomite member and the lower part of the Cobleskill dolomite.
Walk back to the entrance of the quarry and go southeast up the hill to the west side of the south quarry. Here there is an exceptionally good opportunity to observe the top of the Scajaquada member, all of the Williamsville member, and the lower half of the Cobleskill formation. A composite section of the north and east sides of the quarry is as follows:
17' Cobleskill (to top of east side of quarry)
2.5' | dolomite with numerous closely spaced fractures in the plane of the bedding. A few stromatoporoids.
10' | Stromatoporoid biostrome. Numerous partly silicified undolomitized stromatoporoids in dolomitic limestone. Some small horn corals, tabulate corals, ostracodes, and small fossil fragments. This is the only locality where this biostrome is known near Syracuse, elsewhere the Cobleskill is completely dolomitized and only a few silicified stromatoporoids remain.
4.5'
Mottled dolomitic limestone with abundant small fossil fragments and some small horn corals. This unit also is not known elsewhere in the Syracuse area.
17' Bertie formation
6' | Williamsville member - thin to medium-bedded argillaceous dolomite
11' | Scajaquada member -
| 8.5' | Thin-bedded argillaceous dolomite with 30% or more collapse breccia due to solution of interbedded salt or gypsum
| 2.5' | Top of dark brown bedded gypsum. The gypsum is reported to attain its maximum thickness of 60 to 65 feet in this area.
The location of the contact between the Williamsville and Scajaquada members is uncertain and is one of the problems to be considered at this stop.
A cross-section of a small subsidence structure is well exposed in the northeast corner of the quarry.

STOP 7. Onondaga and Manlius formations. (Lunch Stop)
The remarkable abandoned waterfall and plunge basin in this park were formed by a river that drained a glacial lake in Onondaga Creek Valley to the west when glacial ice blocked the drainage to the north.
The lip of the falls is on the Edgecliff member of the Onondaga limestone. The Nedrow and Moorehouse members are exposed nearby at higher elevations and are at the edge of the plunge basin on the north side.
This is the type locality for the members of the Manlius formation. These and other members of the Manlius, except the Thacher is covered, are well exposed along which the stairway on the south side of the plunge basin. The section here is as follows:
Onondaga limestone Clark Reservation and Jamesville
17 to 18' | Edgecliff member, 2' of sandy limestone and calcareous sandstone at base.
--- disconformity ---
Manlius limestone formation
5'9" | Pools Brook member, dolomitic limestone
19' | Jamesville limestone, numerous stromotoporoids in upper 8 feet.
3'13" | Clark Reservation oolitic limestone
9'10" | Elmwood dolomite and dolomitic limestone member
| 2'7" | Elmwood C argillaceous dolomite submember
| 2'9" | Elmwood B dolomitic limestone submember
| 4'6" | Elmwood A argillaceous dolomite submember
22' | Olney limestone to bottom of exposure

Roadcut in Manlius fm
Road cut on left in the upper few feet of the Rondout dolomite and the Thacher and Olney limestone members of the Manlius. Some unusually large algal colonies are present in the Thacher in a zone about 3 feet thick.

STOP 8. Penitentiary quarries
The two Onondaga County penitentiary quarries provide exceptionally good exposures of most of the Manlius and Onondaga limestone formations. Also a thrust fault can be seen in the upper quarry.
The stratigraphic section of the quarries is as follows:
Onondaga limestone formation
5' | Seneca limestone member (To top of quarry).
24' | Moorehouse limestone member
13' | Nedrow limestone member
23' | Edgecliff member including 4.5 feet of sandstone at the base (Springvale sandstone bed).
--- disconformity ---
Manlius limestone formation
7'3" | Pools Brook limestone member
22'2" | Jamesville limestone member
3'3" | Clark Reservation limestone member
11'4" | Elmwood member
| 3'6" | C submember
| 3'0" | B submember
| 4'8" | A submember
19' | Olney limestone member
The strata exposed in the lower quarry range from the lower part of the Olney member to the bottom 1-foot of the Pools Brook member. The main floor of this quarry is at the top of the Olney limestone with a few inches of the bottom of Elmwood A dolomite in places. The Elmwood A and C submembers are distinguished by their yellow brown weathering color, the Clark Reservation limestone by its very light gray weathering color and diagonal fractures, and the Jamesville limestone by the massive stromatoporoid biostrome that constitutes its upper half.
Most of the Pools Brook member and the overlying sandstone (Springvale sandstone bed of the Edgecliff member) are exposed in the stripped area between the two quarries. The Pools Brook is easily recognized by its thin bedding and sparseness of fossils. The Springvale sandstone is brown and contains scattered black phosphatic nodules.
The upper quarry is entirely in the Onondaga limestone. Most of the floor is on the top of the Springvale sandstone. On the downthrown side of the thrust fault, at the north side of the quarry, the floor is in the lower part of the Moorehouse limestone member. The middle and upper parts of the Moorehouse member are most accessible for examination on the downthrown side of the thrust fault at the north side of the quarry, where loosely coiled cephalopods of the Halloceras bed are exposed on the floor. Oliver (1954, G.S.A. v. 65) designated this quarry as the type locality of the Moorehouse member. He derived its name from Moorehouse Flats nearby. The Seneca member is poorly represented in the quarry. All but a few feet has been eroded.
The Edgecliff member contains numerous rugose and tabulate corals and much crinoid debris including some unusually large columnals. It is most easily seen at the west end of the north side of the quarry. The Nedrow member also is most accessible here.
The reverse fault on the north side of the upper quarry strikes about N 70 W, dips about 20 degrees south, and has a throw of 31 feet. It is complicated in places by multiple slip planes, drag, and crushing. Small veins in north-south joints near the fault contain calcite, dolomite, fluorite, quartz, and a solid hydrocarbon. These are best seen in the Olney limestone of the lower quarry.

STOP 9. View to the South
View to south of the stripped surface on the Onondaga Limestone which forms a prominent bench about 150 feet above the bottom of Butternut Creek Valley. The Marcellus and Skaneateles formations of the Hamilton Group form the steep slopes to the southeast.

STOP 10. Coral Bioherm in Onondaga Limestone
Taylor Road crosses a coral bioherm here. Most of the exposures are in the wooded tract on the west side of the road. This is the only bioherm known in the Onondaga Limestone in the Syracuse area. Usually these bioherms start in the Edgecliff member and, if thick enough, extend upward into higher members. In the absence of exposures of the adjacent limestone, it is not possible to determine the stratigraphic range of this bioherm, but it appears to extend well up into the formation.

Thrust fault
A thrust fault, which strikes about N 70 W, dips about 20 degrees south, and has a throw of 42 feet, crosses Route 173 near this road junction. Formerly it was exposed in one of the old quarries that are now filled. Present exposures east of the road junction show the Onondaga and Manlius limestones offset by the fault.

Onondaga outcrop
Outcrop of Onondaga limestone at edge of road on left.

Subsidence structure
Subsidence structure in Onondaga limestone in field on left. Exposed beds have an anomalous dip west because of this structure.

Smoky Hollow cross channel
Road crosses west end of Smoky Hollow cross channel at an altitude of about 780 feet. This is the southernmost of the well-developed cross channels eroded between Onondaga Valley and Butternut Creek Valley by the outflow from glacial lakes in Onondaga Valley. The channel was eroded in Marcellus shale down to the more resistant Onondaga limestone.

STOP 11. View of Onondaga Creek Valley
Some of the topographic, glacial, and stratigraphic features of this part of the valley will be pointed out at this stop.

Onondaga limestone roadcuts
Turn left (S) on Kennedy Road. Road cuts on the new divided highway (Route 81) to right are in the Edgecliff and Nedrow members of the Onondaga limestone. The road cuts on Kennedy Road are in the Moorehouse member and the top few feet of the Nedrow member.

STOP 12. Top of Onondaga and thrust fault
STOP 12. Top of the Onondaga limestone and Union Springs shale displaced by a small thrust fault. The upper 8 feet of the Onondaga limestone and about 10 feet of the Union Springs shale are exposed on the side of the deep drainage ditch on the east side of the road. Exposures of the top contact of the Onondaga such as this are rare. At the south end of the drainage ditch a thrust fault with a throw of about 5 feet cuts the top of the Onondaga but is absorbed in the Union Springs shale above by complex crumpling and jointing.

STOP 13. Manlius and Onondaga fms.
The stratigraphic units exposed in the road cut are as follows:
Onondaga limestone formation
11'6" | Moorehouse limestone member (to top of exposure)
11-12' | Nedrow limestone member
12'8" | Edgecliff limestone member
--- disconformity ---
Manlius limestone formation
10' | Pools Brook limestone member
18' | Jamesville limestone member
4' | Clark Reservation limestone member
9'10" | Elmwood dolomite and dolomitic limestone member
| Elmwood C (only the top few inches exposed)
The lowest part of the section is at the north end of the cut where the top few inches of Elmwood C, the Clark Reservation, and the Jamesville are exposed.
This stop provides an opportunity to compare the stratigraphic units with the same units seen at the Penitentiary quarries (stop 8) 4 miles northwest. Most of the units are similar, but one significant difference at this stop is the absence of the Springvale sandstone bed at the base of the Edgecliff member and another is the presence of a bed with stromatoporoids and favositid corals at the top of the Pools Brook member. This bed has a small erosion surface at its base suggesting that it might correlate with the Bishop Brook limestone exposed on the hill northeast of Manlius, which is in a similar stratigraphic position and also has an erosion surface at its base. However, the bed appears to resemble the Jamesville more closely than the Bishops Brook both faunally and lithologically.
Inclined joints are well developed in the Nedrow member on the south side of the exit road from Route 81. Many of these are limited to certain beds and end upward against prominent shaly partings. They also are numerous in the Manlius at the north end of the road cut where the beds are slightly arched.

STOP 14. Type locality of the Nedrow member.
Indian Reservation quarry in the Onondga limestone, the type locality of the Nedrow member. This quarry formerly was worked for building stone.
The stratigraphic units exposed in the quarry are as follows:
Onondaga limestone formation
15'19"' | Seneca limestone member (To top of quarry).
18'6" | Moorehouse limestone member
11-12' | Nedrow limestone member
12'0" | Edgecliff limestone member (base not exposed).
The main floor at the south end of the quarry is at the top of the Edgecliff member. The south face exposes the Nedrow, Moorehouse, and Seneca members. The Tioga bentonite bed (8" to 9" thick), which Oliver (1954, Bull. G.S.A., v. 65) uses as the boundary between the Moorehouse and Seneca members, can be seen in the upper part of the face where it forms a reentrant a few inches above a 4-inch layer of black chert.
The best fossil collecting is on the main floor of the quarry where brachiopods, corals, bryozoa, and crinoid debris, including segments of unusually large columnals, are abundant.
Climb up the south side of the quarry to observe the Tioga bentonite and the Seneca member at the top. A zone of pink chonetid brachiopods is exposed about 2 feet below the highest beds at the edge of the stripping.
Walk east to the fence on Route 81 to observe the Union Springs shale and the Cherry Valley limestone exposed in a new road cut.

Marcellus Shale
Ravine in Marcellus shale on left a short distance west of the County Home.

STOP 15. Quarries in Manlius and Onondaga limestones
Split Rock quarries in the Manlius and Onondaga limestones. Park in old part of quarry at end of road and walk east into the easternmost quarry in the Manlius. The Edgecliff member of the Onondaga limestone can be seen in this quarry to rest disconformably on Elmwood A bed of the Elmwood member. The 33 feet of limestone between the Elmwood A bed and the Rondout dolomite exposed on the floor of the quarry, is considered to be the Olney member of the Manlius formation by Rickard (1962, N.Y.S. Mus. Bull., 386). The bottom 5 feet of this limestone, however, has beds characteristic of the lower part of the Thacher limestone member to the east. These beds will be examined in an attempt to evaluate their significance in resolving the problem of the "disappearance" of the Thacher. End of Trip

D: GEOMORPHOLOGY OF THE NORTH MARGIN OF THE APPALACHIAN UPLANDS NEAR SYRACUSE
Surficial Geology of the Syracuse Field Area
Ernest H. Muller

Start

Meltwater channel
Cross meltwater cross channel utilized as corridor by N.Y. Central R.R., Erie Boulevard and formerly by Erie Canal. Channel is below main Iroquois lake level and auguring shows peat and marl over fine sand and clay, underlain by coarse alluvium, suggesting rise of Iroquois waters into meltwater channel, followed by swamp development in poorly drained basin left after Iroquois extinction.

Sharp Slope on Syracuse Formation
Crossing Erie Boulevard at traffic light, proceed S on Thompson Rd. rising onto sharp slope developed on Syracuse Formation.

Thin till
Turn right (W) onto Salt Springs Rd. over drumlinized upland developed on thin till over Syracuse shales.

Meadowbrook Meltwater Channel
Continuing SW on Meadowbrook Drive, follow meltwater channel to its end in "t-intersection"

Rock Cut road
On left, railroad cut exposes section in Fiddlers Green dolomite which forms floor of flat-bottomed, steep-walled Rock Cut or Railroad Channel leading east from this point. With its threshold at 550-ft. this is one of several major meltwater channels which controlled eastward escape of water from lakes impounded in central New York through valleys, between the northward receding margin of the ice sheet and the plateau divides to the south.

Rise at Elmwood Formation
In .2 mile rise sharply over scarp developed on Manlius Group, with Elmwood Formation exposed at left near bench edge.

Onondaga trough
Descend to floor of Onondaga trough over strata of Manlius Group. Cross U.S. Rte. 11 (Salina St.) and Onondaga Creek.
Near Onondaga Lake, about 3 miles north, the bedrock floor of Onondaga trough is 417 ft. below the surface or about 25-ft. below sea level.

Dorwin Springs Bench
Near Dorwin Springs, road ascends onto gravel bench, dissected and with low constructional topography. At right (W) massive Onondaga Limestone supports narrow benches on the valley wall. At left (E) the gravel bench is about at level of the threshold of Rock Cut Channel on opposite side of the valley.

STOP 1 Saunders Gravel Pit
Discussion of character and structure of gravel bench in its relationship to Onondaga Trough history

Cross Commissary Creek
Cross Commissary Creek which dissects end of 560-ft bench

Bench at 620 ft
Ascend onto bench at approximately 620 ft.

Rise to 720 ft bench
Continue west on Johnny Cake Rd., leaving N.Y. Rte 80 at Griffins Corners. Rise to level of 720-ft. bench. Cross Onondaga Hill Rd. then descending toward Nichols Corners, note sand and gravel exposures on left (S).
2009: Perhaps Rte 80 used to go through South Onondaga, and Tanner Road used to be called Johnny Cake Road?

Nichols Corners
At Nichols Corners, turn right onto Cedarvale Rd. Just before turning note red clay till in stream bank at left (S).
Proceeding NW on Cedarvale Rd. follow Cedarvale meltwater channel. Note constructional topography due to deposition from stagnant, debris-littered ice on slope at right (NE).

Benches at 680 and 800 ft
Turn left (S) onto Amber Rd. and proceed across gravel bench at 680 ft. msl, with sharp rise to bench above 800 ft. msl on right.

STOP 2 Cedarvale Gravel Quarry
Composition and structure of the gravel bench in relationship to Cedarvale Channel and Onondaga Trough history

View of Delta Remnant in distance
Continuing on Amber Rd. turn sharply south and continue ascent. Note flat-topped mesa-like delta remnant on left (E) at 800 ft. msl. near South Onondaga.

Navarino Channel
On right (W) note head of sizable meltwater channel, the Navarino Channel by which glacial meltwaters escaped southward into basin of Otisco Lake.
Continue through area of moderate constructional topography deposited by stagnant ice. Note Navarino Channel paralleling Amber Rd.

Head of meltwater channel
At Joshua Corners, on right (SW) note level swampy area at head of minor meltwater channel which contributed to complex Amber delta deposited into a predecessor of Otisco Lake, 3 miles SW.

Bioherm in the Spafford Shale
Turn right (S) at Lords Corners, onto Lords Hill Rd., N.Y. Rte. 80. Ascend over Hamilton section, near summit passing biohermal zone in Spafford Shale, rich in rugose corals, overlain at top by Owasco shale. When not tar-concealed by Highway Department these gullies afford fine collecting.
Descend and cross open, marshy east-west valley. To left (E), Fall Ck. flows to Rattlesnake Gulf. To right (W) stagnant ice features comprise divide between 0tisco and Onondaga drainage basins.

Glacial Trough
Descend SE along trough like glacial furrow occupied by headwaters of Onondaga Creek.

Tully moraine belt
Cross Onondaga Creek. Enter complex Tully moraine belt where minor ridges project into this tributary trough with curvature convex to the northwest. At Fellows Falls, Onondaga Creek drops with hanging and barbed juncture into Onondaga trough, in this area called Tully Valley. To the left ahead (NE) local reIief exceeds 1250 ft. from upland to trough floor on proximal (northern) flank of massive Tully (Valley Heads) moraine. The abrupt proximal border and gently graded distal slope of this moraine is characteristic of valley-blocking moraine loops of this system in central New York.
Seismic refraction profiles suggest that the unconsolidated valley fill in mid-trough opposite Fellows Falls may be 400 to 500 ft. thick with the bedrock floor at 300 to 400 ft. msl.

STOP 3 Green Lake (Tully Lakes)
Examination of features and materials of pitted outwash plain. Discussion of significance in terms of Valley Heads and Onondaga trough glacial history.
Proceed east toward Tully.
2009: With Interstate 81 in the way, Lake Road no longer continues East here. The path gets us to Tully just the same.

Kame and kettle
Leave N.Y. Rte. 80. Continue south along west wall of Onondaga trough. On right Moscow shale exposed in trough wall. On left, Tully moraine with strong kame and kettle topography. Southward the kames diminish in relief and grade into kame terrace. Crooked Lake at left occupies a compound kettle.

Leave outwash plain
Leave outwash plain and ascend onto upland developed on Ithaca and Sherburne Formations.

Kettle Dotted Outwash Plain
Turn left (E) across kettle-dotted outwash plain. Stagnant ice of the Tully ice tongue extended about one mile south of this route to an "advance Valley Heads" position, before receding 3 miles north to the massive "main Valley Heads" position. The position of this moraine complex has been ascribed to bedrock topographic control at the former drainage divide. Seismic data at Tully Lake suggest depth to bedrock of about 225 ft.

Enter distal margin of Tully moraine
Enter distal margin of Tully moraine. For next 2 miles constructional topography is strong, diminishing gradually on proximal edge of moraine.

Butternut Creek trough
At traffic light in Lafayette, turn right (E) onto U.S. Rte 20, Cherry Valley Turnpike. In.2 mi. turn left (N) onto Lafayette Rd. The gently curving, partly drift-filled trough of Butternut Creek is visible ahead on right, with U.S. Rte 20 swinging across at Big Bend.
Crossing the upland, bedrock ridges, such as Irish Hill on right (E) are streamlined, gently molded and parallel to lineation of drumlins a few miles to the north.

Drumlin field
Pass Bull Hill Rd. Drumlins on left (W) are composed of bouldery, lime-rich lodgment till. Alignment is N5W, as compared to N30W in outskirts of Syracuse. Artificially impounded Jamesville Reservoir on right (NE) ahead.

STOP 4 Horseshoe or Loop Channel
Consideration of nature of Smoky Hollow and the Loop umlaufberg, and of their significance with respect to late Cary glacial recession.
Continue north on Barker Hill Rd. Descend onto terrace that blocks upstream end of the Loop. Roadcut at the terrace edge exposes rhythmically laminated lake sediments. The eastern arm of the Loop contains kame gravels.

Smoky Hollow
Cross Smoky Hollow, part of a major meltwater channel with bedrock floor just below 800 ft. msl. Sharply incised into non-resistant Hamilton shales, this outlet may have controlled drainage of impounded waters in Onondaga trough at level of highest delta in Cedarvale Channel. Note that drumlin on right (E) is truncated by wall of Smoky Hollow, indicating that channel cutting postdated final drumlin moulding. Continue north on Barker Hill Rd.

Descend onto Onondaga bench
Descend from drumlinized Hamilton upland onto channeled Onondaga bench.

STOP 5 Clark Reservation
Examination of features due to erosion by glacial meltwater, solution by underground water and joint control as developed near Green Lake and along south wall of Rock Cut Channel. Discussion of significance in terms of interpreted history of glacier recession.
Return to N.Y. Rte 173 and turn left (E) toward Jamesville.
On left (N) of road note deep channel leading east from Green Lake to Butternut trough.

Fiddlers Green Dolomite
Cross tracks and turn left (N) onto Jamesville Rd. which parallels Butternut Creek. Below falls, in .2 mi. Butternut Creek exposes type Fiddlers Green dolomite.

Rock Cut view and Rams Gulch
At fork bear right, continuing N on Jamesville Rd. Descend to floor of Butternut trough. Cross Butternut Creek and the eastern or outlet end of Rock Cut Channel is visible on left (W), notched by narrow post-glacial Rams Gulch.

Alluvial Plain of Iroquois Lake
Recross Butternut Creek on alluvial plain at approximate level of Iroquois Lake which may have inundated lower end of valley as a consequence of isostatic upwarp northward. Rise onto trough wall and proceed north.

E: STRATIGRAPHY OF THE HAMILTON GROUP IN THE SYRACUSE AREA
Newton E. Chute and James C. Brower

E: STRATIGRAPHY OF THE HAMILTON GROUP IN THE SYRACUSE AREA

View of hills in the Marcellus and Skaneateles fms ahead.

Drumlin and scarp
Drumlin on the left and a scarp in the Manlius and Rondout formations on the right.

Entering Rock Cut Channel.
This large cross channel was cut during the recession of the glacial ice by the drainage from a glacial lake in Onondaga Valley to the west.
2010: What is now called "Old Stonehouse Road" used to be the continuation of Nottingham Road. It continues, on the far side of I 481, as "Rams Gulch Road" where the bridge beneath the railroad still exists. This ends at Rock Cut Road, which used to be called "The Jamesville Toll Road." The route here will get you to the next stop...

Cobleskill and Roundout fms
Road cut on right in the Cobleskill and Rondout dolomite formations. The Cobleskill is thicker bedded and is composed of purer dolomite than the Rondout.
DEC site 416

Bridge over the D. L. & W. Railroad.

Stone crusher building
Junction of Jamesville Toll Road and Jamesville Road. The stone crusher building of the Solvay Process Division of the Allied Chemical Corporation can be seen on the hillside to the left.

Edgecliff member
Exposure of the Edgecliff member of the Onondaga limestone on the left near top of grade.

Cherry Valley member
Small exposure of the Cherry Valley limestone member of the Marcellus formation in road cut on left near top of rise.

View of the Solvay Process Division Quarry on left.

STOP 1. Monocline in the Onondaga
STOP 1. Monocline in the Onondaga limestone and exposures of the Union Springs shale, Cherry Valley limestone, and Chittenango shale members of the Marcellus formation.
Walk south up the stream for about 500 feet to where the top beds of the Onondaga limestone exposed in the stream bed dip northward due to the presence of a monocline that strikes about N 70 W. This monocline probably grades into a thrust fault in the Solvay Process Divisionis quarry. Solution-widened tension joints are well-developed in the limestone on the monocline.
Continue up the stream to where it forks. About 15 feet of Union Springs shale and about 3 feet of Cherry Valley limestone are exposed at a small waterfall on the left branch not far from the fork. The Union Springs consists of black shale with numerous thin beds of black limestone. Styliolina fissurella, a small mollusc shaped like a penci point, is common in the shale of the upper part of the member. The Cherry Valley limestone forms the lip of the falls. This member is noted for cephalopods and one or more may be seen in the stream bed at the top of the falls. The basal few feet of Chittenango shale, exposed in the stream bank above the falls, contains one or more thin beds of black limestone. Numerous styliolina fissurella can be seen on the bedding surfaces of some of the shale.

Small waterfall on the left branch not far from the fork

STOP 2. Chittenango and Cardiff shales.
This shale is quarried by the Alpha Portland Cement Company for use in cement manufacture at its Jamesville plant. The upper bench is in the upper 40 to 50 feet of the Chittenango shale member of the Marcellus formation.
Although these shales are similar in appearance, they can be distinguished easily by their streaks. The Chittenango shale, because of its relatively high content of carbonaceous matter, streaks brown when scraped by a hard object such as a geologic hammer, whereas the Cardiff streaks light gray. Examination of drill core from several test holes has shown that the change in color of the streak takes place within a vertical interval of 3 feet. The contact is placed where, in going downward, the streak becomes distinctly brown. Located this way, the contact is near the top of the lower face, 5 to 6 feet above the upper layer of large septarian concretions.
Many of the septarian concretions in the upper part of the Chittenango are several feet across. The Cardiff shale on the other hand has only a few concretions and these are seldom more than 6 inches in diameter. The cracks within the septarian concretions commonly contain calcite, ferroan dolomite, and white, platy barite. Small crystals of barite with some pyrite also coat joint surfaces in the shale in places.
Fossils are sparse or lacking in most of the Chittenango and Cardiff shales, but one or more zones near the top of the Chittenango contain numerous carbonized plant remains and a few fish scales, fish body plates, pyritized straight cephalopods, and small brachiopods. Because the shale tends to break down into small pieces after exposure for a few months, the success of fossil collecting depends on the recency of quarrying in the fossil zones.

Centerfield member in road cuts.

STOP 3. Butternut member
Road cuts and small quarry in the upper part of the Butternut member of the Skaneateles formation.
About 40 feet of the upper Butternut is exposed in the small quarry and road cuts nearby. Most of the exposure consists of shale with thin siltstone layers and silty shale that increase upward. The top 5.5 feet in the quarry is siltstone. This siltstone and the silty shale below contain some brachiopods particularly Leiorhynchus sp. The lowest beds exposed in the road cut are poorly fossiliferous shale that splits into thin flat pieces "paper shale", a characteristic of the shale of the middle and lower parts of this member.

STOP 4. Platform of Staghorn Point biostrome.
Stop opposite the yellow brick house. Walk about 100 feet up the hillside on the west side of the road to exposures of siltstone strata that form a bench on the hillside. This is the siltstone platform on which the Staghorn Point coral biostrome was formed. It is about 50 feet above the base of the Otisco member of the Ludlowville formation and is an important horizon marker in Syracuse area. The exposed section here is as follows:
Ludlowville formation - Otisco member
8" | siltstone bed with numerous molds of corals in bottom 2 inches
3'0" | covered
4'10"
siltstone platform with several thin discontinuous fossil-rich layers. Base not exposed but total thickness of siltstone probably about 6 feet.

STOP 5. Delphi Station and Pompey members.
Observe the upper beds of the Pompey member exposed near the top of the falls. Walk right on path along the edge of the gorge to where the falls can be observed.
The top 60 feet of the falls is Cooper's (1930, Am. J. Sci. v. 19) type section of the Pompey member. The resistant siltstone beds that form the lip of the falls are his  Eunella-Nyassa zone that marks the top of the Pompey, distinguished by the presence of  Eunella lincklaeni, Athyris cora, and  Nyassa arguta. The lower part of the falls exposes the upper part of the Delphi Station member. The Mottville limestone member which underlies the Delphi Station member is exposed a moderate distance downstream from the falls.
DEC sites 347, 348

Small shale quarry
Small shale quarry in the Butternut member of the Skaneateles formation on the right side of the road.

STOP 6. Pompey and Delphi Station members
Road cut in the Pompey and Delphi Station members of the Skaneateles formation.
This cut exposes about 115 feet of the Pompey and Delphi Station members. The 8 feet of siltstone at the top of the cut is Cooper's Eunella-Nyassa zone that marks the top of the Pompey, the same unit that forms the lip of Pratts Falls. This siltstone grades downward into gray shale.
The contact between the Delphi Station and the Pompey members is not easily located and is one of the problems to be considered at this stop.

Butternut member
Road cut on the left in the Butternut member of the Skaneateles formation on road connecting Routes 81 and 20.

STOP 7. Lower part of the Centerfield
Lower part of the Centerfield calcareous siltstone member of the Skaneateles formation.
Walk a short distance north from Route 20 to the waterfalls on the lower part of the Centerfield. The deep ravine below the falls is in the Butternut shale member of the Skaneateles formation.

STOP 8. Centerfield member.
Walk southeast about 200 feet to the stream where the Centerfield member forms a waterfall. Most of the Centerfield is exposed here, and the upper part with calcareous concretions is accessible for close observation. The gradational nature of the bottom contact of the Centerfield with the Butternut member can be seen on the side of the falls. The total thickness of the Centerfield is not closely determined in this area, but may be about 30 feet.
One of the noteworthy features here is the joint controlled cleft at the top of the falls through which the stream flows.

STOP 9. Joshua Coral Reef
Joshua Coral Reef in the Otisco shale member of the Ludlowville formation.
This is the famous Lords Hill locality described by W. A. Oliver, (1951, Amer. Jour. Sci., p. 705-728). The coral bed is estimated to be as much as 50 feet thick in this area and to be about 90 feet above the bottom of the Otisco Member. The exposure was much better before the road ditches were coated with blacktop, but some of the corals can still be seen and collected. According to Oliver, the most common genera of rugose corals here, in order of abundance, are: Cystiphylloides, Siphonophrentis, Bethanyphyllum, Heliophyllum, and Heterophrentis. In addition the colonial rugose form Eridophyllum and several species of Favosites are present.

Ivy Point siltstone member
Small exposures of the Ivy Point siltstone member of the Ludlowville formation on both sides of the road. The Ivy Point forms benches in this area.

STOP 10. Owasco, Portland Point and Windom members
Road cut in the Owasco member of the Ludlowville formation, and the Portland Point and Windom members of the Moscow formation.
Moscow formation
1'6" | Windom shale member (to top of exposure)
9'1" | Portland Point member
| 7'6" | shale and thin interbedded fossilrich limestone layers
| 1'7" | impure limestone, fossiliferous
Ludlowville formation
2'3" | Owasco siltstone member
2'0" | Spafford shale member (to base of exposure)
The Portland Point member, according to Cooper (1930), consists of 1 foot of crinoidal limestone overlain by 8.5 feet of calcareous shale with interbedded thin layers of limestone. At this locality the basal limestone is a little thicker, and thin beds of fossiliferous limestone are present in the overlying shale for about 7.5 feet above the limestone. Because of the indefiniteness of the position of the upper contact, the amount of Windom present in this exposure, if any, is uncertain.

STOP 11. Tully limestone.
Small exposure of the upper part of the Tully limestone on the south side of the road opposite a red barn. Walk down the hill to the east a short distance and turn into the old quarry in the Tully limestone on the north side of the road. The top 5 feet of the quarry is the West Brook member below which is 10 feet of the Apulia member. The contact between them is placed at the bottom of the nodular limestone of the West Brook. The Tinkers Falls member is not exposed. Fielding (1956, MS thesis, Syracuse Univ.) estimates the total thickness of the Apulia member to be 18 feet and the West Brook member to be 9 feet in the South Onondaga quadrangle.
The Apulia member contains crinoid fragments, ostracods, and brachiopods particularly Hypothyridina venestula. The coral Lopholasma is characteristic of the West Brook member. In addition, Fielding (1956) reported finding Metriophyllum tullium, Elytha fimbriata, Phacops rana, Tornoceras uniangulare and crinoid fragments.

STOP 12. Windom member of Moscow fm.
About 20 feet of the top part of the Windom shale member is exposed in the road cut on Kingsley Road. The shale becomes silty near the top of the exposure and is sufficiently resistant to have formed a bench about 500 feet wide. A few small calcareous concretions can be seen in this exposure and enough pyrite is present to cause considerable limonite staining. Brachiopods, pelecypods, and trilobites are present, but are not abundant. End of trip.

GUIDEBOOK TO FIELD TRIPS
Philip C. Hewitt and Leo M. Hall
Editors
Contributing Authors
Donald W. Fisher*
Yngvar W. Isachsen*
Philip C. Hewitt
Robert G. LaFleur
William E. McClennan
Harold Nilsson
Host
UNION COLLEGE
Schenectady, N. Y.
April I-May 2, 1965
* Published by permission of the Assistant Commissioner, New York State Museum and Science Service.

A: MOHAWK VALLEY STRATA AND STRUCTURE
Saratoga to Canajoharie
by Donald W. Fisher
State Paleontologist
New York State Museum & Science Service
"The crust of our earth is a great cemetery, where the rocks are tombstones, on which the buried dead have written their own epitaphs".
Agassiz

A: MOHAWK VALLEY STRATA AND STRUCTURE

Normanskill Graywacke
Outcrop of Middle Ordovician Normanskill Graywacke and Shale along east (northbound) lane. This is the westernmost extent of a large area of Normanskill, interpreted as a thrust outlier of the Taconic Allochthon or as a north-trending anticline protruding from beneath a cover of younger rocks.

Crossing Mohawk River
These dual tied-arch bridges won an award in 1958 for their design.

Former channel of the Mohawk River.
Crossing former channel of the Mohawk River. To the east, Round Lake occupies a portion of this now abandoned channel.

Snake Hill Shale
Long exposure in Middle Ordovician Snake Hill Shale, a dark gray silty facies of the Canajoharie Shale of the Mohawk Valley.

STOP 1. Lester Park
This is the type section for the Late Cambrian Hoyt Limestone, noted for its biostromal reefs of colonial algae called  Cryptozoon (see Fig. 9, Plate 1). The lowest reef has been planed by glacial erosion revealing the algal heads in horizontal section; a higher reef, in the recently enlarged road cut, exhibits a vertical section of  Cryptozoon. A still higher reef in the abandoned Hoyt Quarry displays a reef of algal mats rather than heads. Between the lowest and middle reefs is a coarse-grained dolomitic limestone with oolites and trilobite fragments; the genera  Prosaukia, Saratogia, Plethometopus, Plethopeltis, and  Dikellocephalus have been collected here, thereby establishing a Trempealeau age.
DEC Links 1 2 3

Petrified Gardens and Old Quarry
On left (east.) is entrance to Petrified Gardens, a privately owned exhibit of the Hoyt Limestone and its  Cryptozoon reefs. On right is old quarry in the Ritchie Limestone, either a local facies of the Hoyt or a slightly younger unit. Its rare fossils (the gastropod  Rhachopea) are not diagnostic. An east-trending normal fault separates this quarry from Lower Ordovician Gailor Dolomite on the downthrown, southern side.
DEC Links 1 2 3

STOP 2 ROCK CITY FALLS stratigraphic section.
In addition to studying several rock units here, there is a fine display of the Lower Ordovician-Middle Ordovician unconformity (disconformity) between the older Gailor Dolomite forming the face of the falls and the Amsterdam Limestone. The falls marks a fault-line scarp, upthrown on the west. The downthrown block exhibits Middle Ordovician Larrabee Limestone beneath the road bridge, some 70 feet lower than in the quarry on the upthrown block.

Glacial features
Morainal pond on north side of road; extensive cover of glacial sand and gravel in this region.

STOP 3
Basal Paleozoic cobble conglomerate consisting of quartz cobbles, derived from a Precambrian quartzite atop the hill to the north, in a siliceous, pyritic matrix. Midway in the exposure is some coarse textured, bedded, quartzose sandstone. This entire unit has been called Potsdam in the past because of its basal position and subjacency to the Theresa Formation, which crops out along the road to the west. Lithologically it is atypical for Potsdam; it seems to be a talus deposit, probably formed at the base of a sea cliff in Late Cambrian time., Precambrian biotite-gneiss may be uncovered by digging beneath this basal Paleozoic conglomerate.

Theresa Formation
Road cut in Theresa Formation, a unit with alternating quartzose dolomites and dolomitic sandstones with occasional golf-ball size quartzite pebbles.

Fault-line scarp
Climb fault-line scarp; this is the northern extension of the Hoffmans Fault, the most easterly of the Mohawk Valley normal or step faults.

Cliff of Little Falls Dolomite, upthrown side
Intersection with West Galway Road, proceed straight ahead. Cliff of Upper Cambrian Little Falls Dolomite on upthrown side of fault parallels road on the right.

Larrabee Limestone, downthrown block
Middle Ordovician Larrabee Limestone along road, on right, opposite old cemetery. This is the eastern downthrown block. Scarp veers southwestward.

There are two normal (gravity) faults here, both downthrown on the east with a small fault block (horse) caught between them (see Fig. 11, Plate 1). The eastern block shows steep east-dipping Larrabee Limestone with included round pebbles of a black, fine-grained, limestone (Amsterdam?) dragged against slightly westward dipping fine-grained, tan-gray, white weathering Lowville Limestone. The Lowville within this horse is overlain directly by the gray, coarse-grained Larrabee Limestone; the Amsterdam Limestone is missing from its accustomed position between the two in the Lower Mohawk Valley. Like all other horses observed by me, this one dips north or reverse from the regional dip. The west block exposes nearly horizontal Little Falls Dolomite.

Hoffmans fault
LEAVE horse, continue west on town road, crossing main branch of Hoffmans Fault.

View of Mohawk Valley to the SW
Atop hill, good view of Mohawk Valley to the southwest, looking down dip.

Underlain by Little Falls Dolomite
This region underlain by Little Falls Dolomite.

Little Falls Dolomite
Long road cut in Little Falls Dolomite (both sides of road). Quartz crystals and chert are absent here although we are less than 50 feet below the Tribes Hill Fm.

Pre-glacial valley
Lower area to west is the course of a pre-glacial valley, tributary to the Mohawk.

Hoffman's Fault
Straight ahead at intersection with West Glenville Road. Outcropping of thick-bedded, coarse-grained, light gray Larrabee Limestone (with "Shoreham" fossil  Cryptolithus) on lumpy-bedded, fine-grained, dark gray to black Amsterdam Limestone on southwest corner. This is the fault-line scarp of the Hoffmans Fault.

WOLF HOLLOW and LUNCH Park on left,horse on right. The road and stream follow the fault trace of the Hoffmans Fault which, here, has a vertical displacement (throw) of at least 1000 feet and very probably as much as 1600 feet (see Figure 8). The downthrown (east) block exposes Middle Ordovician Schenectady Graywacke and Shale in the southern part of the Hollow and Canajoharie black shale in the northern part. The upthrown (west) block shows the Lower Ordovician Gailor Dolomite forming the impressive cliff. A small horse on the west side of the road of "Shoreham" Limestone and Canajoharie Shale dips north. Wolf Hollow well exemplifies the role exerted by faults in controlling drainage.

Fault exposure
Sharp left curve. Schenectady Graywacke and Shale dragged at a 40° angle, diminishing to less than 5° at eastern limit of exposure, some 500' distant.

Cliff
Long high road cut begins where Toureuna Road joins NY 5; lower 40' is Little Falls Dolostone and the remainder of the cliff is Gailor Dolostone. A small hill atop the cliff exhibits Lowville, Amsterdam, Larrabee, and "Shoreham" Limestones and Canajoharie Shale in their normal stratigraphic positions. Thus, the stratigraphic succession can be demonstrated conclusively in this single section.

Road cut on NY 5 at railroad overpass. The two middle members of the Tribes Hill Formation are exposed here;the massive Wolf Hollow dolomitic calcilutite (fine-grained limestone) is in contact with the thin bedded Palatine Bridge dolomitic shale and quartzose calcisiltite (medium grained limestone) and calcilutite. Note the white and buff fretwork weathering of the Wolf Hollow member with the buff dolomite in relief. The Palatine Bridge member is lighter colored and more quartzose and pyritic. A single dolomite bed, 2 1/2 feet thick, in the lower part of the Wolf Hollow member can be traced throughout the Valley; it is a bluish-gray, medium-textured dolostone with pockets (vugs) of dolomite crystals. Fossils are scarce in both members. The Wolf Hollow member has a molluscan fauna of large, loosely coiled gastropods and straight or gently curved ellesmeroceroid and clarkoceroid cephalopods. In contrast, the Palatine Bridge member has an arthropod (trilobite) and brachiopod fauna. Both faunas indicate an Early Canadian (=Tremadoc) age.

Fort Johnson
Baronial home of Sir William Johnson built in 1749 on northwest corner.

Tribes Hill Fault
Cross Tribes Hill Fault, upthrown on west.

Roadcut with weathered rock
On north side of NY 5 is a cut in the same portion of the section viewed at the previous stop. Note the change in appearance owing to longer weathering (exposed initially in 1958). When first revealed, there was a two-foot iron oxide zone at the top of the Palatine Bridge member; this corresponds to the two-foot dolomitic shale zone at the previous stop.

Parking area
Parking area, splendid view of Mohawk Valley with Schoharie Valley in distance.

On north side of NY 5, Middle Ordovician Canajoharie Shale, here more of a calcareous argillite which is typical of the lowest 200' of the formation, has graptolites (See Figure 13, Plate 1) in the upper few feet of the exposure. These extinct animals, excellent guide fossils for subdividing the Ordovician and Silurian Periods, are thought to have been floaters (plankton) and, thus, achieved wider distribution in a relatively short period of time as compared to bottom dwellers.

STONE RIDGE This is a critical section in deciphering structure and Ordovician stratigraphy in the Valley.
The three upper members of the Tribes Hill Formation are exposed (upper Palatine Bridge and Wolf Hollow in Van Wie Creek to the west of Borden Road and Fonda member in road ditch and road cut). The Chuctanunda Creek Dolostone is missing due to erosion. This is a superb example of a disconformity (See Figure 7). The older Tribes Hill Formation has been subjected to subaerial erosion and the crevices at its summit are filled, in places, with whiteweathering Lowville Limestone with vertical worm borings. Lumpy bedded limestone (Amsterdam or Larrabee ?) occurs above; the fossils are not diagnostic in distinguishing which Middle Ordovician unit crops out in this cut. Further up Van Wie Creek, undoubted Larrabee and "Shoreham" Limestones are overlain by Canajoharie Shale. In the road ditch a coarse grained limestone (calcarenite) with glauconite yields abundant fossils. Most of these are stained with iron oxide and are water-worn. Gastropods are abundant but the unusual pelecypod-like arthropod,  Ribeiria, (See Figure 14, Plate 1) exceeds all others in numbers. Trilobites, ellesmeroceroid cephalopods, and brachiopods round out the major faunal elements. Rare calyx plates of cystids and conodonts complete the known fauna.

Fonda wash plain across river
Note flat topped Fonda wash plain across river. This is an Ice Age delta consisting of water-laid gravels and sands which extends north for 4 1/2 miles and west for 3.5 miles from Fonda to the Noses Fault.

NOSES FAULT and ANTICLINE ? NONCONFORMITY or FAULT CONTACT ?
Park next to barn at intersection of Anderson and Currytown Roads, walk across bridge over Yatesville Creek through private property to rock exposures along railroad and old Erie Canal.
Precambrian garnet-biotite-gneiss brought to surface along old canal and railroad in upthrown (western) block of Noses Fault. These exposures of the basement could be due to relief of the Precambrian surface or to an anticline being upwarped slightly west ? of the Noses Fault. The basal Paleozoic rock here is the Late Cambrian Little Falls Dolostone. This Precambrian outcrop (one of five within this inlier) is capped by a one foot shaly zone rich in quartz and pyrite; some traces of gold and silver were reported by Darton (1895). Is the shaly zone fault gouge or is it residual soil atop the Precambrian? One must look to the basal Little Falls breccia to determine whether it is tectonic or sedimentary. You be the Judge! Much of the Little Falls Dolostone here is heavily chertified; quartz crystals may be found after careful search. Elsewhere within the inlier, the basal Little Falls is not brecciated but is a dolostone rich in rounded quartz grains. At the Precambrian exposure north of the river along NY 5, a six foot wide mafic dike (unmetamorphosed) cuts the older garnet-biotite-gneiss. The basal Little Falls is concealed but exposures 20 feet above the Precambrian are not penetrated by the dike. Presumably, the dike was injected during a late Precambrian (Keewanawan) orogenic episode. Very scarce lingulid brachiopods are the sole fossils discovered in place in the lower Little Falls at the Noses Inlier. A loose  Elvinia free cheek was found by me along the raIlroad in 1949. Within the Late Cambrian this would signify an early Franconian age.

Noses Fault and Yatesville Creek
Proceed south (uphill) paralleling Noses Fault. Note that Yatesville Creek's course is largely controlled by the fault.

Dragged Shale
Dragged Canajoharie Shale along road on right. Dips up to 75° E.

Ledge of Wolf Hollow Limestone
Ledge of Wolf Hollow Limestone crosses to the east of the road. Canajoharie Shale in road ditch near house. Upper Tribes Hill (Fonda), Chuctanunda Creek Dolostone and Lowville, Amsterdam, Larrabee, and "Shoreham" Limestones are missing here owing to either non-deposition or, more probably, erosion. The Canajoharie Shale, too, is but 350' thick. This area atop the Noses is considered to be the crest of the Adirondack Axis and was an effective barrier to sedimentation and faunal interchange during the Wilderness and early Barneveld Stages of the Mohawkian Series.

Look back at scarp
Looking backward, note Noses scarp extending north toward Precambrian Adirondack Mountains. Land to the east (downthrown block) underlain by Middle Ordovician Schenectady Formation. Throw of the Noses Fault here about 500'.

Largest Horst
For the next two miles we are traveling across the top of the largest horst in the Mohawk Valley.

View to Southwest
Note hills to the southwest near Cherry Valley composed of Lower and Middle Devonian strata. At Sharon Springs, 8 miles south of Canajoharie, Late Silurian Brayman Shales are in contact with Medial Ordovician Schenectady shales. A few miles west of Cherry Valley, the Medial Silurian Clinton Group intervenes between the Late Ordovician Frankfort Shale and the Late Silurian Vernon Shale. The Paleozoic section, thus, thickens markedly as one proceeds west from the Adirondack Axis. The section also thickens markedly east of the Axis but the thickening occurs within the Medial Ordovician.

Dropping off horst
Dropping off western side of the Noses horst; good view looking up the Mohawk Valley toward Fort Plain and St. Johnsville.

River alluvium
Cross Flat Creek and drive on river alluvium to Canajoharie.

Inactive quarry at eastern limit of Canajoharie on south side of NY 5-S exposes the Cambrian-Ordovician contact, i.e. Little Falls Dolostone-Tribes Hill Formation. The uppermost Little Falls Dolostone is stained red with interstitial hematite and has vugs of quartz and anthraxolite. Anthraxolite is a black mineral with 92-98% carbon with much the same composition as anthracite coal. The physical properties, however, are quite different. For example, anthraxolite does not ignite. Note that anthraxolite occupies the lower half of the vugs; the upper half is usually filled with quartz but sometimes dolomite crystals complete the cavity. Anthraxolite is believed to be a hydrocarbon residue of petroleum and to have been derived from algal reefs in the Late Cambrian seas.
The overlying Fort Johnson member of the Tribes Hill Formation is a calcitic dolostone to dolomitic calcilutite. Its scarce fossils (Ophileta, Finkelnburgia, Asaphellus) denote an early Canadian age. Because the uppermost Little Falls Dolostone here has not yielded any fossils (except the non-diagnostic  Cryptozoon we cannot be certain whether the Little Falls - Tribes Hill contact here is a paraconformity (surface of erosion but with no relief) indicating a gap ip the record or whether the subtle change from relatively pure dolomite below to dolomitic limestone above indicates continuous sedimentation from the Cambrian into the Ordovician Period. The physical clues (zone of hematite, vuggy dolomite with contained minerals) lean toward the paraconformity view (see Figure 7). The splendid long stratigraphic sections along Flat and Canajoharie Creeks cannot be examined by large groups. They are, however, critical in reconstructing the geologic history of the Valley and are accordingly included in Figure 3.

Water Gap
Valley narrows to water gap at the "Noses"; valley walls are entirely Little Falls Dolostone.

Dike
Across river, road cut in Precambrian on NY 5 showing six-foot dike cutting garnet-biotite-gneiss.

Anticlinal Effect
Precambrian gneiss and Little Falls Dolostone on right along old Erie Canal and West Shore branch of N.Y. Central Railroad displaying anticlinal effect.

Two Kames
Across river, two kames (chocolate-drop-shaped hills) of gravel and sand in shadow of Noses escarpment. Fonda flat-topped wash plain extends from here for 3.5 miles eastward to Fonda.

Gravel over boulder till
Water-laid gravel and sand overlying boulder till blankets much of the inner valley from here eastward.

Roadcut
Road cut along eastbound lane exposing uppermost Tribes Hill Formation, Amsterdam, Larrabee, and "Shoreham" Limestones.

Auriesville Shrine
Auriesville Shrine atop hill to the south.

Schoharie Creek
Schoharie Creek, east side of Schoharie Valley here is boulder till.

Gailor Dolostone
Across river, large cut in Gailor Dolostone, the dolomitic facies of the Tribes Hill Formation.

Hoffman's Fault
Crossing Hoffmans Fault.

Lower Ordovician Dolostone
Road cuts along eastbound lane in Lower Ordovician Dolostone.

Schenectady Graywackes and Shales
Hills forming Valley walls composed of Schenectady Graywackes and Shales.

Lake Albany Plain
Mohawk Valley broadens into Lake Albany Plain. Note gravels along north river bank. These thick gravels and sands are excellent reservoirs for ground water; the entire city of Schenectady and neighboring suburbs obtain their public water supplies from these almost inexhaustible water-bearing glacial deposits.

Climb out of Mohawk Valley
Climb over south valley wall out of Mohawk Valley proper.

Helderberg Escarpment
Prominent topographic feature straight ahead is the Helderberg Escarpment (not produced by faulting). Note terraces of Lower and Middle Devonian Limestones.

West shore of Lake Albany
Approximate west shore of glacial Lake Albany. Sand plains with profuse growth of pine trees extend from here to Albany. Area of sand dunes atop lacustrine varved clays, the dunes produced by wind whipping the relatively thin veneer of lacustrine sands into north-south trending hills.

Sand Dune
Sand dune.

Boulder till

B: GEOLOGIC EXCURSION FROM ALBANY TO THE GLEN VIA LAKE GEORGE
by Yngvar W. Isachsen

B: GEOLOGIC EXCURSION FROM ALBANY TO THE GLEN VIA LAKE GEORGE

Glacial Lake Albany terrace
The road cuts through an arrested sand dune developed on a former sand terrace of glacial lake Albany.
The excursion route between Albany and the Lake George region passes over the floor of this glacial lake. It is marked by lacustrine sand terraces which have, in part, been reworked by wind to form an undulating dune topography. The landscape has been further modified by post-glacial drainage. Beneath the sand veneer, which is generally less than 50 feet thick, is a rock terrace at about 300 feet elevation. This Tertiary erosion surface forms a broad platform extending between the block-faulted scarp of the Adirondack Highlands on the northwest, and the Taconic Mountains on the east and the Appalachian Uplands to the south.

Descend to Mohawk
Road descends toward the Mohawk River cutting through the blanket of lacustrine sands and into the Middle Ordovician Normanskill Formation which is exposed on the right. Lithologies represented are graywacke with mud pellets ("flysch and chips") and overlying shale. The large area of Normanskill of which this is a part has been interpreted alternatively as a thrust outlier of the Taconic klippe and as the core of a north-trending anticline.

Bridges
The attractive pair of tied arch bridges spanning the Mohawk River ahead received honorable mention for design in 1958 by the American Institute of Steel Construction.

Mohawk and Gorges
Cross the Mohawk River which here occupies a post-glacial gorge cut into the Normanskill Formation.
Immediately to the west is a deeply buried pre-glacial gorge referred to as the Colonie channel (Fig. 6). Since this paleostream channel has the flattest gradient of the tributaries as presently known, it may have been the major river draining the southeastern Adirondack region in Tertiary times. In contrast, the buried Tertiary Hudson channel probably drained the Hoosic and Batten Kill water sheds, as does the present Hudson River, but did not extend much farther north (Simpson, 1949). Beneath the present Hudson River at the foot of Madison Avenue in Albany, the buried Tertiary Hudson channel is almost 100 feet below sea level.
Immediately west of our present location, the floor of this filled channel is about 200 feet below the present Mohawk River which meanders across it at right angles. At the north end of Saratoga Lake it is about 45 feet above sea level, and west of the City of Albany about 80 feet below sea level.
The Northway roughly follows the course of this channel for the next 20 miles or more to a point at the north end of Saratoga Lake (Fig. 6). Beyond this, its extension is largely hypothetical, although supported where drawn across the present Hudson River near Glens Falls by an anomalous lack of outcrop in that short stretch. From Albany north for a distance of about 10 miles where the configuration is best known, it is a relatively steep walled channel, perhaps owing to glacial 'scour.'
The main tributary to the Colonie channel, the ancestral Mohawk Channel shown on figure 6., has been traced as far west as the Hoffman Fault where a 100 foot high waterfall may have existed in pre-glacial times (Simpson, 1949). There are about 200 feet of channel-fill in the stretch between Schenectady and Hoffmans, and the present Mohawk River meanders over its surface.'
Within the next mile the road climbs back up on the Pleistocene cover. Immediately to the east, a bedrock ridge protrudes a hundred feet above the level of the Tertiary terrace. Such relatively rare projections were islands in glacial lake Albany, which had a shoreline at about the present 300 feet contour.

Ballston Creek
Northway crosses one of the glacial meltwater channels which is now occupied by Ballston Creek. Looking down the valley to the southeast the Round Lake depression may be seen. This and Saratoga Lake to the north represent unfilled depressions, perhaps kettle lakes, on the glacial debris occupying the pre-glacial Colonie channel (Woodworth, 1905; Cook, 1930 p. 197).

Drummond Creek
Road descends into the valley of Drummond Creek, and for one-half mile cuts into highly fissile black shale of the Snake Hill Formation.

McGregor Fault
The escarpment which has been intermittently visible to the west extends from Saratoga Springs northward for a distance of 25 miles. It is a fault line scarp produced by differential erosion along the McGregor fault which marks the boundary between the Precambrian (here composed mainly of east-west trending metasedimentary rocks) and the Paleozoics. On the basis of measured Paleozoic sections in the Mohawk and south Champlain valleys, it is estimated that the vertical displacement along the McGregor is at least 2200 feet.
It is only possible at present to date the normal faulting of the eastern and southern Adirondacks and the adjoining Mohawk Valley region as post-Frankfort (i.e. post Late Ordovician) inasmuch as these are the youngest rocks known to be involved. All of the faults in the Mohawk Valley region either hinge out before reaching the Silurian at the base of the Helderberg escarpment, or pass beneath it without being recognized. Field relationships do not permit an absolute resolution of this question, but the fault movement is inferred to have occurred during the Taconic disturbance (Kay, 1942, p. 1627).

Precambrian outcrop
Outcrop of Precambrian; the rock here a quartzo-feldspathic gneiss, similar to that exposed at STOP 1.

Large scale recumbent folding and related structures in biotitic paragneiss.

View of Lake George
Note views of Lake George which lies in a graben between two blocks of Precambrian gneiss.

You are standing on Paleozoic rocks at the floor of the Lake George complex graben, completely surrounded by Precambrian rocks. The steeply rising valley walls are fault-line scarps which give the region a spectacular relief such as is generally found only well within the Adirondack perimeter; the local relief here reaches 2000 feet. Combining this value with the 500 foot estimated thickness of the Paleozoics here gives a minimum vertical displacement of at least 2500 feet.
The crystal clear waters for which this lake is noted, result from the fact that only short mountain brooks drain into the lake, and hence the very fine clay fraction common to most drainage systems is virtually absent. Most of the lake is not deeper than 50 feet, although measured depths of up to 190 feet are shown on the hydrographic map published by the Lake George Power Squadron. The many islands in Lake George number 184, and of those 154 are State-owned. Most are composed of bedrock but several are gravel drumlins according to Newland and Vaughan (1942).
Lake George now drains northward into Lake Champlain, with a decent of more than 200 feet (from 319 ft. to 95 ft.). In Tertiary time, however, both lake basins were river valleys separated by a drainage divide. The Lake Champlain valley drained into the St. Lawrence as it does today, but the Lake George basin drained southward through the relatively wide graben valley located just east of French Mountain (Fig. 7). This valley is now clogged with glacial debris including a well-shaped drumlin 1 and 1/2 miles long (Fig. 7). The inferred Tertiary drainage course is shown in Figure 6.
At the close of the last ice advance, a glacial lake occupied the basin as indicated by the presence of sand terraces representing several transitory levels in the lowering of the lake to its present elevation. The highest of the terraces has an elevation of 600 feet, and is well represented 1 and 1/2 miles to the southeast, just uphill from the Northway exit on Route 9L (see mileage 56.3).
The Paleozoics here are exposed in the railroad bed of an abandoned spur of the Delaware and Hudson Railroad, which carried vacationers from down-state to Lake George via Fort Edward and Glens Falls, until 1957. The exposed dolomite strata are either Little Falls or Beekmantown equivalents; fossils have not been found. A fault breccia in the cut contains fragments of lithographic limestone which are probably down-dragged Beekmantown limestone.
A brief summary of Colonial history of the Lake George region is given in the appendix.

Spheroidally weathered gabbro
Spheroidally weathered metagabbro is exposed in road cuts on the right.

Be alert for falling rock!
This outcrop is interpreted as an untransported soil (saprolith) formed by weathering during the Tertiary from biotitic quartz-feldspar gneiss. Note the degree which Precambrian structures, textures, and minerals are preserved. Above the Tertiary saprolith, the Pleistocene is represented by two fluvioglacial boulder gravel units. The lower gravel is weathered and hence of probable preclassical Wisconsin age; the upper gravel is unweathered and of presumed classical Wisconsin age.
When the exposure was first created in 1936, a 2 to 3 foot thick layer of varved clay was visible between the boulder gravels. This clay is thought to have-accumulated in a local body of water along the ice edge rather than as part of the main glacial lake that occupied the Lake George valley, inasmuch as the clay here is some 180 feet above the highest glacial sand terrace in Lake George Basin (Newland & Vaughan, 1942).
Tertiary saproliths such as this rarely survive Pleistocene glaciation, and are even more rarely exposed, owing to rapid mechanical disintegration and concomitant plant overgrowth. This steep outcrop apparently survives only due to constant removal of material for human use from its base. Similar saproliths have, however, been discovered in a number of localities in the Adirondacks, and in the Hudson Highlands as well, by geologists of the State Department of Public Works in connection with highway construction; they are generally short lived exposures. The structural and topographic conditions that control the preservation of these soils have not been investigated.

Spheroidally weathered gabbro
Where hill starts to level off, note the spheroidally weathered metagabbro cropping out on the right. A fresh outcrop of this lithology will be seen at STOP 5, just north of Warrensburg.

New road cuts being made for the Northway here expose pink, gray and green varieties of granitic gneiss. The typical pink granitic gneisses of the Adirondacks are composed chiefly of microcline or microperthite and quartz along with subordinate amounts of oligoclase and one or more of the dark minerals, hornblende, biotite, pyroxene. In most areas, these gneisses are equigranular, but in parts of the southeastern and northwestern Adirondacks they are inequigranular, containing pink microcline crystals (probably porphyroblasts) which measure up to an inch or more in length. This variety is generally considered to have formed by metasomatism of a biotite-quartz-plagioclase paragneiss into which it grades laterally. A subordinate lithology in this suite is leucogranitic (alaskitic) gneiss which is most prominent in the Northwest Lowlands, although it appears in the southern and southeastern Adirondacks. In the eastern Adirondacks, several large magnetite ore bodies occur in this gneiss. The granitic gneisses occur as sheets or lenses in a variety of other rock types.

Schroon River
The highway follows the flood plain of the meandering Schroon River. Sand terraces at an elevation of about 760 feet may be seen 80 feet above the valley floor. These are representative of Glacial Lake Warrensburg. (Miller, 1923).

Both contacts of this thick sill are clearly delimited, and the lower one is actually exposed.
Aside from obvious metasedimentaries, metagabbro is the only metamorphic rock in the Adirondacks whose origin has never been questioned for reasons given earlier.
Although all the minerals of this sill are the product of metamorphic recrystallization, the textures are relict igneous except at the very margin where the rock has been converted to a biotite schist.
The textures are best shown on weathered surfaces. Throughout most of its width, the sill displays a subophitic fabric, but within a few feet of the contact, the rock has a finer-grained chill border with a diabasic texture. The laths of plagioclase that define these relict textures are not single crystals of plagioclase, as originally, but granoblastic aggregates of andesine-labradorite which presumably represents an equilibrium composition for this metamorphic grade and for this bulk chemical composition. In some Adirondack metagabbros, cores of unrecrystallized igneous minerals have survived metamorphism; most notable are "dusty" plagioclase, augite, hypersthene, and olivine.
Primary constituents of the Adirondack metagabbros are plagioclase (labradorite to bytownite), augite, hypersthene, olivine, ilmenite, and magnetite. Re-equilibration of this mineral assemblage under conditions of granulite facies metamorphism has resulted primarily in reaction between plagioclase and the mafic minerals to produce less calcic plagioclase plus garnet and/or augite. Where water has entered the system, hornblende is a common metamorphic mineral. In many metagabbros the border zone has been converted to amphibolite lacking all trace of the parent igneous texture. Aside from the local addition of small amounts of water, however, the metamorphic reconstitution of gabbroic rocks in the Adirondacks has been an essentially isochemical process. In this exposure, the relatively high biotite content of the metagabbro along its lower contact indicates limited influx of K2O as well as H20 .
This roadcut clearly shows the metagabbro to be a sill. Commonly, however, the poor outcropping characteristics of the thinner metagabbros make it difficult or impossible to determine shape of the intrusives. This may account in part for the fact that the bodies are commonly shown on the older reconnaissance quadrangle maps as circular masses (Fig. 2).

Fault breccia in chloritic hornblende-biotite granitic gneiss is evidence of an episode of brittle deformation. Rotated angular and tectonically-rounded fragments of the gneiss are cemented by a chlorite paste, and within the gneiss biotite is largely altered to chlorite. This retrograde metamorphism and the local presence of drusy cavities are among the features of Phanerozoic faults that transect the Precambrian.
Dating the normal faulting that is so prevalent in the southern and eastern Adirondacks and in the adjacent Mohawk Valley (Fig. 6) is a major regional problem. The wise adage of mining geologists, "Once a fault always a fault," doubtless applies here and further complicates the problem. Inasmuch as the trends, steep dips, and other structural characteristics of those faults which are wholly confined to Precambrian crystallines do not differ from those which also involve the peripheral Paleozoics, it might be assumed that all are of the same age, namely, post-Frankfort, as mentioned under Mileage 31.5. Some faults, however, are marked by healed breccias whose mineral assemblages are in equilibrium with the regional metamorphic grade of the Precambrian Grenville orogeny. Thus, some Phanerozoic normal faulting apparently represents reactivation along Precambrian zones of weakness.
It may be of interest to note in passing that such normal faulting accounts for the rectangular drainage pattern in the Elizabethtown quadrangle to the north. Prior to detailed geologic mapping by Matt Walton, the Elizabethtown quadrangle had been cited for many years as a classic area of rectangular drainage induced by rectangular jointing.

Outcrops of paragneiss
On the left are outcrops of paragneiss, and immediately to the north are exposures of intricately contorted and refolded calcite marble and interlayered calcsilicate rock.

Marble
Road cuts through isoclinally folded beds of calcite marble containing laminae of calc-silicate minerals.

At junction of Route 28 and Potter Brook Road. Charnockitic gneiss. This rock is part of a "charnockitic suite" of metamorphic rocks which has widespread occurrence in the Adirondacks (Fig. 2). The suite includes the true charnockites (hypersthene-bearing gneisses of granitic composition) and varieties departing from granitic composition by: 1) having a lower quartz content than the required 10% (or 20%, depending upon rock classification used), and 2) a range in the ratio of plagioclase to K-feldspar of from less than 1 to more than 1. The gneisses are characteristically gray to dark green in fresh exposures, and weather to a maple-sugar brown; pink facies occur also, however. Microperthite is the predominant mineral; mafic minerals may include hypersthene, augite, hornblende, biotite, and garnet. Owing to the variation in percentages of the "essential" minerals, (commonly within a single mapping unit) and the attempt to fit these lithologies into igneous-rock pigeonholes, they have been mapped under at least 12 different names during the past 50 years. They have been most commonly designated "quartz syenite" and "syenite". However, such terms carry a misleading connotation inasmuch as the rocks are at present largely, if not wholly, metamorphic, whatever their ultimate origins.
In much of the Adirondacks, rocks of this suite occur as unbanded, relatively monolithic layers many hundreds of feet thick. In the southern Adirondacks however, banded charnockitic gneiss with intimately interlayered sedimentary rocks occurs in a number of areas. The monolithic layers are most commonly exposed as the cores of domes and antiforms, as is expectable from their relatively high resistance to erosion.
The Hudson River, which flows by a few hundred feet to the west, is cut into metasediments.

Quarry on right side of the road in banded, pink and gray paragneisses with scattered biotite schist layers. Breccias occur at northern end of outcrop, but more prominent there is a diabase sill with fine-grained chill borders. This is one of many such undeformed diabase intrusives in the Adirondacks. They generally occur as this, steeply-dipping dikes. Inasmuch as they are undeformed they must postdate the Grenville Orogeny. They have been generally interpreted as Late Precambrian.

Roadcut in marble across from junction with road to Friends Lake.
The calcite marble and calc-silicate beds here are typically highly deformed, having been isoclinally folded - and probably refolded as well. The relatively competent calc-silicate layers have been stretched, attenuated, and dismembered well beyond the boudinage stage so that they occur as disconnected lenses, hooks, and clots. Such floating fragments have sometimes been picturesquely tagged "tectonic fish", and "dead snakes". Minerals which can be readily found and identified include graphite, diopside, brown tourmaline (dravite), pyrite, sphene. Undeformed mafic dikes with fine grained chill borders may be seen cutting the marble.
Continue on Route 28 across Hudson River, which here cuts into metasedimentaries.

Cross a second bridge, over small, tributary to the Hudson River, and immediately park on the left at entrance to closed road. Descend to stream, where may be found glacial boulders of most of the resistant Adirondack lithologies. The only major rock type not yet seen on this excursion - anorthosite - is well represented. Both the relatively pure Marcy-type anorthosite, and the more mafic Whiteface type maybe found. Proceeding upstream a short distance, a wide variety of metasedimentary lithologies may be seen cropping out in the stream bed. These include: paragneisses, quartzites of varying purity, amphibolite, marble and calcsilicate rocks.

C: GLACIAL LAKE SEQUENCES IN THE EASTERN MOHAWK-NORTHERN HUDSON REGION
by Robert G. LaFleur
Rensselaer Polytechnic Institute
18 Stops
No road log

Long, narrow drumlins with east-west trend, 2 miles west of Mariaville Lake.

Flaggy boulders of Schenectady Formation predominate drift north of Duanesburg; well exposed along Duanesburg Churches Rd. Excellent view of drumlin terrane north from Highland Park Rd.

Overlook of Duanesburg channel (of Delanson River) at Duane, Rt. 7 one mile south of Duanesburg.

Drumlins north of Rt. 20, 1 1/2 miles east of Duanesburg. Roadcut exposes till. Good view north across Normans Kill valley.

Overlook of lower Mohawk Valley from hill one mile northwest of Rotterdam; 350' terrace remnant of Mohawk delta; river gravels; islands in the Mohawk River at Scotia.

Outlet channel of Early Lake Amsterdam now occupied by NYS Thruway; 1/2 miles west of exposure no .·5.

Delta in Late Lake Amsterdam at Hoffmans; Wolf Hollow gorge of Chaughtanoonda Creek has formed along the Hoffmans Fault, accentuating a striking topographic lineament traceable for 3 miles to the north.

Glenville kames along the West Glenville Rd.; suggesting the location of the ice margin which defended Early Lake Amsterdam.

View from Potter Rd., one mile north of Glenville, south to rock benches of the Glenville Hills.

View from Ostrander Rd., one mile east of Guilderland Ctr., southwest to Helderberg escarpments.

Along Grant Hill Rd., one mile southeast of exposure no. 10; dissection of the south (lee) side of a drumlin by the Normans Kill exposes 100 feet of bouldery till.

Guilderland kame terrace along southwest shore of the Watervliet Reservoir. Several gravel pits expose southwest-dipping gravels and sands; also isolated pockets of rhythmic clays. A solitary kame is located at the intersection of Routes 158 and 146. The Lake Albany 330' beach has modified the northeast (ice contact) side of the kame terrace.

Rensselaer (Lake Albany) kame delta, east of city limits of Rensselaer. Turbidite sands in delta bottomset beds; graded bedding, sole markings.

Lake Albany beach ridge with gravel pit excavation; one mile north of Defreestville on Bloomingrove Rd.

Teller Hill promontory, one-half mile west of Sherwood Park. Panorama of Hudson Valley, the Hampton Park kame delta, and the Hudson flood plain.

Eskers of the Albia-Burden Lake complex, exposed in several large gravel pits on Route 66 east of Wynantskill.

Panorama from East Line Rd., 3 mlles north of Jonesville. Ballston outlet channel at East Line; Round Lake depression and channel, Malta sand plain. Round Lake channel also shown where it is crossed by the Northway one mile east of exposure no. 17.

Coveville outlet and plunge pool three miles south of Schuylerville on west side of Hudson River.

D: GEOLOGIC PHENOMENA IN THE SCHENECTADY AREA
P.C. Hewitt
Wm. E. McClennan Jr.
Harold Nilsson
Three Stops

STOP 1 The Clifton Park Anticline
Location
The outcrop is located at the top of a hill in the town of Clifton Park on N.Y. Rt. 146, 1.7 miles east of the intersection of Rts. 9 and 146. If approached from the east the outcrop lies 0.5 miles west of the intersection of Rts. 146 and 236.
Description
The Clifton Park anticline is an excellent outcrop for teaching purposes. At the one locality many structural and sedimentological features may be observed. It also is a prime example of the thrust faulting in the eastern part of the lower Mohawk Valley. There are only a few faults of this type in the area and they probably represent only small scale thrusting. Though associated with Taconic thrusting they are not part of the Taconic region itself but are west of the westernmost zone of that much discussed area.
The strata exposed at Clifton Park are assigned to the Normanskill formation and represent primarily the Austin Glen Graywacke member. Some black shales are interbedded with the siltstones and graywackes. The mud pebble conglomerate so common in the Normanskill may also be observed at this outcrop. No fossils have been reported from this exposure but the lithology is typical of this Middle Ordovician unit and fossils found in the near vicinity assure this age assignment. The outcrop extends for about 600 feet on either side of the road. It is apparent from a rapid glance that the strata on the north side of the road do not match those on the south side. To gain the most from this exposure it is best to start your traverse at the west end on either side of the road and to walk toward the east and return in the opposite direction on the other side of the road. A series of thrust faults may be seen on either side of the road.
At the west end of the exposure on the south side of the road is a small thrust which may be observed to blend into a bedding plane fault to the east. Virtually all of the faults show mineralization along the fault plane. The mineralization usually consists of well slickensided calcite. No individual fault can be traced any great distance but there is no difficulty in detecting the faults nor in following them over a distance of several yards or more. The entire section of strata on the south side appear to be less contorted than on the north. This is more apparent than real, however, for the whole area is part of an anticline plunging to the south.
Structural features on the north side of the road are quite different. Starting at the east end one may see beds dipping about 30° to the southeast followed by a small symmetrical anticline. About 25 ft. further west is a small faulted anticline. The fault here is a small thrust with a strong drag zone. Gouge may be seen in the fault plane itself. Another small but tight fold succeeds the fault to the west. About 75 ft. from the small fault is an interesting overturned anticline with an east limb dipping only a few degrees to the east and a west 11mb dipping 75° to 80° to the east. As a result the beds on the west limb are up-side-down. For a distance of about 30 ft. is a zone of shattered siltstone which may represent one of the faults on the opposite side of the road. Still walking westward the last structure to be encountered is a symmetrical anticline whose limbs dip 30°. Jointing is obvious through the section.
In addition to the structural elements there are many sedimentary features to be seen on both sides of the road. Mud pebble conglomerates, large ripple-marks, graded bedding and other features may be observed throughout. It is also interesting to note the result of unloading of the surface upon the siltstones and graywackes. Here, the beds have fractured and it is possible to see the difference between the beds which are actually several feet thick and the zone in which the beds appear thinner due to unloading. Furthermore, it is obvious that the beds of siltstone and graywacke do not maintain a constant thickness as one traverses the outcrop.
Discussion
The primary cause of interest at the Clifton park anticline lies in the differences in strata and structural appearance on either side of the road. Some students have suggested that a fault, striking east-west is responsible for the disparity. This seems unlikely and is not needed to explain the exposure. On the contrary, an asymmetrical fold plunging to the southwest which was later cut by faulting seems to provide a simple and more adequate explanation. The explanation lies more in the asymmetry of folding followed by erosion than in any other factor. Certainly there is room for interpretation at this outcrop and we will welcome any comments.

STOP 2 Geyser Park and the "Vale of Springs"
Location
This area is a portion of the state-owned Saratoga Springs Reservation located just so~th of the city of Saratoga Springs, between N. Y. 9 on the east arid N.Y. 50 on the west. Geyser Park is situated in the western half. Entrance to the Park is via.a new road at the southern limits of the reservation which connects with both Route 50 and Route 9. The old entrance and approach to the Park, near the Hall of Springs, has been closed to vehicular traffic making it impossible to approach the. park from the north. Visitors may, however, elect to park in that section of the reservation and walk down the hill into the upper section of the Park.
Features and Lithology
This area has the highest concentration of "springs" and "geysers" of any area in or around Saratoga. Altogether four "springs" and three "geysers" will be in operation upon the completion of a multi-million dollar reconstruction program.
The mineral waters discharged by the "springs" and "geysers" are representative of the Saratoga type mineral water; a highly saline water charged with varying amounts of carbon dioxide gas. Occurrences of this type mineral water is restricted to only one other locality in the United States.
The wells in the Park,some almost 1,000 feet deep, continuously discharge large volumes of water. The water is carried up in the well by the release of gas pressure in much the same manner as a warm and well-shaken bottle of soda ejects its contents when opened.
This water pressure, passed through a small orifice at the top of some wells, produces the so-called "geysers" to be seen in the Park.
The large proportion of salts in the water, particularly carbonates, produces interesting tufa deposits in the form of cones, flows and terraces.
Geyser Brook, a non-carbonated, non-potable stream winds through the Park from the north, cutting a small valley and exposing the Canajoharie shales in several places. Rather poor specimens of some graptolites can be secured at several horizons in the shale.
Tour and Discussion
The first of three "geysers" to be observed is the Polaris "Geyser." All "geysers" are free flowing, but the force with which they leave the casing is regulated by using a small orifice. All of the "geysers" have been drilled and are actually wells which are allowed to run free. We have placed the word "geyser" in quotation marks since a true geyser is associated with hot water driven from the ground by steam pressure. Part of the cone of the Polaris has been created with stones piled around the casing, but a considerable amount of tufa (travertine) has been deposited since their initial operation.
The Park road eventually reaches a large parking lot, snack bar and comfort station. Further exploration will be on foot. Proceed across the bridge and turn right on the path. Just above the bridge is the Hayes Spring (well). The terminology becomes difficult at this point as both the spring and well apply. The impervious cap rock was pierced by a well in 1909. However, the water flows under its own pressure much as in a spring. Arguments could be collected in favor of an artesian well or spring. The reader is invited to choose one or the other. The Hayes is a pleasant water for those who are native to the area and who have acquired a taste for Saratoga type mineral water. It is well carbonated and moderately saline and popular with mineral water enthusiasts. A hole on the upstream side of the Fountain permits people to inhale the excess gas from the well and it is guaranteed to "clear your head." An analysis of the Hayes Well is appended for people with geochemical interests or for those who are just plain curious about what they are drinking. It is only fair to warn the drinker that many of the dissolved salts have had a reputation as "diuretics and cathartics," and they seldom fail to achieve this result when taken in any quantity. The "geyser" a hundred feet or so upstream is appropriately named the Island Spouter "Geyser." Its waters ascend in a graceful flow to heights of thirty feet or more and is a much photographed object. The tufa cone and surrounding terrace is no more than 40 years old but in that time it has acquired a considerable thickness. The terrace is very slippery and the water tastes the same as the Hayes. Since another terrace is more accessible, it is not necessary at this point to get any closer to it than you are.
A much larger and more impressive tufa flow occurs a few hundred yards upstream where the overflow from the Orenda "spring" cascades over the bank and enters the brook below. This action results in a vertical structure approximately thirty feet high and two to five feet thick. This tufa flow is, in a sense, a miniature Yellowstone of the east, with the notable exception that it is almost 93 percent carbonates from cold water rather than siliceous matter (silicates) from hot water. According to Strock, the travertine is built up at the rate of 0.5 gram/liter of water. Literally translated to English units, it works out to be one pound in 240 gallons, or a potential two tons per million gallons.
The terrace is an interesting physical structure but the tufa itself has a few singular features. First of all, it is radioactive. Minute amounts of radon and other radioactive materials dissolved in the water become highly concentrated in the tufa. The tufa also affords an open-air, above ground exhibition of cave type travertine formation. The rapidity with which it forms causes it to be more coarse and granular but the laminations are readily visible. The rapid formation of tufa gives rise to a sort of "instant fossilization" process. Twigs and leaves are quickly coated with the carbonates and become a part of the fossil record. Loose pieces of tufa show excellent imprints and faithfully record the botanical activity near the terrace. With some luck one can occassionally find an insect accumulating a calcareous overcoat.
Some of the shales on either side of the terrace have a few graptolites. These would be Ordovician but identification is difficult because of an absence of detail. The best horizons seem to range from two to five feet above the level of the path. Further upstream the path terminates at a bridge which crosses Geyser Brook as it emerges from a stone culvert which once carried the water beneath the now abandoned roadbed of the Delaware and Hudson Railroad. This is a very interesting area following a heavy rain; a prime spot to study the Venturi effect on the velocity of liquids.
The pipe discharging water into the stream at the southern end of the bridge is actually the water from the Champion spring (well). The well has sufficient pressure to be a "geyser" and was for a long time, and it may again function as such. The water is noticeably sulphurous in taste and smell, the only water in the Park to have this characteristic. Since this is not typical of Saratoga Mineral Wateor, we can assume that the casing has been perforated by corrosion and ground water is entering from the shales. Considerable quantities of sulfur water are encountered throughout the Canajoharie and Snake Hill shales much to the consternation of suburban Saratogians. At Saratoga Lake the waters become heavily charged with hydrogen sulfide. Luther's White Sulfur Springs, at one time, was a small spa itself but is unfortunately eclipsed by more famous sulfur springs to the west at Richfield and Sharon Springs. All sulfur water seems to be a product of the Ordovician Shales which outcrop in the Mohawk Valley from Utica eastward.
A second Champion "Spring" flows from the bank about 50 feet beyond the bridge. After crossing the bridge, the path climbs up the west bank and enters a road which passes south along the bank, passing the Orenda "Spring" whose overflow is responsible for the tufa terrace previously inspected. An excellent view of the Island Spouter "Geyser" is obtained along the road just before it descends to stream level at the Hayes Well and the parking lot. The Karista "Spring" is located a few hundred yards down stream on the west side of the brook from the bridge. Its mineral composition and gas content are much lower than either the Hayes or the Orenda. However, unless the visitor has a special interest in mineral water, it might be well to terminate the tour at the bridge and return to the parking lot.
The Saratoga Mineral Water Mystery
The manner in which this water was produced has excited the interest of many people and the theories seem to be directly proportional to the number of investigators. A few facts seem to have universal acceptance.
First, the water is in limestones and dolomites covered with the impervious layers of Ordovician shales which extend to the north, east and south. The Little Falls dolomite was given the credit for some time until Fisher and Hanson (1951) established the dolomite as Ordovician and renamed it the Gailor dolomite.
The water appeared at Saratoga because of an extensive fault (MacGregor) which forms a scarp north of Saratoga and then bifurcates as it approaches Saratoga. The eastern branch of the fault breached the shale and allowed the water to escape upward along the fault plane. This is graphically displayed at the north end of Saratoga Springs at High Rock Park. Route 9N traverses the top of the scarp and at the base approximately 30 feet of dolomite is exposed. High Rock Park is the site of the High Rock Spring, a true spring, which was known by the Indians long before Jacques Cartier first reported it in 1535. Only the tufa cone of this spring remains but a hundred yards to the north the Old Red continues to flow, having done so since 1774.
The control of the fault is striking. All springs and wells are always on the eastern side and the water issues forth at many places from Wilton, four miles north of Saratoga to Ballston Spa, seven miles to the south. Altogether some 200 springs and wells have produced Saratoga type mineral water, and always on the eastern side of the fault.
The source of the large mineral and gas content of the water has always been the difficult part of the problem.
Kemp (1912) looked to some deep-seated source for CO, Cl, Br and Fe. His ideas were deeply influenced by the presence of an old volcanic mass at Northumberland (Stark's Knob) some 15 miles northeast of Saratoga.
Strock (1944) on the basis of geochemical data, felt that the chemical content was in many ways related to sea water. As a result he placed the source in the Salina group, the extensive salt beds of Central-Western New York. Such beds extend eastward into Schoharie county, an area about forty miles to the southwest of Saratoga. Ruedemann-Cushing (1914) suggested that Saratoga waters originated to the east of the region, aided in their movements up the bedding planes and fractures of the limestones and dolomites by a hydrostatic head established in the Green and Taconic Mountains. The "volcanic exhalation" would doubtlessly furnish the CO2 but in all probability furnish other gases as well. It leaves a question as to the mineral matter and overlooks the lack of any thermal activity which in most cases might be associated with deepseated activity.
The virtual absence of all sulfates in the Saratoga water is difficult to correlate with the average chemical composition of sea water, either ancient or recent. Strock (1944) envisioned the water as coming down the Mohawk Valley and then moving northward. Unfortunately the dolomite outcrops long before it reaches the fault and in all probability would give up the water long before it reached the Saratoga fault. Then, too, it must be remembered that all wells and springs occur on the eastern side of the fault. The eastern basin theory seems to have fewer "ifs" and more positive evidence. The limestones and dolomites are buried at depth and covered by thick and impervious shales. The upturned edges of these beds, raised in the Taconic disturbance, collects the water. The limestones and shales are reasonably competent and withstood the compression of the Taconic disturbance without difficulty until it grounded out against the crystalline base of the Adirondacks. The north-south lineation of the fault would tend to substantiate this idea. This places the source of the water in the dolomites and limestones. Considerable amounts of sodium, calcium and magnesium salts are available plus the halogens which are noticeably high in the water. The Hoyt limestone beneath the dolomite contains a vast  Cryptozoon population which suggests shallow seas and possibly intermittent periods of dryness whereupon some elements would crystallize out and into the calcareous material of the sea floor. Any acid bearing ground water introduced into these carbonates would immediately begin an attack on the carbonates which in turn would begin the production of CO2. This gas, sealed in the acquifer by the shale above and brought up in pressure by a hydrostatic head, would produce a strong carbonic acid system which would increase with further solution until reasonably high pressures were developed. More than ordinary solution would occur, unlike the conventional solution as observed in other limestone areas. The water, driven westward by a hydrostatic pressure, reaches the fault and is carried up the thousand or more feet by the sudden release of the gas pressure. Colony (1929) in his report to the Saratoga Springs Commission examines all previous ideas and debates them in far more detail. Although the mineral water industry has declined seriously, the controversy as to its source and origin has flourished. Anybody with a new theory??
Selected References
Colony, R. J. 1929 Report to the Saratoga Springs Commission, Restudy of the Geology of the Saratoga Area and the Problem of the Mineral Waters. N.Y.S. Legislative Document #70, 1930.
Fisher, Dopald W. and Hanson, George F. 1951 Revisions in the Geology of Saratoga Springs, New York and Vicinity. American Journal of Science, Vol. 249, Nov. 1951, pp. 795-814.
Kemp, James F. 1912 The Mineral Springs of Saratoga. N.Y. State Museum Bull. No. 159, pp. 5-79.
Rudemann, R. and Cushing, H.P. 1914 Geology of Saratoga Springs and Vicinity. New York State Museum Bull. No. 169.
Strock, Lester W. 1944 Geochemical Data on Saratoga Mineral Waters-Applied in Deducing a New Theory of Their Origin. Publications of Saratoga Spa No. 14, 1944.
DEC Links 1 2 3

STOP 3 Stark's Knob
Stark's Knob is a protuberance of volcanic rock located north of the town of Schuylerville, New York. It was named after General John Stark of the Revolutionary Army that hindered Burgoyne's retreat to the north (Woodward, 1901). It is found 1.2 miles north of Schuylerville just west of New York State Highway #4. The Knob is a mass of'basalt about 200 feet high and is surrounded by Ordovician Normanskill shales. The rock has been quarried for road metal resulting in exposure of the interior of the rock mass. In describing the Knob and locating its features, it will be convenient to refer to the quarried face on the east and the natural face, which is a steep cliff, on the west. Prior to quarrying, the Knob was probably ovoidal or circular. It may be noted that basalt is also found on the south side of the dirt road located south of the Knob.
Standing at the base of the quarried face one can see a mass of dark basalt broken by many fractures and fault planes. A prominent fault or fracture extends upward along the middle of the quarried face. A less obvious fault exists about 50 feet up slope from a small circular well or pool at the base, near the southern corner of the quarried face. One can also see pillow lava or lava ball structure displayed allover the quarried face. The western natural face is almost vertical on its north end and is partially covered by talus on its southern end. The southern portion of the Knob is unquarried and is extensively covered by brush and trees. A foot path extends over the crest of the Knob. At the summit" a plaque offers the history of the area and a presumed explanation of the geology.
Rock Types
The basaltic Knob is surrounded by slaty shales of the Normanskill formation. The shales are blue-gray and weather to buff and locally rusty-red. Cleavage is well displayed, and bedding is obscure. The shale-basalt contact is exposed on a small hump at the base of the Knob along the dirt road leading to the quarry. The contact is also exposed along the northern end of the Knob at the edge of the quarry where it curves eastward, and in a small patch near the summit along a path leading down the talus slope of the natural face. No apparent macroscopic contact metamorphism of the shales has been observed. Some of the shales at these contacts may be fault slices or inclusions in the basalt.
Where the shales have been faulted, their character changes. This may be seen at the base of the quarry area and on a linear mound or hump which trends east-west at the base of the Knob on its southeasterly side (south of the quarry area). This mound will be discussed in the section on structure. The shales, which apparently have been faulted, do not show such prominent fissility as displayed in shales farther from the Knob. The rock has curved, platy surfaces and weathers rusty-red.
The basalt occurs as pillows) balls or ovoidal structures embedded in a matrix. Both the lava balls and the matrix are liberally penetrated by calcite veins. The pillows range from approximately an inch to four feet along the greatest dimension. They display radial jointing in the outer portions. The lava pillows are surrounded by a dark~ foliated~ shaly matrix. This matrix concentrically su~rounds and winds through the space between the pillows. Some pillows have a dark, glassy coating which in some places appears to be part of the matrix and at others, part of the pillow. Lava balls and limestone inclusions are beautifully displayed on the quarry face. Balls of varied sizes and shapes are randomly grouped. The balls show coarser grained interiors with a fine grained rind on the surface. In'rare cases they display characteristic pillow structure including the tail-like feature.
On the southeast unquarried portion of the knob the basalt does not show ball-structure as clearly. This rock is very porous, apparently due to leaching of calcite or some other mineral. There are many large and small holes in which lady bugs may be found hibernating during cold weather. This porous rock crumbles when struck by a hammer. Massive patches of basalt in which faulting is manifested by planes with slickensided calcite also occur on the unquarried portion of the knob. On both the quarried and natural faces the lava pillows contain amygdules. Many pillows, however, show no amygdaloidal structure.
Limestone inclusions may be found readily in the lava balls. The limestone is medium to dark gray and is medium to fine grained. The limestone weathers to buff or tan~ surrounded by a darker portion near contact with the basalt. Fracturing along calcite veins may give the appearance of a limestone inclusion. Care must be taken to make sure one is looking at an authentic inclusion. On the natural face the limestone is especially different from the quarried face. Here the inclusive nature of the limestone is less apparent and the limestone may actually be in the matrix. Locally a limestone matrix with basalt fragments appears as a breccia. The limestone itself is porous and is almost entirely calcite. An extremely small amount of fine, unidentified, insoluble residue was obtained from this limestone.
Structural Geology
The only secondary structures that can readily be seen in the basalt are fractures and faults. On the quarry side there are many ledges, over which one may walk, which exhibit slickensided calcite. Locally, calcite veins offset by fractures can be found. Along the crest over the quarry face there are fractures which are parallel or semi-parallel. Calcite veins occupy some of the fractures. Along this same crest and on the natural face the fractures are closer spaced than on the quarry side. Throughout the knob, calcite and quartz crystals occupy large fractures. Irregular calcite veins pervade the basalt and are not apparently related to fractures.
Faulting is manifested in the slickensides found along the calcite veins. At least some faulting must have taken place after the deposition of the calcite. There is one large fault plane or fracture striking N 500W and dipping 520 NE on the quarry side. It is covered with talus and vegetation making investigation difficult. Another prominent fault striking N 450W and dipping 320 NE is exposed above the small well just south of the quarry area. The rock here is crushed, folded and has a peculiar shaly appearance and is probably gouGe. There is basalt above the fault and talus below. Intersecting this fault almost perpendicularly is another fault which strikes N 650W and dips 790 NE. The fault surfaces here have very prominent slickensides.
The linear mound or hump mentioned previously strikes N 550E and plunges away from the Knob near the bottom of its southeast slope. The hump is about 12 feet across and 70 feet long. The rock exposed here is slaty shale but, as mentioned before, is different from the surrounding Normanskill shales.
Problems of Stark's Knob
This report is, of course, brief, superficial and almost entirely descriptive. It does not propose nor support any genetic theories for Stark's Knob. However, one cannot help but question the origin of this rock, and how it, unlike any other in the State, could have occurred here.
The main question concerning the orlgln of Stark's Knob is whether it is a volcanic neck, indigenous to this locality, or an allochthonous mass faulted in from some other area.
Cushing and Rudemann (1914) hesitantly support the theory that the knob is autochthonous and was intruded where it stands. Never the less, they acknowledge the apparent lack of contact metamorphism and the absence of any inclusions, especially shale, other than the limestone.
The irregular, fine grained calcite veins contrasted to the coarse, crystalline and slickensided ones may indicate more than one period of calcite precipitation. The pillow-type structure is similar to known subaqueous pillow lavas, hinting at under-sea extrusion of the basalt precipitating calcium carbonate dissolved in the water.
Bibliography
Cushing, H.P., and Ruedemann, R. 1914, N. Y. State Museum Bull. 169, p. 115-135
Woodward, J. B., 1901, N. Y. State Geol. 21st Rept., p. 17-24.
DEC Links 1

GEOLOGY OF WESTERN NEW YORK
Guidebook
New York State Geological Assn
1964
Department of Geological Sciences
State University of New York at Buffalo
Buffalo, N.Y.
E. J. Buehler, Editor

A: SILURIAN STRATIGRAPHY OF WESTERN N.Y.
by Edward J. Buehler
State University of New York at Buffalo
and
Wiliam J. Kilgour
Buffalo Museum of Natural Sciences

A: SILURIAN STRATIGRAPHY OF WESTERN N.Y.

STOP 1. DeCew Generating Station
Refer to papers by Fisher (p. 1), Kilgour (p. 10), and Zenger (p. 19). The following stratigraphic column for DeCew Falls is taken from Bolton, 1949.
0 - 12 | Dolomite, light grey dense nodular, weathering buff to white. | Lockport
12 - 25 | Dolomite, as above, but with abundant nodules of chert. | Ancaster
25 - 56 | Limestone, coarsely crystalline and porous, or sandy, with thin shale interbeds. | Gasport
56 - 64 | Dolomite argillaceous to sandy, calcareous, dark grey, weathering buff to tan. | DeCew
64 - 120 | Shale, fissile, green-grey to dark grey. | Rochester
120 - 127.5 | Limestone, pink to dark grey, coarsely crystalline, crinoidal. | Irondequoit
127.5 - 134 | Limestone, dolomitic, dense, light grey; top 0.5' sandy. | Reynales
134 - 142 | Limestone, dense, light grey, massive, with thin sandy partings. | Reynales
142 - 143 | Shale, greenish grey to dark grey. | Neahga
143 - 148 | Sandstone, fine grained, massive, white to light grey, with a few thin shale partings. | Thorold
148 - 148.5 | Shale, dark grey. | Grimsby
148.5 - 152 | Sandstone, as above | Grimsby
152 - 183 | Sandstone, fine grained, red mottled with green, with interbedded red shale. | Grimsby
183 - 194 | Shale, red and green, with minor beds of red sandstone. | Grimsby
194 - 242 | Shale, dark grey to green, calcareous, with beds of sandy shale and light grey calcareous sandstone. | Power Glen
242 - 254
Sandstone, quartzose, white to light grey, massive to thick bedded with small scale crossbedding. Thin zones of grey shale pebbles (intraformational conglomerate).
Whirlpool
254 - | Shale, brick-red with 0.3' of light green shale at top. | Queenstone

STOP 2. Lunch. Examination of exhibits at Power Vista.
Following is the stratigraphic section here. See papers by Fisher (p. 1), Kilgour (p. 10), and Zenger (p. 19), for details.
Eramosa | 20'
Goat Island | 19'
Gasport | 27.5'
DeCew | 8'
Rochester | 68'
Irondequoit | 26'
Reynales | 8'
Neahga | 6'
Thorold | 7'
Grimsby | 52'
Cabot Head, etc. | 36'
Whirlpool | 25'
Queenston | 100' exposed

Ascend Niagara Escarpment

Lockport Dolomite outcrop

STOP 3. Frontier Crushed Stone Quarry
The following units of the Lockport are exposed here. See paper by Zenger (p. 19) for details.
Goat Island | 24.0'
Gasport | 29.5'
DeCew | 8.5'

STOP 4. Akron Falls
STOP 4A. The following members of the Bertie dol. are exposed at the falls. See paper by Rickard (p. 24) for further details.
Scajaquada | 8'
Falkirk (the massive Member) | 20'
O-atka | 20'
The reentrant of the base of the falls is identified as the top of the Camillus Shale.
STOP 4B. About 1/4 mile upstream from the falls. The units here are:
Nedrow member of Onondaga | about 6' exposed
Edgecliff member of Onondaga | 5'
-- Silura-Devonian unconformity --
Akron dolostone | 8'
Williamsville member of Bertie | 6'
See papers by Rickard (p. 26), and Oliver (p. 32) for details.

B: UPPER DEVONIAN N.Y.S.G.A. FIELD TRIP
by Dr. Irving H. Tesmer
State University College at Buffalo

B: UPPER DEVONIAN N.Y.S.G.A. FIELD TRIP

Onondaga Limestone
Observe Onondaga Limestone to left (Buffalo NW quad)

STOP 1. Hamburg Park
Hamburg Park (Buffalo SE quad); exposures of Ledyard and Wanakah

STOP 2. Home of Piarist Fathers
Home of Piarist Fathers (Eden quad); exposures of Wanakah, Tichenor, Windom, Genundewa and West River;
2010: Now the Graycliff Conservancy maintains this Frank Loyd Wright house

STOP 3. New York Central Railroad Bridge.
Arrive 11:15. Follow path to left along west side of railroad to banks of Eighteen-mile Creek (Eden quad); observe exposures of Cashaqua and Rhinestreet; depart 11:30.

STOP 4. Church Parking lot
Walk 0.2 miles further east along Eighteen-mile Creek Road to U.S. 20 and then to bridge over Eighteen-mile Creek (Eden quad); observe exposure of Rhinestreet; depart 12:00.

Sand Ridge
Observe prominent sand ridge to right (Angola quad) . Next 1.2 miles.

STOP 5. Evangola Parking Lot
Arrive 12:30. Evangola State Park (Farnham quad);lunch and rest stop; exposures of Angola Shale; depart 1:30.

STOP 6. Bridge over Cattaraugus Creek
Arrive 11:45. Niagara Trading Post and bridge over Cattaraugus Creek (Farnham quad); observe Angola Shale and preglacial course of Allegheny River; depart 2:00.

STOP 7. Walnut Creek
Arrive 2:15. Walnut Creek (Silver Creek quad); exposures of Angola, Pipe Creek and Hanover; depart 2:45.

STOP 8. Point Gratiot Park
Arrive 3:15. Exposures of Dunkirk Shale; depart 3:30.

Hanover Shale
Observe various exposures of Hanover Shale in the Lake Erie cliffs to right (Silver Creek and North of Dunkirk quads). (Next 4.7 miles.)

Abandoned Lake Beach
Observe abandoned lake beach to right, associated with glacial Lake Warren at Sheridan, New York (Dunkirk and Forestville quads)

Hanover-Dunkirk contact
Silver Creek interchange #58; observe Hanover-Dunkirk contact (Farnham quad).

Rhinestreet Shale
Observe exposures of Rhinestreet Shale (Buffalo SE quad). (Next 0.3 miles)

C: LATE PLEISTOCENE GEOLOGY AND GEOMORPHOLOGY OF NORTHWESTERN NEW YORK
by Parker E Calkin and Charles J. Caseau
State University of New York at Buffalo

C: LATE PLEISTOCENE GEOLOGY AND GEOMORPHOLOGY OF NORTHWESTERN NEW YORK

Subdued Niagara Falls Moraine
Pass south over very subdued Niagara Falls Moraine; 20-30 feet of relief at stream cuts on otherwise very flat plain of Lake Tonawanda. This is the lowland of Upper Silurian, Salina Group.

Plains of former Lake Tonawanda
Turn right at Exit N-16 onto U.S. Rt. 290, Youngman Expressway, and proceed east over plains of former Lake Tonawanda.

Onondaga limestone Escarpment
Rise south over Onondaga limestone (M. Dev.) Escarpment. Exposure here in roadcut as you pass under Main Street.

Cazenovia Creek
Cazenovia Creek, a tributary of the Buffalo River at your right.

Morainal ridge
Turn left (E) onto Main St. and proceed along well defined morainal ridge at 660-670' through Ebenezer. Ridge is a probable westward extension of Leverett's (1902) Alden Moraine. DeCew 15' Orchard Park 7 1/2' It has been mistaken for a Lake Dana beach ridge but has probably been altered by Lake Dana waters (680-700'). Cellar cuts reveal a dense till, rich in large, striated boulders of Onondaga limestone.

Subdued morainal ridge
Join Seneca St. and proceed along subdued morainal ridge.

Road collapse
Turn right (SE) onto N.Y. Rt. 16, still continuing on Seneca Rd. At right, lateral migration of Cazenovia Creek has caused collapse of paved road.

Tichenor limestone falls
Note at left the falls formed by resistant and fossiliferous Tichenor limestone Member.

Glacial Lake Warren beaches
Beyond intersection with Kingsley Rd., Northrup crosses shaley gravel of glacial Lake Warren beaches, 800-830'. At left, 7 miles beyond is gravel beach ridge, 830', behind green house.

Glacial Lake Whittlesey
Proceed left (S) on Transit Rd. rising up to glacial Lake Whittlesey features, 900'.

STOP 1. Cancer Prevention Research Center.
View postulated, (Fairchild, 1906) Lake Whittlesey, wave-cut beach and scarp at left and right on north side of hill. Ridge appears to be largely shale, but its north side is partly flanked by well sorted sand.

Ridge crest in Lake Whittlesey gravel
Cross ridge crest (880') after .3 miles. Cellar of Barren house at right, was dug in Lake Whittlesey (?) gravel. Bear right (S) beyond ridge onto Willardshire Rd.

Hamburg Moraine
Proceed past probable kame moraine gravel ridge at right on north side, Hamburg Moraine.

Hummocky terrain
Cross Cazenovia Creek and proceed on Willardshire Rd. across typical hummocky topography of Hamburg Moraine.

Lake Whittlesey beach
Proceed through intersection of Jamison and Conley Roads with Seneca Rd. which overlie a Lake Whittlesey beach and spit at 900'. Beach topography is now nearly obscured except for minor sand ridges on grounds of Moog Plant at right (N). Descend from split, .3 miles west of Moog Plant.

Beaches of glacial lake Warren
Turn right (E) beyond Church onto Rice Rd. which follows beaches of glacial lake Warren (lower or second Lake Warren).

Beach Ridge
Observe prominent beach ridge at left of intersection with Dellwood Dr.

Pit cut in beach
An abandoned gravel pit 1.3 miles beyond Seneca Rd. cut in the beach exposes 20' of well sorted gravel.

Second Lake Warren ridges
Note again at least two prominent ridges of Second Lake Warren (Blackmon, 1956) left, .7 miles from Bowen Rd.

Cross Buffalo Creek.
Pipeline trenches adjacent to creek here revealed 2' of gravel over blue shaley till.

Lake Warren beach ridges
Turn left onto Stille Rd. (Stolle Rd.) noting well formed beach ridge of Lake Warren on right. Cross at least 3 NE-SW trending ridges of Second Lake Warren 835-800'.

Delta
Turn right onto Clinton Rd. and pass across delta of Buffalo and Little Buffalo Creeks formed in Lakes Whittlesey and/or Warren.

STOP 2. Huber and Huber sand pit.
Turn right into Huber and Huber sand pit. Observation and discussion of exposed Lake Warren beach and delta structures.

Beaches
Turn left (N) onto Town line Rd. and pass across beaches of Second Lake Warren, possible Lake Wayne 800' (.4 miles), and Lake Grossmere, 790;, (0.8 miles) beyond Clinton Rd.

Possible Lake Wayne beach
Possible Lake Wayne beach 800' (.4 miles from Clinton).

Possible Lake Grossmere beach
Possible Lake Grossmere beach 790;, (0.8 miles) beyond Clinton Rd.

Cayuga Creek
Cross unidentified beach ridge, 760', and Cayuga Creek, the eastern most river draining into Erie Basin. Proceed south over very subdued remnants of Alden Moraine. Borrow pits and cellar cuts reveal red, stony silts and normal clay till in this general region.

Ice contact deposits
Cross Ellicott Creek and turn left (W) onto N.Y. St. 33, Genesee St. Pass gravel pits in ice-contact deposits on right.

STOP 3. Pine Hill Concrete Co. sand and gravel pit.
Over 45' of ice-contact, stratified drift is exposed on the northeast corner. Thin layers of flow (?) till occurs at some horizons and the deposit is overlain by 7-10' of cobbly till in the northwest corner. This together with cross-bedding data suggest a possible (a) kame delta or (b) ice marginal stream origin. These and adjacent deposits may be related to the Buffalo Moraine of Kindle and Taylor (1913) .

Down Onondaga Escarpment
Proceed under Sheridan Dr. overpass and down Onondaga Escarpment to Lake Tonawanda plain, 630'. This area is largely underlain by lacustrine red silts and clays overlying Camillus Shale (U. Silurian). Scattered till ridges and drumlins project above its surface.

Crest of Niagara Falls Moraine
Cross over crest of Niagara Falls Moraine.

Drumlin
Turn right (E) onto Branz Rd. (Bartz Rd.) and proceed up onto NE-SW trending drumlin. This and next drumlin have no more than 35' of relief but stand out clearly from flat Lake Tonawanda plain.

Crest of NE-SW trending drumlin.

Hummocky ridges of Barre Moraine

Barre Moraine crests
Good crests of Barre Moraine, near stop light at Lincoln Ave., City of Lockport.

Barge Canal / Erie Canal
Cross N.Y.S. Barge Canal/Erie Canal at Lockport. Canal leads NE through one of Lake Tonawanda outlet spillways.

STOP 4. Outwater Park for lunch
Turn left onto Outwater Dr. and proceed to Outwater Park for lunch. The park lies on the Lockport Dolostone (M. Sil.) forming the prominent Niagara Escarpment overlooking glacial Lake Iroquois plain to north. Lake Ontario lies 11 miles to the north.

Spillway draining Lake Tonawanda
You are passing down from Niagara Escarpment through one of many spillways cut by water draining from Lake Tonawanda to Lake Iroquois.

Ridge Rd. follows the Lake Iroquois beach ridge
Ridge Rd. follows the Lake Iroquois beach ridge, 390'+; Lake Ontario stands at 246'.

Bar of Lake Iroquois.
Bear right following N.Y. Rt. 93 at fork onto bar of Lake Iroquois.

STOP 5. Abandoned gravel pit
Abandoned gravel pit exposes shingled gravel of Iroquois bar, lightly cemented with secondary calcium carbonate as to preserve details of imbrication, bedding, and cut-fill structure.

Iroquois Beach
Turn right (W) onto RL 104 Ridge Rd. and proceed along Iroquois beach to Lewiston. Note Niagara Escarpment prominently displayed at left is reached at Dickersonville, where rise begins from Iroquois plain, 400' to Tonawanda Plain at 600'+.

Proceed up Niagara Escarpment
Turn left (S) onto N.Y. Rt. 18, Creek Rd. at outskirts of Lewiston and proceed up Niagara Escarpment. After.4 mile note exposure of Lockport Dolostone at left and view to right of Escarpment, and the broad Lower Niagara River. Emerging from the Gorge at Cataract Basin, the river spreads out to a width of 2,000', flowing with a gradient of less than 0.16' per mile to Lake Ontario 6 miles to the north.

Cross Niagara River
Cross Niagara River into Canada with Old Narrow Gorge and power projects at left, Lewiston Branch Gorge Section and Cataract Basin at right.

Brock Monument
Turn right (S) at first exit after paying toll, and after .4 mile turn right again at intersection with Niagara Park Commission, "River" Road. Brock Monument, and Niagara Escarpment are at your left (N). Proceed south over Barre Moraine represented by hummocky relief .5 mile from the bridge toll stop.

Sir Adam Beck Niagara Generating Station No.2
Pass Sir Adam Beck Niagara Generating Station No.2, a facility of Ontario Hydro. From this area to the Whirlpool (Stop 7) we pass through a shallow channel of the Niagara R. from Lake Tonawanda to Lake Iroquois. The deposits are red Silts with grey clay layers overlying bouldery till.

STOP 6. Vista
Vista overlooking Gorge and Robert Moses Niagara Power Plant. Both Canadian and American Power Stations take their water from the Upper Niagara River. A clear view Of the Niagara stratigraphic section is revealed here from Queenston Shale to the Lockport Dolostone at the top. Proceed south along River Rd.

Wintergreen Flats and Niagara Glen
Pass Wintergreen Flats and Niagara Glen at left. Large talus blocks, some 20' in diameter and cut by giant potholes, lie below massive dolostone cliffs which remained when the retreating former Falls narrowed and gorge cutting resumed to the east.

STOP 7. Whirlpool Basin
Turn left off main road to the Whirlpool parking area. The Whirlpool is a basin 1,700' by 1,200' with a maximum depth of 125'. The water enters the Whirlpool at high velocities after moving up to 30' per second through the Whirlpool Rapids upstream. Most of the flow rushes past the outlet to the far side of the Pool, makes a complete circuit counterclockwise, and escapes through the narrow outlet by passing under the incoming stream. Below the Whirlpool, there is another two miles of rapids with a drop of 40'. The feature responsible for the Whirlpool is the buried St. David's Gorge, intersected here by the Niagara Gorge. It is observed trending northwest from the opposite side of the Whirlpool and extends to the village of St. David on the escarpment west of Lewiston. Various excavations for road, canal, and power projects reveal that it has steep sides and a depth approximate to that of parts of the Niagara Gorge. It has been filled by till, mantled with red lacustrine silts and gray clays probably related to the former Lake Tonawanda. The Middle and Lower Silurian section is clearly revealed here. The Whirlpool Sandstone is at the river level,

Cross Bowmen River
Continue south along River Road. Cross Bowmen River which has partially excavated St. David's Gorge.

STOP 8. Refectory view of falls
Refectory view of Upper Great Gorge, American Falls, Goat Island, and Horseshoe (Canadian)Falls at right. Goat Island divides the Upper Niagara River into two channels, one leading to the American' Falls and the other to the Horseshoe Falls. In each channel the water flows over resistant ledges of the southerly dipping Lockport Dolostone Caprock to form rapids and cascades with a drop of about 50'. Before construction of a submerged weir above the Cascades (Horseshoe Rapids), only five per cent of the total flow went over the American Falls; a little more than one half the present percentage. The relatively small flow is distributed evenly along the 1,1OO feet crest of the American Falls so that the discharge per feet rarely exceeds 20 cubic feet per second compared to a maximum of 200 at the Horseshoe. At the 2,500' wide crest of 510-520' above sea level, there is a straight drop of about 160'. The crest has been lengthened as much as 100' in the past 100 years because the central portion recedes faster than the ends. In some places along the crest, there are depths from 6 to 12' but there are several small islands and shoals. In particular, there is a large central shoal dividing the flow into two main channels, which converge toward the central part of the crest. The massive Lockport caprock of the Falls is clearly shown beneath the observer and between the two falls. It is some 80' thick here, thickening to 130' south at the Cascades head. The black Rochester Shales beneath are hidden by the falls and the blocky dolostone talus. The latter is not removed from beneath the American Falls because of the low discharge. The recession of these shales has caused undermining and consequent joint block by joint block retreat of the Falls from Lewiston. The river in the Upper Great Gorge below the Falls, drops only five feet in its two and one quarter mile length. Soundings show maximum depths of from 100' to 187'.

STOP 9. Horseshoe Falls and Scenic Tunnels.
Proceed south, passing the Cascades and Canadian Niagara and Toronto Power Plants successively on the left, and the river-cut cliff and shelf in the Niagara Falls Moraine at right. This latter cut, now occupied by Queen Victoria Park was probably made (Taylor,. 1932) after the Falls had retreated past the high point of land just north of Stop 7. At this time the curved course of the river in the rapids threw a powerful current against the bank west and south of the fall.

Niagara Falls Moraine
Turn right (W) encircling Dufferin Is. and skirting 60' cliff of Niagara Falls Moraine. Return north toward Rainbow Bridge past Falls.

Power Intakes
Pass Niagara River and Power Intakes for Robert Moses Power Project. Twin conduits, each 46' by 66', carry water four miles beneath the city of Niagara Falls, The concrete bulkheads held the closing doors for these conduits.

D: ONONDAGA LIMESTONE IN WESTERN NEW YORK
by Dr. Edward J. Buehler

D: ONONDAGA LIMESTONE IN WESTERN NEW YORK

STOP 1. Buffalo Crushed Stone Quarry
STOP 1. 9:00 A.M. See paper by Oliver (p. 32) for stratigraphic details. Leave Quarry at 10:00 A.M.

STOP 2. Onondaga Bioherm
STOP 2. Arrive at Quarry at 11:15 A.M. This quarry exposes an Onondaga Bioherm. See paper by Oliver (p. 32) for details. Leave quarry at 12:15 P.M.

E: HAMILTON FOSSIL LOCALITIES
by Harvey Hambleton
Buffalo Museum of Natural Sciences

E: HAMILTON FOSSIL LOCALITIES

STOP 1. Oatka Creek shale and Stafford Limestone.

STOP 2. Centerfield Limestone.
This is the most western outcrop of Centerfield.

STOP 3. Wanakah Shale and Ledyard Shale.

STOP 4. Tichenor Limestone and Wanakah Shale.

May 5-7, 1967
GUIDEBOOK FOR FIELD TRIPS
Editor
Russell H. Waines
HAMILTON COLLEGE
Clinton, New York

A: THE PLEISTOCENE GEOLOGY OF THE WALLKILL VALLEY
G.GORDON CONNALLY
S.U.N.Y. College at New Paltz
LESLIE A. SIRKIN
Adelphi University

A: THE PLEISTOCENE GEOLOGY OF THE WALLKILL VALLEY

Schunemunk Mountain
Railroad Underpass. Schunemunk Mountain, a northeasterly plunging syncline is on the left. This is the easternmost manifestation of typical Appalachian, ridge-and-valley topography.

Salisbury Mills and Moodna Creek
The village of Salisbury Mills with Moodna Creek close by on the left. Moodna Creek served as a major drainage-way for pro-glacial lake waters in the Wallkill Valley and controlled the 400 foot lake level reported by Adams (1934).

Home of Brotherhood Wineries
Washingtonville is the home of the Brotherhood Wineries, reputed to be the oldest in the country in continuing existence.

Post-glacial stream channel
Note the post-glacial stream channel cut in bedrock. This channel is the result of a drainage reversal caused by the deposition of a crevasse filling (moraine?) south of Chester. This stream originally flowed southward into Black Meadow Creek but now drains only the muck area north of Chester.

View of Chester Esker
The Chester Esker is on the right side of the road.

Chester Esker
The road ascends the 60 foot high Chester Esker. This esker has its crest at about 540 feet and evidently represents a channel that drained southward through stagnant ice, into the 500 foot lake in the southern Wallkill Valley. This channel was probably in existence during the building of both the Pellets Island and New Hampton Moraines.

STOP A-1 Gravel Pit
This gravel pit is operated by Chester Ready-Mix. It is part of a southward extension of the ice channel filling represented by the Chester Esker. Examine the relationship between ice-contact stratified drift, flow (?) till, and non-ice-contact drift. In addition, examine the exotic lithologies represented in the gravels.

Ice-margin
Turn left (west) on Route 94. The road essentially parallels an ice-marginal position between here and Florida, New York.

Muck farming
Cross Quaker Creek on small bridge. This is the main muck farming area of Orange County. The organic soil is the result of filling of a 500 foot pro-glacial lake with lake silts and then organic deposits. On approaching the ridge of till knobs to the west a change in color of the topsoil illustrates the change from muck soil (developed from the bog deposits), to Canandaigua soils developed from underlying lake silts and clays) to Cossayuna-Troy soils (developed from the till that underlies the lake deposits).

Drumlinized till ridges
Turn left (south) on the Pulaski Highway following the series of drumlinized till ridges.

STOP A-2 Lodgment Till
Examine the lodgment till exposed in the cut behind the Big Island Garage. This till appears similar in lithology, weathering profile and soil development to the Olean till of western New York.

Distal face of the Pellets Island Moraine
Note the distal face of the Pellets Island Moraine to the front and left. (North)

Proximal slope of the Pellets Island Moraine
The proximal slope of the Pellets Island Moraine is to left.

STOP A-3 Pellets Island gravel pit
This is the Pellets Island gravel pit of the Orange County Sand and Gravel Co. The undisturbed foreset bedding on the distal side of the moraine suggests deposition into the open water of the 500 foot lake level. Exploratory cores for the City of New York Port Authority show almost 100 feet of lake clay, overlain by 0-20 feet of organic muck south of the moraine. Large blocks of flow (?) till are periodically exposed on the proximal side confirming it as an ice-contact face.

STOP A-4. Berkman bog
Leave the buses and cross the road to the west. Walk up the gentle slope parallel to the stonewall until the trail becomes clear in the orchard. Follow the trail for about 1/4 mile before descending into the Berkman bog. The implications of the pollen record will be discussed in relationship with the deglaciation of the region and the drainage history of the bog.

STOP A-5. Phillipsburgh crevasse filling
Leave the buses and gather on the hill on the right side of the road. Observe the Phillipsburgh crevasse filling that trends to the northwest toward the Wallkill River. QUESTION: Why are there no drainage features nor ice-contact deposits to the south and east of this feature?

Crevasse filling on the left
Continue northwest parallel to the crevasse filling on the left and Route 17 on the right.
2010: Route 17 truncates the route shown on the Road Log. Returning to where Owen's Road crosses it gets us to the lunch stop.

Bridge across the Wallkill River.
The river flows on bedrock on the east bank.

STOP A-6 Gravel Pit
This is one of the gravel pits operated by E.Tetz & Sons. Examine the pebble lithology as contrasted with that seen at Stop A-1. QUESTION: What is the significance of the large boulders of Shawangunk conglomerate?

STOP A-7. Large Kettle Hole
Cross through the barbed wire fence on the left side of the road and proceed up the hill to the large kettle hole. Here the significance of the stagnant ice topography found in the Wallkill Valley will be discussed.

Plain of washed till
Turn left (east) on Stoney Ford Road. The road traverses a plain of washed till adjacent to the Wallkill River.

Kame complexes
Turn left (north) at the Stop Sign and drive through more kame complexes similar to stops A-6 and A-7.

Distal slope of the Circleville Moraine.
Ascend the distal slope of the Circleville Moraine. The relationship of this moraine to the Pellets Island and New Hampton Moraines is uncertain.

STOP A-8.
This is one of a number of gravel pits operated by the Dickenson Sand and Gravel Co. of Bloomingburg. Examine the drift lithology. The significance of the numerous crevasse fillings in the Shawangunk Kill Valley north of Otisville will be discussed.
2010: Construction of Route 17 truncates the route given in the road log. The path here will get to the same entrance onto Route 17.

Chester crevasse filling and Chester Moraine
The Chester crevasse filling and Chester Moraine are seen on the left. Camp La Guardia is located on the Chester Moraine.

Mass Wasting
Note the mass wasting evident in the till cut to the right.

Valley-choker Moraine
Note the massive valley-choker moraine to the right. This pit once displayed magnificent forest bedding toward the south.

B: THE ECONOMIC GEOLOGY OF THE MID-HUDSON VALLEY REGION
A diverse terrain endowed with a wide variety of avai lable mineral resources, sustained demand for these resources and economical means of transportation have combined to foster a dynamic mineral industry in the Mid-Hudson Valley region which has prospered since the early 19th century. Production valued at about 100 million dollars in 1965 accounted for approximately one-third of the State1s entire mineral economy. Of greater significance is the fact that the Mid-Hudson Valley's mineral production is concentrated in less than one percent of New York State1s total land area (47,944 square miles). The principal products are crushed stone aggregate, bui Iding stone, lightweight aggregate, sand and gravel, portland cement, natural cement and brick - materials all necessary. to bui Iding and highway construction.
Systematic geologic studies of the nature and use of rock raw materials have produced revolutionary changes in the economics of industrial mineral production in the Hudson Valley during the last decade. The result has been an increase of crushed stone reserves by a factor of 3 to 5, cement reserves by a factor of 5 to 10 and lightweight aggregate reserves from nothing to well over a billion tons. This represents another example of taking what is available and utilizing it all, by separation or by blending, for the most useful purpose. The economic rock section ranges in age from Cambrian to Middle Devonian (Tables Bl and B2).
Trip B is specifically planned to allow participants the opportunity to examine in a day's time the greatest variety of rock raw materials and mineral commodities typical of the Mid-Hudson Valley. The following U.S. Geological Survey 7 .5-minute topographic quadrangles cover the route of the trip in order: Newburgh, Wappingers Falls, Poughkeepsie, Hyde Park, Kingston East, Kingston West, Rosendale and Clintondale.
JOHN H. JOHNSEN
Vassar College
SIMON SCHAFFEL
The City College of New York

B: THE ECONOMIC GEOLOGY OF THE MID-HUDSON VALLEY REGION

STOP 1: Shale quarry and clay pit
Shale quarry and clay pit of the Beacon Brick Corporation Exposed in the quarry are grayish-black, red and green slaty shales of the Normanskill Formation (Table Bl) which are blended with clay to manufacture brick. Note slaty cleavage parallel to bedding. Hudson Valley brick is produced by either the "soft mud" or "stiff mud" process. "Soft mud" brick is made from clay to which an excess of water has been added to secure plasticity. The soft mud is placed in wooden molds which have been dusted with sand and the clay is allowed to dry before firing. Extreme care must be exercised to avoid drying cracks and shrinkage. The "stiff mud" process is used most frequently by the modern brick industry. Highly plastic clays are undesirable for this process so that ground shale is usually added to the mix. The stiffer clay or clay-shale mix is extruded through a rectangular die and bricks are cut off by taut wires. These unfired bricks, being stiffer, can be handled with less danger of deformation. Proceed to clay pit. Exposed in the pit is clay that represents fine mud deposited in one of many meltwater lakes that occupied the Hudson Valley during the retreat of the ice in the Late Pleistocene. The clay is normally bluish gray but it may be yellow when weathered due to the oxidation or iron. Thin beds and lenses of sand are frequently inter-stratified with the clay. The thickness of the clay is variable in this region, but it may exceed 200 feet in some localities. This glacial clay is well adapted to brick manufacture. It is plastic and usually has sufficiently large proportions of fluxing agents - such as alkalies, iron, lime and magnesia - to permit vitrification at relatively low temperatures. The finished product is generally red or pink in color. The Beacon Brick Corporation uses a clay-shale mix to make extruded wire-cut brick. Firing takes place in a tunnel kiln having a capacity of 100,000 bricks per day. The chief market area is New York City with transportation by barge. Lightweight aggregate is manufactured from shale or clay by heating these materials until they expand to form porous, scoriaceous material by the evolution of gas bubbles at elevated temperatures (see Stop 3). The Normanskill Shale is considered a potential source of lightweight aggregate raw material; however, pilot tests of the shale from this area yielded an unsatisfactory product because of the lack of compositional uniformity and the large amount of micro- and mega-structural diversity. The slaty cleavage caused slivery rather than equidimensional fragments on crushing which produced a pleated appearance on bloating similar to expanded vermiculite. Although this structure does not necessarily result in an aggregate of low strength, it does make a less attractive aggregate in terms of consumer acceptance. So far as is known, there has been no attempt to produce lightweight aggregate from Hudson Valley clay.

STOP 2: Clinton Point Quarry
New York Trap Rock Corporation, Clinton Point Quarry Plant Office and loading dock. Hard hats will be loaned to those participants not bringing them. The borrowed hats will be returned at Nytralite Aggregates, Inc. (Stop 3).
Two belts of dolostone suitable for crushed stone aggregate occur along the Hudson River in the lower reach of the Mid-Hudson Valley (see Lower Hudson Sheet, Geologic Map of New York State, 1961). The southern most of these two belts follows the northern margin of the Hudson Highlands north-northeast from the vicinity of Beacon to the eastern portion of Dutchess County where it veers more northerly, eventually crossing into northern Connecticut and Massachusetts; the other belt begins B6 southwest of Newburgh and also trends north by northeast to cross the Hudson at New Hamburg (situated at the mouth of Wappinger Creek) where it occurs in two distinct bands over a short distance and continues in the same north-northeasterly direction to the upper part of Dutchess County.
The rocks take their name, Stockbridge Group, from Stockbridge, Massachusetts, where the northeastern extension of the southernmost belt has been metamorphosed to marble. In the field trip area, the carbonates are unaffected by metamorphism and frequently are referred to as the Wappinger Group, a name well established in the literature. The Stockbridge succession includes carbonate rocks that are Late Cambrian to Early Ordovician in age although that part of the succession in the vicinity of the Hudson River may be all Cambrian. The sequence includes a series of dense to finely crystalline, gray dolomitic rocks ranging from dolomitic limestone to dolostone which collectively are calcitic dolostones.
At Clinton Point, the rock is dolostone, with a magnesium carbonate content of 38.16 percent. Here the New York Trap Rock Corporation, a subsidiary of the Lone Star Cement Corporation, produces every conceiveable size of stone ranging from riprap to stone sand and screenings.
The quarry opening is effectively blocked from river view by a 500-foot wide buffer zone or "mercy strip". The dolostone reportedly extends to considerable depth and a portion of the quarry floor is now 60 feet below the level of the Hudson River. Downward development is possible because the rock in the buffer zone is sufficiently tight to hold back the river water.
Two inactive quarries are located in a different part of the dolostone sequence on the west bank of the Hudson opposite New Hamburg at Cedar Cliff. In these quarries the dolostone is locally characterized by considerable chert of a variety that is known to have a deleterious effect when used as concrete aggregate. If reopened, selective quarrying would be necessary until new advances in concrete technology nullify these effects. There is no reason why other applications are not possible, provided the rock meets the necessary specifications.

STOP 3: Nytralite Aggregate, Inc. Quarry
Nytralite Aggregate, Inc. - Quarry and Tour of Plant Nytralite Aggregates, Inc. is one of the leading producers of lightweight aggregate in the Mid-Hudson Valley. Lightweight aggregates are special materials incorporated with cement in the manufacture of concretes- which range in weight from 120 pounds per cubic foot to less than 62 pounds per cubic foot. The latter is able to float on water. By comparison, conventional concretes containing other aggregates, such as crushed carbonate rock seen at Stop 2, weigh about 150 pounds per cubic foot. Lightweight aggregate is used in substantially more than half of the concrete block produced in the United States. The desirable properties gained by this usage are: lightness, high strength-to-weight ratio, low shrinkage, low thermal conductivity, good acoustical properties, a coefficient of expansion similar to that of steel and low production costs. The use of lightweight aggregate in the concrete roadway of San Francisco-Oakland Bay Bridge reduced the cost of steel by three million dollars. Lightweight aggregate may be manufactured from clay or shale by heating these substances until they expand to form porous, cinder-like materials. Expansion is a bloating process in which two conditions occur simultaneously. Upon firing, the clay or shale fuses to form a viscous liquid, while at the same time, a gas, released as a result of mineral decomposition, becomes entrapped within the viscous mass. If the gas-producing mineral, or minerals, decomposes before any appreciable liquid formation takes place, expansion will not occur, as the gas will escape through the open-pore structure. Satisfactory expansion also will not occur if the gas is evolved at temperatures much greater than the softening point, as the gas will again be lost because the melt will be too fluid to retain it. If, for some reason, the gas is retained under this condition, cells may be too large and their walls too thin for good strength. Non-bloating argillaceous materials can often be induced to expand by adding pulverized coal and pelletizing into desired size prior to ignition. The rock most suitable for the manufacture of lightweight aggregate is a massive, somewhat silty (arenaceous); unweathered shale of uniform quality. It may contain a small amount of calcite, either disseminated or as thin veinlets, and a little pyrite. Slaty cleavage should not be well developed, but it causes no problem in its incipient stages. This type of rock yields a good, uniform aggregate of adequate strength and an acceptable appearance. It bloats at approximately 2000 degrees F. The Esopus Shale exposed in the Nytralite quarry fits this description. Note the gentle dip of the massive beds to the southeast (north face) and nearly vertical cleavage (east face). The quarry is located on the gently dipping western limb of an asymmetrical syncline, the axial planes of which dips to the southeast. The trace of the axial plane is roughly parallel to the crest of Fly Mountain. Fly Mountain is basically a northeast-trending asymmetric synclinal ridge characterized by a number of similarly-trending subsidiary folds. It is composed mainly of Late Silurian and Early Devonian carbonate rocks {Figures B3, 84} which have been thrust northwestward over the Esopus Shale along multiple faults. Exit quarry. Cross Route 32 and proceed up road to plant. Exit buses and proceed on foot. Note initial test quarry in Esopus Shale to north. Walk up hill, noting the carbonate rocks, to primary crusher and Plant Office. Route essentially parallels the section given in Figure B4. Plant Office. Lunch stop and tour of plant. Refer to flow diagram {Figure B5}.

STOP 4: Natural Cement Mine, Century Cement Mfg. Co.
Natural cement is produced by calcining an impure, argillaceous limestone or dolomitic limestone containing from 15 to 40 percent silica, alumina, and iron oxide at a comparatively low temperature (about 14000 F.) so that decarbonation but no fusion takes place. The burned mass will not slake if water is added, but when ground to a powder it will harden rapidly with the addition of water. Natural cement acquires most of its untimate strength in 5 years and only one-eighth of its ultimate strength in 7 days whereas most portland cements approach their ultimate strength in one year and reach 65 to 75 percent of their ultimate strength in 7 days.
In the United States, the cement industry began in 1818 with the discovery of natural cement rock near Chittenango, New York, by Canvass White. White applied to the State of New York for exlcusive rights to manufacture the cement for 20 years. His request was denied but the State awarded him $20,000 in recognition of his valuable discovery. The cement was used in the construction of the Erie Canal.
In 1825, during the building of the Delaware and Hudson Canal, a natural cement rock was discovered here at Rosendale. Work was progressing along the route of the canal through the farm of Jacob L. Snyder when it became necessary to blast through some rock. The rock, as blasted, had the appearance of limestone and fragments were taken to a blacksmith shop at High Falls to produce lime. The stone was burned in the forge and attempts to slake it were made by adding water. The calcined material, soft and chalky after burning, did not slake but instead, after a few hours, lost all of its chalkiness and began to harden. It had been planned to obtain the cement necessary for the canal locks from Chittenango but with the discovery of cement along the route, a contract was awarded to a Mr. John Littlejohn to supply the canal's needs. Littlejohn built a "pot" kiln in which the burning of each charge was a separate operation. The pot kiln was a shaft excavated in the side of a hill and lined with cement rock. At the base of the kiln, an "eye" or shaft at a right angle to the main shaft was filled with cordwood and an arch of large cement rocks, to act likea grate, was formed just above the cordwood. The kiln was then filled with cordwood and an arch of large cement rocks, to act like a grate, was formed just above the cordwood. The kiln was then filled with broken cement rock and the cordwood ignited. The burning continued until the highest stone in the kiln was calcined (5 to 6 days) and then the entire charge was withdrawn. The kiln was then recharged and the procedure repeated.
The charge, as drawn, contained some raw and some over-burned materials. These were carefully removed and the raw material was used in the next kiln charge while the over-burned material was discarded. This procedure was necessary not only from a technical standpoint but also from a mechanical one. The mill equipment would grind neither the hard over-burned clinker nor the hard under-burned stone. The grinding equipment was fashioned on the same principle as a grist mill, utilizing millstones made from the quartz pebble conglomerate or "grit" of the Shawangunk Formation. The growth of the natural cement industry fostered a sizeable millstone business. The rocks in the Rosendale district are so intricately folded and faulted that natural cement raw materials crop out almost everywhere. Repeated exposures are clearly indicated by the many abandoned mines in the region and it is obvious that the early miners knew what to look for. The natural cement rock was at first quarried but eventually it became necessary to drive headings and open a mine where the dip carried the desired rock below the surface. To aid visibility, it was customary to mine down dip a certain distance, return to the outside, and create a similar new opening 30 feet or so along the strike. These headings would then be worked at right angles until they were connected. The procedure was repeated again and again, leaving a series of adits, which provided the light to work with, separated by 30-foot pillars. As it became necessary to penetrate deeper underground, illumination was provided by kerosene torches and the miners copied from their successful adits the scheme of leaving 30-foot pillars to support the roof. This room and pillar arrangement is clearly demonstrated in the Century Cement mine.
Natural cement production in the United States grew from 100,000 bbls. a year in the 1830's to 10,000,000 bbls. per year in 1899. At the peak of the industry, in the Rosendale district, some 20 plants employed 5,000 men and turned out 4,000,000 bbls. per year.
About 1894, portland cement, a carefully controlled blend of cement raw materials to insure uniformity, came into general use. In 1900 production of natural cement and portland cement was identical, 8,500,000 barrels each. During the early 1900's, the first large structure of its type to be entirely constructed with portland cement was the Boonton Dam in New Jersey. The Boonton Dam was to be a part of the water supply of Jersey City and Rosendale natural cement was originally specified for its construction. However, a director of the Alpha Portland Cement Company was a member of the Board of Water Supply and he proposed to supply the Jersey City job with portland cement from his company at the same cost as Rosendale natural cement. The dam was built with portland cement. Then portland cement gained ascendency over natural cement anq by 1910 natural cement production throughout the United States was reduced to about 1,000,000 bbls. The plants began to close down after the start of the 20th century and by 1920 only one plant remained in the Rosendale district - Century Cement. In fact, this company is the only producer of natural cement in the United States today and that on a limited basis. The natural cement produced in the Rosendale district is a low lime, high silica, high magnesia, hydraulic cement of pozzolanic properties. A typical chemical analysis of the raw cement rock (Rosendale Member of the Rondout Formation) mined by Century Cement is:
SiO2 | 17.5
Al2O3 | 5.0
Fe2O3 | 2.8
CaCO3 | 41.5
MgCO3 | 31.5
Alkalies | 1.7
| 100.0%
The working faces are now about half a mile from the mine entrance and slightly more than 100 feet below the surface. Production is presently limited to the Rosendale Member.
A significant portion of the mined-out lower level has been leased for the underground storage of vital records. Construction of vaults and other preparations are in progress.

C: MIDDLE AND UPPER DEVONIAN CLASTICS OF THE CATSKILL FRONT, NEW YORK
The Middle and Upper Devonian of the Catskill Mountains region of southeastern New York consist of approximately 8000 feet of strata which commence with limestones at the base and grade upward through black shales, gray siltstones, gray sandstones, red beds, and, at the top, conglomerates (Fig. 3). The lowermost 2000 feet (Onondaga, Bakoven, and Ashokan Formations) are described by Chadwick (1944, p. 94-116). The purpose of this field trip is to examine the red bed-gray sandstone and conglomerate facies or depositional phases (Rickard, 1964) that have been referred to as "Catskill."*
*Rickard (1964) calls the conglomerate phase "Pocono."
FRANK W. FLETCHER
Susquehanna University

C: MIDDLE AND UPPER DEVONIAN CLASTICS OF THE CATSKILL FRONT, NEW YORK

STOP 1. (15 minutes) Onondaga Limestone (Middle Devonian).
This is primarily a stop for introduction to the basic Middle and Upper Devonian stratigraphic sequence of the Catskill Mountains region (see p. C1-C8). The Onondaga at this locality consists of very cherty, fossiliferous limestone. It dips toward 258° at 13°0 and forms a low escarpment. An excellent panorama of the chief physiographic elements of the region can be observed from this location. The topographic depression directly west of the Onondaga escarpment is Bakoven Valley, which is underlain by the relatively soft black shales of the Bakoven Formation. The low Hoogeberg range west of Bakoven Valley is composed primarily of resistant siltstones of the Mount Marion Formation and is capped by the Ashokan Sandstone. The plain beyond the Hoogebergs is underlain at its most easterly part by the upper Ashokan Formation and at its westerly edge by red beds of the Plattekill Formation. Towering above all of these elements is the Catskill Front; and, beyond, the high peaks of the Catskills including Slide Mountain, Wittenberg Mountain, and Cornell Mountain, whose summits are composed of the Slide Mountain conglomerate (Fig. 4).

STOP 2 (60 minutes) Manorkill and Gilboa Formations.
Buses will allow field trip participants to disembark and then will drive to top of section. Participants will walk along right (north) side of highway to top of section. CAUTION: Road is narrow, so "cling" to side.
The upper part of Kaaterskill Creek can be seen approximately 0.2 miles northeast of this locality. This is the location of Prosser's classic example of stream piracy, where the headwaters of Schoharie Creek were captured by the much-steeper gradient Kaaterskill Creek.
Figure 13 describes the stratigraphic section of this stop. Many of the typical rock types and sedimentary structures of the lower Catskill facies can be observed here. Especially note-worthy are the fining-upward cycles discussed on page C1.

STOP 3 (90 minutes) CONTINENTAL SEQUENCES IN THE PROXIMAL GENESEE GROUP
LUNCH (40 minutes) Guest Lecture by PETER J.R. BUTTNER Computing Center, University of Rochester
Follow NYSGA trail markers along rim of Catskill Front to outcrop of the "Twilight Park Conglomerate." CAUTION: Watch your footing along the Front. Please remain at least five feet back from the edge of the ciff. NO SPECIMENS MAY BE TAKEN FROM WITHIN THE PARK BOUNDARIES.
Trail lies on strata of the lower Oneonta Formation. Note crossbedding, excellent jointing and joint-controlled face of the Catskill Front. An excellent view of the Hudson Valley, the low Taconics, and, on very clear days, the Berkshires is available from the Front.
Return along trail to buses and field trip headquarters.

D:UPPER SILURIAN-LOWER DEVONIAN STRATIGRAPHIC SEQUENCE, WESTERN MID-HUDSON VALLEY REGION, KINGSTON VICINITY TO ACCORD, ULSTER COUNTY, NEW YORK
The remarks concerning the Upper Silurian and Lower Devonian stratigraphic units described in this paper largely pertain to strata within the Field Trip area (Fig. 1) extending in a belt from Accord (Stop 9) northeast to just beyond Kingston (Stops 1 and 2). The entire belt appears to be underlain with angular unconformity by a disrupted sequence of graywackes and shales to the northeast (Austin Glen affinity) and shales and siltstones to the southwest (Snake Hill affinity). The relations of these two lithologic groups in this area are not clear but it does seem that both were somewhat uplifted and folded (if not faulted) during the Taconian Orogeny; by latest Middle Silurian (?) the Ordovician sediments and structures were eroded to a surface of seemingly low relief or uniform slope. Subsequently a sequence of conglomerate (Shawangunk), shale (High Falls), sandstone (Binnewater) and carbonate (Rosendale-Wilbur) was deposited on the erosion surface in an apparent, general progress ion to the north east.
From Rosendale-Wilbur times through the remaining Late Silurian and Early Devonian the region was generally covered by marine waters, although intertidal and supratidal conditions existed intermittently on a local to regional scale. The Late Silurian and Early Devonian strata are relatively uniform in lithology and thickness throughout the area but some local and regional differences in depositional environments are evidenced within the Rondout, Thacher, Connelly and perhaps other formations. Apparent throughout the Rondout-Lower Devonian sequence is a more or less rhythmic alternation of variously interrelated, high energy-low energy, clay-carbonate, "shallow water"-"deep water", marine environments of deposition.
RUSSELL H. WAINES
S. U. N. Y. College at New Paltz
FLORENCE GROSVENOR HOAR
Winthrop, Maine

D:UPPER SILURIAN-LOWER DEVONIAN STRATIGRAPHIC SEQUENCE, WESTERN MID-HUDSON VALLEY REGION, KINGSTON VICINITY TO ACCORD, ULSTER COUNTY, NEW YORK

Toll Booth, NYS Thruway Interchange 17 (Newburgh).
Proceed north (right) onto Thruway toward Albany. Between Newburgh and New Paltz occur occasional road cuts in Ordovician (Martinsburg-Snake Hill (?)) slates and siltstones. Note the generally progressive decrease in degree of foliation of the beds northward.

NY 299 overpass near NYS Thruway Interchange 18 (New Paltz).
North of New Paltz the degree of foliation in several extensive road cuts in the Ordovician shales is much less pronounced than further south. A fauna found in Ordovician beds north of New Paltz shows affinities with that of the Snake Hill Shale (Late middle Ordovician).

Wallkill River
Wallkill River cutting Ordovician shales and siltstones on the right.

Rondout Creek cutting Ordovician shales and siltstones.
Rondout Creek cutting Ordovician shales and siltstones. Lefever Falls (rapids) on the left. This is about the northernmost extent of Ordovician outcrops along the Thruway in the field trip area (Fig. 1).

Underpass NY 32.
For the next 5.3 miles there are intermittent outcrops and road cuts in a more or less regularly ascending order of formations from Kalkberg (Lower Devonian) through Onondaga (Middle Devonian). High speed traffic does not permit close observation.

Esopus Creek.

Extensive road cuts
For the next 2.1 miles are extensive road cuts in gently dipping siltstones and shales of Mt. Marion Formation (Middle Devonian).

Mt. Marion (?) outcrop north of road and east of creek.
Bridge over Esopus Creek.

STOP 1: Road Cuts
STOP 1a: Road Cut in Esopus and Schoharie Formations. Pull off onto north side of highway with care. On this trip (Stops 1A-C) do not cross over onto south side of highway because of high speed traffic. Observe anticlinal exposure of upper (40-45') of Esopus Shale to the west and synclinal exposure of Schoharie Formation to the east. Contact between the two formations is covered but contacts, lithologies and thicknesses of the Carlisle Center, (including Black Bed), Aquetuck and Saugerties Members of the Schoharie can be observed. Fossils are best collected from the Saugerties Member. Sections of the feeding burrow Zoophycos cauda-galli are common in the Esopus Shale and Carlisle Center Member. Total extent of road cut is about 0.3 miles. Proceed east on foot along north side of highway right-of-way about 0.5 miles to the next stop.
STOP 1b: Road Cut in Glenerie, Port Ewen, Alsen and Becraft Formations: In this anticlinal exposure a partial section of Glenerie Formation and complete or almost complete sections of the Port Ewen and Alsen Formations can be closely examined on the western flank. A partial section of Becraft Limestone is exposed in the core of the structure. Although the contact between the Glenerie and Port Ewen Formations is covered, the Connelly Sandstone which intervenes to the south does not seem to be present here. The Port Ewen-Alsen-Becraft contacts are well-exposed. Some fossils can be collected in the Glenerie, Alsen and Becraft Formations. This road cut extends about 0.1 miles.
Proceed east on foot along north side of highway right-of-way about 0.2 miles to the next stop.
STOP 1c: Road Cut in New Scotland, Kalkberg, Ravena and Thacher Limestones: In this road cut a sequence of west-dipping beds are exposed. From west to east these are: the New Scotland Formation (incomplete); the Kalkberg Limestone with its two members, the Broncks Lake and Hannacroix (complete); the Ravena Limestone, sole representative member of the Coeymans Formation (complete); and the Thacher Limestone, sole representative member of the Manlius Formation. The Thacher-Ravena-Kalkberg and possibly Kalkberg-New Scotland contacts are well-exposed. Fossils can be collected from all formations or members, but especially the New Scotland Formation. The brachiopod Gypidula coeymanensis is noteworthy in the Ravena and Hannicroix limestones but is difficult to obtain whole. Stromatoporoids are noteworthy in the Thacher Limestone.
This road cut extends about O. 1 miles.

STOP 2: Wilbur, Austin Glen, Roundout, Thacher, Revena fms
STOP 2a: Road Cut Exposing Wilbur Limestone - Austin Glen (?) Graywacke Angular Unconformity: Because of high speed traffic please do not cross highway on this trip. Here is exposed a slightly folded, but largely horizontal, bed of Wilbur Limestone (lowermost member of the Rondout Formation) in distinct angular unconformity with underlying graywackes of possible Austin Glen affinity. It is possible that the unconformity is actually a fault but the same relations obtain too often elsewhere to make this likely. Some fossils may be extracted from the Wilbur Limestone. Coenites is abundant locally.
Proceed with care on foot south along NY 32 about O.1 miles.
STOP 2b: Road cut, Austin Glen (?), Rondout, Thacher and Ravena Formations and Members with Structural Complications. Watch for falling rocks. This road cut extends for the next 0.3 miles. Starting from the north end there is a stratigraphic succession from Austin Glen (?) through Ravena Limestone which is somewhat complicated in the north half of the cut by faulting. Individual stratigraphic units are well exposed but Figure 4 should be consulted in order to verify their structural relations. The following Formations or Members are present and their lithologies and contacts (/) indicated:
Ravena ls./Thacher ls./Whiteport dol./ Glasco l./ /Rosendale dol./Wilbur ls.?Austin Glen (?) graywacke
A few fossils may be collected from all units except perhaps the Whiteport and Rosendale dolomites and the Austin Glen (?). Especially noteworthy are Cystihalysites and stromatoporoids in the Glasco limestone.

Intermittent Outcrops and Road Cuts
From the south end of STOP 2b (39.4 miles) south to the intersection of NY 32 and US 9W (42.3 miles) there are intermittent outcrops and road cuts in a more or less regularly ascending stratigraphic order from Austin Glen (?) through Onondaga Formations. The overall picture is somewhat complicated structurally. Of especial note however, is a two to three foot bed of Connelly Sandstone exposed at the south end of a road cut on the east side of the highway about mile 40.6 of this trip. Traffic does not permit close observation from a bus.

Trailways bus depot. Rest Stop.

STOP 3: City of Kingston Wilbur Gravel Pit
Standard Reference Section of the Rondout Formation and Type Section of the Wilbur Member; Intercalation of the Wilbur Member with Rosendal Member; Binnewater Sandstone disconformably underlying the Rondout Formation and overlying the Ordovician Austin Glen graywackes and shales in angular unconformity. Walk up road to gravel pit (northeast) about O.1 miles. The cliff to the northwest is formed of an extensive sequence of Upper Silurian and Lower Devonian strata (mostly carbonates) partly repeated by faulting. Rickard (1962, p. 30) suggested that the standard reference section for the Rondout Formation be located in this quarry and Hoar and Bowen (1967, p. 4) designated this locality as the type section for the Wilbur Limestone Member which here inter-tongues with the Rosendale Member (Fig. 2). Disconformably underlying the Rondout Formation is the Binnewater Sandstone which is absent further north (STOP 2a, 2b) and which, at the present stop, overlies graywackes and shales of Austin Glen (?) affinity with angular unconformity.

STOP 4: Road Cut NY 32, Bloomington Vicinity; Glenerie, Connelly and Port Ewen Formations:
Here is exposed an almost continuous sequence of northwest-dipping beds of the upper part of the Port Ewen Formation (up hill) through the Connelly Sandstone into the lower part of the Glenerie Formation (downhill). The Connelly Sandstone has thickened considerably from the two or three foot exposure about one mile south of Stop 2a. Layers of abundant brachiopods exposed in section can be seen in the Glenerie limestones but collection in the round will prove difficult.

STOP 5: South End Quarry Hill
Binnewater Sandstone - High Falls Shale - Shawangunk Conglomerate - Snake Hill ? Sequence: Examine the disturbed siltstones and shales of Ordovician Snake Hill (?) aspect then examine the northwesterly dipping partly covered sequence of beds between the quarry and the edge of the mine pit to the west. Don't crowd edge of pit! From west to east the formations present are: Binnewater Sandstone (partly covered), Highfalls Shale (largely covered), Shawangunk Conglomerate, Snake Hill (?) shales and siltstones. The Binnewater-High Falls contact is covered but the High Falls-Shawangunk-Ordovician shale contacts are fully exposed. Noteworthy is the two to three foot thickness of Shawangunk Conglomerate and its relatively dark color (typical of the top of the formation locally). Also of note is the first two or three feet of shale beneath the conglomerate. This shale seems to differ from more typical Ordovician shales which underlie it. The mine pit to the west is excavated in a fault-complexed body of Rosendale Dolomite. The far wall (west) of the pit from bottom to top reveals a normal sequence of Glasco Limestone (ledge), Whiteport Dolomite (lower portion mined out) and lower part of the Thacher Limestone (upper part of the cliff).

Abandoned natural cement kilns on roadside to right.
Turn sharp left into open field and head toward distant kilns to the west by following dirt road left then right.

STOP 6: Fourth Lake; Rosendale Member Type Section
Fourth Lake; Rosendale Member Type Section; Ordovician, Snake Hill (?) Shale, High Falls Shale; Rondout Formation; Thacher Limestone (part) Sequence:
Park in front of kilns. Walk uphill to the right (north) over a glaciated shale outcrop of Snake Hill (?) affinity, then bear northwest over rubble pile and continue west at top of hill to New York Central Railroad tracks. Total distance is about O.1 miles.
Walk north right about 0.05 miles along track to rai I road cut in Ordovician shales of Snake Hill (?) affinity. Retrace steps south about 0.07 miles along west side of track examining soil of covered interval for first signs of red shale particles (High Falls). Because traces of the Shawangunk Conglomerate are lacking and because the formation is not exposed locally, it is assumed that the High Falls Shale is in direct contact with the Ordovician shales even though the contact is covered at this Stop and not exposed locally. Continue walking south to the partly covered contact between the High Falls Shale and the Binnewater Sandstone. For the next O.1 miles in the railroad cut along the west side of the track is exposed a continuous sequence of northwest-dipping strata including uppermost High Falls (north) through Binnewater, Rosendale, Glasco, Whiteport and lower Thacher (south) members and formations. Examine the various units in light of general descriptions in the text. Contacts between units should be observed - some with caution. Except for pillars the bulk of the Rosendale and lower Whiteport members has been mined out. Please do not fall into the pits. Hoar and Bowen (1967, p~ 4) has designated this locality the type section of the Rosendale Dolomite Member of the Rondout Formation.

STOP 7: Williams Lake
Williams Lake; Rondout Formation; Binnewater Sandstone; High Falls Shale; Shawangunk Conglomerate Sequence: For the next 0.1 miles north in the railroad cut on both sides of the track is exposed a continuous sequence of westerly-dipping strata which include the Whiteport (south) through Glasco, Rosendale, Binnewater, High Falls and Shawangunk (north) members and formations. The various units and their contacts (where exposed) should be examined in light of general descriptions in the text. The Shawangunk Conglomerate, apparently absent at Stop 6, is well-developed here as well as locally, but the Shawangunk-Ordovician angular unconformity is not exposed.

Rosendale Hill lies directly ahead.

Century Cement Company natural cement kilns on right.
These are still in occasional operation.

Extensive cliffs on right are formed by New Scotland Formation.

STOP 8: High Falls, NY 213 Road Cut
High Falls Shale - Shawangunk Conglomerate Contact: Examine slightly anticlinal, light-colored exposure of Shawangunk conglomerate along extent of road cut (about 0.05 miles). Note the High Falls - Shawangunk contact at the east end of the cut (uphill) and determine whether it is distinct, conformable, gradational and/or interbedded. Note the dark color of the uppermost conglomerate layer.

Delaware and Hudson Canal
Sign on right noting the discovery of natural cement at nearby Bruceville in 1818. Just ahead is a section of the Delaware and Hudson Canal. The recently formed (1966) Delaware and Hudson Canal Historical Society plans to restore to operating condition some of the canal locks at High Falls. The canal played an important part in the transportation of natural cement and coal in the latter half of the nineteenth century.

High Falls and Central Hudson generating facilities on the right.
The face of the falls is formed of the Glasco Limestone and Rosendale Dolomite members of the Rondout Formation. Extensive exposures of Binnewater Sandstone and High Falls Shale occur from the base of the falls downstream.

Outcrops and Road Cuts
Outcrops and road cuts for the next 0.4 miles reveal a succession of strata from the New Scotland Formation (north end) through the Whiteport Dolomite in the bed of Kripplebush Creek at mile 62.5 (south end).

STOP 9: Abandoned New York, Ontario and Western Railroad Cut at Accord
Glasco Limestone (part), Rosendale limestones and Bossardville ? Formation (Accord Shale) Sequence: Walk a short distance southeast over abandoned road and descend into abandoned railroad cut. Walk to east end of cut. Walk west in cut and observe the following sequence: stromatoporoidal limestone of the Glasco Member overlying highly calcareous Rosendale member (compare with Rosendale at Stops 2, 6 and 8) which contains a highly arenaceous unit at the base and which overlies a laminated soft-weathering argillaceous dolomite and dolomitic shale (compare with Binnewater Sandstone and thin interbedded shales at Stops 6 and 7). The argillaceous, dolomitic beds here are tentatively assigned to the Bossardville Formation. They have also been referred to as the Accord Shale (Fisher, 1960). Extent of cut is about 0.1 miles. Time permitting, visits may be made to nearby quarries in the Rosendale limestones and in the Thacher and Ravena limestones.

Quarry in Rosendale limestones
On left is entrance to quarry largely excavated in Rosendale limestones. Road skirts northwest side of quarry.

Outcrop of Shawangunk Conglomerate on left.

Ascend the Shawangunk Mountains
Begin ascent of the general dip slope of the Shawangunk Mountains. For the next 6.1 miles the Shawangunk conglomerates and orthoquartzites which, in effect, sheath the Shawangunk Mountains, crop out extensively giving rise to typical Shawangunk Mountain topography.

Ordovician shales of Snake Hill (?) aspect
Ordovician shales of Snake Hill (?) aspect on the right. This exposure is part of an Ordovician shale window in the Shawangunk Conglomerate. Several years ago a very deep, very dry, wildcat was drilled in this window.

Lowermost part of the Shawangunk Conglomerate
Bridge underpass. Lowermost part of the Shawangunk Conglomerate is exposed in the road cut just east of the bridge.

Begin descent
Exposure of Ordovician shales of Snake Hill (?) aspect to the left. View of the Mid-Hudson Lowlands to the east and on a clear day, the Hudson Highlands to the southeast. Begin descent of Shawangunk Mountains.

Eastern face of Shawangunk Mountains
Shear cliffs of the eastern face of Shawangunk Mountain cuesta tower on the left, capped by almost two hundred feet of conglomerate and orthoquartzite. These cliffs are much used for practice in mountain-climbing as they present most, if not all grades of climbs. On weekends and holidays the cliffs are well populated with climbers from many states and Canada. The sport is not without risk; at least two climbers have "come off" here in the last three years.

Ordovician shale and siltstones of Snake Hill (?) affinity.
Proceed northeast through countryside underlain by Ordovician shale and siltstones of Snake Hill (?) affinity.

E:GEOLOGIC STRUCTURE OF THE KINGSTON ARC OF THE APPALACHIAN FOLD BELT
The Appalachian orogen when observed in its areal extent from Alabama to Newfoundland shows in its pattern a series of arcs, some bowed northwestward toward the foreland, others bowed inward toward the eugeosynclinal belt. One of the more prominent of these arcs, bowed eastward and southeastward toward the crystalline core of New England, is located at Kingston, New York, its hing-zone being situated in the old Rondout and Wilbur districts of the City of Kingston. The western extremity of the arc lies in the vicinity of Rosendale, and in its northern extension continues to the environs of East Kingston and the Kingston-Rhinecliff Bridge on the Hudson River.
The type of deformation evident within the Kingston Arc may be of some interest to the structural geologist and the purpose of this field trip is to observe the geologic structure at several localities where exposures are favorable.
GEORGE R. HEYL, S. U. N. Y. College at New Paltz
MORRIS SALKIND, Saugerties High School

STOP I: The Nytralite Quarry on Route 32
STOP I: The Nytralite Quarry on Route 32 is developed in the Esopus Shale. The operations of this company extend on both sides of the highway. Shale is trucked from the quarry floor to the crushers on the ridge of Fly Mountain, where the material is processed. It is then heated in the kiln, causing the shale to expand. A conveyer leads down the south side of Fly Mountain, where the expanded shale is loaded on barges in Rondout Creek to be carried down the Hudson River to markets in the New York City area. Trucks are used to carry the expanded shale to customers in the Mid-Hudson area.
Though the Esopus Shales are not highly resistant to erosion, in this area they commonly are minor ridge-makers. Where exposed, they show as massive blocks whose bedding is difficult to follow, but whose cleavage is readily apparent. The cleavage may therefore be easily mistaken for the bedding in an outcrop.
Both the cleavage and the extensive fracture pattern in the shales is reflected in details of the topography of the region. The strongly-cleaved shales are more easily eroded and the intersection of the cleavage with the accompanying joints results in the appearance of gently sloping planes dipping in various directions where the shales are exposed (Fig. 1 - The vertical lines indicate cleavage).
Where freshly exposed, the shales appear black, blue-black, or olive-brown. Often they show vertical white bands, a result of re-deposition on their cleavage surfaces of some of the minerals dissolved from the shale.
Weathering of the shales will often bring out color changes that emphasize the bedding planes. Occasional lenses or thin layers of other material, e.g., sand, help in the delineation of the bedding. Where the shales have been exposed to weathering, some of those having a greater lime content will show a grayer surface.
At this locality the beds are generally more gently dipping than the cleavage. The response of the shales to folding was not paramount; they show some flexures, but the continued impress of the deforming forces caused the shales to shear rather than to fold. Shear planes present in some cases cut across the cleavage. Where a conjugate set of shear fractures exist they are parallel to the cleavage (Fig. 3). The cleavage is generally parallel to the strike of the beds. However, it should be evident that strike joints will generally merge with the strong cleavage.
Occasional fossil shell fragments can be found in the shales. Nodules of pyrite are frequent.

STOP II: Callanhan's Quarry and Railroad Cut
STOP IIa: Callanhan's Quarry is in the village of Connelly south of Rondout Creek. From the quarry floor, facing northeast, approximately 170 feet of limestones have been exposed by the quarrying operation. There are three areas or"pits" where the quarrying operations take place all at varying distances from the northwest-southeast section line drawn across the quarry floor. In the accompanying section, the pits are labeled by number (Fig. 5).
The limestone, commercially known as "traprock", is crushed to different sizes after being blasted from the walls of the quarry. It is used primarily in various kinds of construction such as road metal for highways, and concrete aggregate for building construction. The Rondout Creek is used to transport bulk shipments of the material.
The limestones show three major high-angle reverse faults cutting through all the beds exposed in the quarrying operation. There are numerous smaller faults. Looking to the southeast, one can see near-vertical faces of limestone. Bedding-surface slickensides are commonly seen in the quarry, for example, between the Alsen and Becraft units and within the New Scotland limestones.
The exposed southeast side of Pit I shows an extensive slickensided surface over much of its length. Also on this same surface and extending for many feet parallel to the slickensides are thick, rod-like mullion structures. The limestones in this pit are gently folded.
In Pit 2 there is an extensive fault zone which includes a major fault. Toward the southeast the quarry wall is near-vertical and shows extensive slickensides. There the beds are bent in a circular arc at the southeastern end of th is section, and are folded synclinally.
The sharp folds are continued into Pit 3. Here the Becraft-New Scotland exposures are near vertical and show extensive slickensiding within the New Scotland beds.
STOP IIb: This stop is in the cut of the West Shore R.R. about one quarter mile east of Callanhan's Quarry. Near the road coming from the floor of the quarry to where it intercepts the railroad track there are exposures of the Hudson River sandstones. The contact of the Ordovician sandstones and the Silurian is not visible here. The Kalkberg and New Scotland beds can be seen just west of the railroad right-of-way. The Becraft limestone outcrop, to which an abandoned wagon trail leads, was mined in earlier years at this site. Many of the abandoned quarries in the Kingston area formerly exploited the Becraft or the Rondout limestones.
Of the quarrying operations the main evidence is a 100-foot shaft situated between the New Scotland and the Alsen through which the Becraft was removed. At the lowest part of the north wall in this shaft one can see part of the synclinal fold in the Becraft, which was also visible from the floor of Callanhan's Quarry. The railroad cut farther northward exposes the Port Ewen limestone (and its time-correlative deposits - the Connelly). The Port Ewen alternates with the Glenerie in exposures along the railroad tracks.

STOP III: Road cuts along Route 199 three miles north of Kingston.
This stop will be made along that section of Rt. 199 extending between Rt. 32 to Rt. 9W. Along Rt. 199 the road cut exposes relatively gentle folding in the Devonian beds (Fig. 6). There are two low concealed areas in the section which are covered by swamp deposits and alluvium.

Angular Unconformity
Approximately one quarter mile south of the entrance to Rt. 199 on Rt. 32 there is a good exposure of the angular unconformity between the Ordovician beds and overlying Silurian limestone.

STOP IV: Glenerie Falls
This stop is at Glenerie Falls and Rt. 9W approximately 6.3 miles north of Kingston. A plan view of the shear structures and the cleavage in the Glenerie Formation in this area is included (Fig. 4). The pattern which is shown in the plan view is seen as a side view where the Glenerie is visible along the highway. Some of the Glenerie exposures along the highway reflect the shear pattern so that the exposed blocks show as rectangles at times pointing toward the highway and at other times away.
The Esopus Creek which upstream meanders through its valley for several miles turns sharply to the east at Glenerie Falls and then flows north again at the foot of the Falls. Beyond, it continues between the confining Esopus Shales and the Glenerie, and has an approximately straight course almost to its mouth; it makes a bend at Saugerties and flows into the Hudson.
The rocks at the Falls clearly express the shear structure in the area. The weak, overlying Esopus Shales are being rapidly eroded. The presence of the Falls indicates a relatively youthful expression of the topography for the falls have not yet been planed down to grade.

F: STRUCTURE AND PETROLOGY OF THE PRECAMBRIAN ALLOCHTHON AND PALEOZOIC SEDIMENTS OF THE MONROE AREA, NEW YORK
The area covered by this trip lies in the northern part of the Monroe 7 1/2′ quadrangle, New York, and consists of a folded and faulted complex of autochthonous Precambrian gneisses, Lower Cambrian through Middle Devonian sediments and allochthonous Precambrian gneisses. Geologic maps covering the trip area have been published by Ries (1897), Fisher, et.al. (1961), and Jaffe and Jaffe (1962). Unpublished maps prepared by Colony and by Kothe (Ph.D. thesis, Cornell Univ.) undoubtedly contain valuable information but are not available for study. Recent workers in adjacent areas include Dodd (1965), Helenek (in progress) and Frimpter (in progress), all in the Precambrian autochthon, and Boucot (1959) and Southard (1960) in the stratigraphy and paleontology of the Paleozoic sediments. The work of Colony (1933), largely unpublished, is impressive.
HOWARD W. JAFFE, University of Massachusetts
ELIZABETH B. JAFFE, Amhurst, Massachusetts

F: STRUCTURE AND PETROLOGY OF THE PRECAMBRIAN ALLOCHTHON AND PALEOZOIC SEDIMENTS OF THE MONROE AREA, NEW YORK

STOP 1: Bellvale Graywacke
The outcrop is on Oreco Terrace, just above the intersection of NY 208 and Oxford Road. Here, the Bellvale graywacke of the Hamilton Group (Middle Devonian) is exposed in a section approximately 220 feet thick. It consists of 20-40 foot beds of dark blue-gray, green-gray, or gray, fine-to medium-grained (.08-.25mm-avge. grain size) lithic arenite or graywacke, rhythmically interbedded with thin beds of dark green-gray to blue-gray shale. A representative modal composition of the graywacke follows:
| |
Detritals | |
| quartz | 20%
| oligoclase | 2
shale
phyllite
44?
siltstone
chert
9.0
| greenstone | 15
Matrix | |
clay, sericite,
chlorite, Mn oxide
15?
Metamorphic | |
| Chlorite | 2
| Muscovite | 1
| | 100%
Texturally, the rock consists of angular, elongated slivers of detrital quartz and predominantly phyllitic rock fragments (.08-.25mm) set in a fine matrix of sericitic muscovite, clay, and chlorite. It is often difficult to distinguish smeared-out phyllitic fragments from balled-up micaceous matrix, both of which frequently blend or flow together. Depending upon the uncertainty of the matrix content, or the classification used, the Bellvale is either a low-rank graywacke (Krynine, 1948), a subgraywacke or a lithic graywacke (Pettijohn, 1957) or a graywacke (Folk, 1954). Larger bent grains of chlorite and muscovite in the matrix, are here interpreted to have grown from fine matrix material, marking the beginning of the chlorite zone - greenschist facies of regional metamorphism imprinted during the Appalachian orogeny.
In general, the Bellvale graywackes tend to show rhythmic interbedding with shale, with graded bedding low in the section and strong current cross-bedding higher in the section. Occasional brachiopods are found low in the section; plant fossils are found higher up. Both features suggest a gradation from marine to nonmarine depositional environment. The provenance was a low-rank metamorphic or sedimentary terrane.
The shattered outcrop at Oreco Terrace is at the southwest corner of Rotated Block 8 (Fig. 2) and lies near the intersection of four directions of faulting. Attitudes of prominent structures at the outcrop are tabulated:
| Strike | Dip | Plunge
Bedding | N 67 W | 30 NE |
Cleavage | N 50 E | 37 SE |
Fault Slickensides | N 13 E | Steep W | 45 N
Fault Slickensides
N 38 E
Steep W
60 N
N 30 W
52 SW
39 W

STOP 2: Shawangunk Conglomerate
Spring Glen Golf Range: Shawangunk Conglomerate
The Shawangunk conglomerate and quartzite (Greenpond conglomerate unit) of Lower to Middle Silurian age occurs in a series of small outcrops extending northeastward along the western edge of the Shunemunk Mountain syncline. At this stop the Shawangunk forms a small, relatively inconspicuous topographic knob as contrasted with its occurrence near Stop 5, where the same unit forms the spine of the steep, southeast-facing escarpment of Lazy Hill. At the present stop the Shawangunk consists of about 75% buff pebble conglomerate intercalated with 25% fine-grained green-gray quartzite.
The conglomerate consists of white pebbles of milky vein quartz (averaging 15-40mm in length) in a matrix of finer pebbles and grains of rounded quartz, all cemented by secondary silica and buff-orange-red ferric oxides. Occasional pebbles of white orthoclase are present as are black pebbles consisting of a mixture of green tourmaline and quartz. The color of the weathered surface of the outcrop varies from pink (hematite) to yellow-brown (goethite) or black (manganese oxide dendrites) with some greens contributed by lichens.
The pebbles, obviously well-rounded when deposited on the Late Ordovician erosion surface, have taken on a secondary angularity and elongation due to stretching, crowding, rotation, and slippage in bedding planes produced during Paleozoic orogenies. Most of the pebbles show maximum elongation parallel to the fold axis (b-direction) and modest elongation parallel to the bedding (a-fabric axis). Many of the pebbles have been corrugated and a large number are cracked and sliced parallel to the b-c fabric plane. Bedding surfaces are slickensided, fluted, and warped parallel to the a-axis (down-dip). The fine-grained, gray-green interbedded quartzite is composed of quartz and minor orthoclase cemented by authigenic quartz, muscovite and chlorite, and Fe-oxides.
The elongation and shattering of the pebbles here and at Lazy Hill to the southwest greatly exceeds that observed in pebble beds in Lower and Middle Devonian rocks (Connelly conglomerate of Oriskany age, and Bellvale graywacke, respectively) in this area, suggesting that the Shawangunk was involved in an additional deformation episode of possible pre-Oriskany age. A pre-Acadian, Silurian deformation period in New York was reported by Megathlin (1939) and discussed by Kay (1942). The sporadic outcrops of Shawangunk quartzite to the north along the western limb of the Schunemunk Mountain syncline are all heavily silicified and sheared, again much more so than quartzites of Oriskany and Bellvale age.
The conglomerate and quartzite outcrop is S-shaped, with the attitudes of the bedding and a cross-fault as follows:
| | Strike | Dip
Bedding, Cgl. | North end of hill | N 8 E | 77 E
Bedding, Cgl. | North center of hill | N 59 W | 70 NE
Bedding, Cgl. | Center of hill | N 27 W | 50 NE
Cross-fault
N 77 W
90
Bedding, Qtz.
South end of hill
N 2 W
60 E
The cross-fault displaces the stratigraphically higher Shawangunk quartzite member to the west, putting it on strike with the lower conglomerate member of the Shawangunk Formation. On first viewing the outcrop, the alternating coarse pebble beds and fine feldspathic quartzites lead one to suspect that the beds are overturned. On close inspection this does not appear to be the case.

STOP 3: Museum Village Klippe
Museum Village Klippe: Allochthonous Pre-Cambrian Leucogneiss Resting On Cambro-Ordovician Wappinger Dolomite
From the Old Mansion Road cut in the Precambrian Museum Village klippe, look south across the N 75° W-trending Quickway crossfault. The ridge due south is the Bellvale synclinal extension of Schunemunk Mountain. The next ridge to the west is Lazy Hill, held up by Shawangunk conglomerate, and offset from the Golf Range Shawangunk conglomerate of Stop 2. To the west of Lazy Hill, the next prominent ridge is the Goose Pond Precambrian klippe, formerly continuous with the Museum Village klippe and now offset about 2 miles along the Quickway cross-fault.
Museum Village klippe is a thin, synclinal, saucer-shaped slice of gray-white albite-quartz-microperthite leucogneiss that has survived five or six orogenies. The rocks of the allochthon were deposited as a clastic wedge (molasse) in a reducing environment, perhaps as long ago as 1500 million years; they were folded and metamorphosed to the sillimanite-almandine-orthoclase metamorphic grade about 1100 million years ago; thrust from the east in Taconic or Late Ordovician time; refolded and faulted in Taconic time; possibly again in Acadian time; refolded and faulted in Appalachian time; and finally shattered by Triassic block faulting and associated block rotation. In outcrop, the leucogneiss is heavily shattered and slickensided with lineations often running in three directions at a given place. Quartz grains and pebbles are stretched into thin corrugated tongues and sheets showing elongations of 15:1 and 20:1 parallel to the b- and a- fabric axes. Over most of the outcrop, biotite and garnet are extensively retrograded to chlorite, and abundant calcite veinlets cross the rocks at all angles.
Towards the central and western part of the cut there occur occasional thin layers rich in fresh biotite and uncommonly coarse laths (not needles) of fresh blue-gray sillimanite that have survived the complex orogenic history. As none of the Cambro-Ordovician or younger rocks in the area show any metamorphic grade higher than chlorite zone metamorphism, the sillimanite is assumed Precambrian in age, and its preservation in large fresh grains in an otherwise extensively retrograded outcrop is remarkable.
The original sedimentary record of Precambrian deposition is preserved in graphite-rich quartzitic layers and in microscopic placer layers rich in apatite, zircon, sphene and ilmenite. In places, volcanic rocks associated with the sediments may be represented by amphibolites such as those in the Bull Mine Mountain klippe to the north.
Modal analyses of samples collected along an east-west traverse across the Museum Village klippe follows:
| East Side | Center | West Side
Andesine (An 32)
-
36.0
32.4
Quartz
Biotite
Almandine-pyrope | 0.1 | 2.0 | - | -
Tourmaline | - | + | + | -
Zircon
+
Ilmenite
The presence of albite in the most retrograded gneisses of this and the other allochthonous Precambrian blocks studied fairly consistently suggests that it may be a retrograded mineral after an originally more calcic plagioclase. The K-feldspar in all of these rocks is microperthite (usually microcline microperthite) and is indicative of a temperature of Precambrian metamorphism of the order of 660° C. The presence of two plagioclases, one as free grains and the other exsolved in microcline microperthite, is characteristic of many of the granitic gneisses of both the autochthon and the allochthons. In some of the allochthonous leucogneisses, the microperthite and the albite tend to occur in separate bands which may reflect original compositional differences.
Park on Oxford Road and cautiously descend hill to the Quickway (N.Y. 17-West = U.S. 6). Beware of high speed traffic and stay close to the outcrop which parallels the highway. Walk to the extreme west edge of the roadcut where the Precambrian leucogneiss rests in overthrust contact on the light gray Cambro-Ordovician Wappinger dolomite. Note the occasional flat-lying, slippery fracture planes at the contact.
The metamorphic layering in the allochthon dips to the east whereas the dolomite bedding dips predominantly west. The average foliation of the leucogneiss is N 33 E,20 SE. The average attitude of the dolomite beds is N 22 W, 35 W. Prominent faults in the klippe parallel the metamorphic layering and trend N 22, E 20 SE. The fault contact of the dolomite and the klippe is irregular and has the same general attitude. Both the dolomite and the klippe are cut by vertical faults trending N 27 W.
Drive west along Old Mansion Road observing the flat topography superposed on the Hudson River pelites. These are more gently folded with increasing distance from the Precambrian allochthon.

Rolling folds in pelites
Cross the Quickway (N. Y. 17) overpass and bear hard left (east) on N.Y. 17-M. Drive about 1.1 miles east noting rolling folds in the Hudson River pelites. Road parallels Quickway fault.

STOP 4:Precambrian Allochthon
Goose Pond Mountain: Precambrian Allochthon Over Overturned Hudson River Pelite
Observe black, fissile Hudson River shales (Middle? Ordovician) in the road cut at the northwest edge of the Precambrian allochthon. Careful observation will show that the attitude of the bedding and cleavage is N 78 E; the bedding dips 70 S and the cleavage 40 S. This indicates that the outcrop is on the limb of an overturned fold with the synclinal axis to the north. The shales both here and at Bull Mine Mountain klippe to the north are all wildly folded and overturned close to the overriding Precambrian allochthons.
Many of the Hudson River black shales are calcareous, and consist of fine laminae (.05-.lmm) of dolomitic silt or mud (marl) intercalated rhythmically (occasionally cross-bedded) with carbonaceous shale. An estimated thin-section mode of a representative Hudson River "shale" follows:
Mineral | Calcareous laminae | Carbonaceous laminae
Detritals and matrix: | |
dolomite, calcite
30%
5%
plagioclase, microcline
10
+
mica, clay, chlorite | 15 | 50
carbonaceous matter, graphite
-
Metamorphic: | - | +
chlorite, muscovite, biotite | - | 5
In the woods about 100-150 feet southwest of the shale outcrop on N.Y. 17-M, moss-covered rubble of shale, dolomite, and "limonitized" fault breccia indicate where the covered contact has been crossed. The edge of the Precambrian allochthon of Goose Pond Mountain is found in place about 130 feet south from the road, and the first rock found in place is a graphitic calcareous quartzite of which sample No. 527 is representative.
Drive 0.4 mi. on N. Y. 17-M, stopping at a white albite-quartz-microcline microperthite leucogneiss (sample No. 20), in places graphitic, biotitic or rarely, garnetiferous. Note the extreme elongation and smearing out of quartz pebbles and grains similar to that seen at the Museum Vi lIage outcrop of Stop 3. Further to the east, the rocks become increasingly calcareous (sample No. 788). At the extreme eastern edge, prehnitized calc-silicate leucogneiss is interlayered with some amphibolite, the latter of probable basic volcanic origin. Modes of representative rock types of the Goose Pond allochthon follow:
Modes Of Gneisses Of The Goose Pond Mountain Allochthon
East Side
Center
West Side
Sample Number
Mineral | | | |
brown hornblende | 0.2 | 33.0 | - | -
Here, as in the Museum Village klippe of Stop 2, the greatest amount of retrograding occurs at the eastern and western margins of the allochthon with some fresh rock occurring near the center. If the klippen are indeed synclinal saucers the presently exposed centers of the masses would lie at a further distance from the sole of the thrust and would be expected to show less alteration. It should be emphasized that the Precambrian autochthonous gneisses in the southern part of the Monroe quadrangle (Jaffe and Jaffe, 1962) are not comparably retrograded except near the Triassic border faults.

STOP 5: Shawangunk Quartzite
Walk 0.2 mile west crossing buried northeast-trending fault contact between the Shawangunk ridge of Lazy Hill rising steeply ahead and the Bellvale ridge of Durland Hill to the rear. Walk to the north nose of Lazy Hill (permission of the owners, the Durlands, is necessary) where a large outcrop of Shawangunk quartzite is exposed. The rock is a thin-bedded, pink, buff and white orthoquartzite consisting of:
Mode of Shawangunk Orthoquartzite, Durland Property
Quartz | 93%
Chert
Sericite, Chlorite
Zircon | +
Hematite | +
Goethite | +
Pyrite | +
Green Tourmaline | +
| 100.0%
The quartz grains are well-rounded, moderately elongated, well-sorted (average diameter, 0.75mm), and the rock is very tightly cemented. Each grain of quartz is cemented to another by authigenic quartz overgrown in optical continuity with the detrital cores. Undulatory extinction due to deformation passes through both the core and overgrowth of each grain. The Lazy Hill ridgetop to the south (not visited) is formed of a coarse white pebble conglomerate interbedded with white orthoquartzite (occasionally ripple-marked) and grades eastward to a red arkosic conglomerate below the ridge-top. Quartz pebbles and orthoclase pebbles are strongly elongated (3:1 and 4:1) and heavily shattered and veined in both the red arkosic and the white conglomerate.

STOP 6: Connelly (Oriskany) -Esopus Contact
The outcrop at Monroe Bowl-0-Fun consists of about 300 feet of the Esopus Formation underlain at the rear of the cut by red and white pebble conglomerate, the Connelly Conglomerate of Oriskany age. Here, the Connelly consists of weathered, yellow, "limonitic" conglomerate (3' or more), succeeded by white to buff, pebble-bearing orthoquartzite (5'), which is in turn overlain by bright red hematitic quartzite (10'). The pebbles in the Connelly conglomerate are of white, round to slightly elongated quartz, averaging 1-2 mm in maximum dimension. The Connelly is disconformably overlain by a lowermost member of the Esopus Formation, recognized by Southard (1960). The attitude of the bedding of both the Connelly and the Esopus at their contact is N 68 E, 45 N. A heavily slickensided fault surface, trending N 53 E, 60SE cuts across the Connelly beds and presumably also cuts the overlying Esopus Formation.
The lowermost member of the Esopus, at its base, consists of fissile, blue-gray siltstones which weather to brown and orange on cleavage surfaces. Many of the rocks are marked withTaonurus cauda-galli on bedding planes. At this outcrop the authors have collected a remarkable fauna including a specimen of the giant trilobite,Coronura myrmecophorus, not previously reported from the Esopus Formation. According to D.W. Fisher, New York State Paleontologist who identified the specimen, it has previously been reported from the Schoharie and Onondaga Formations. The specimen was donated to the N. Y. State Museum collection.
The lowermost member is also relatively rich in conulariids, none of which have yet been identified. Other fauna include the brachiopods:Leptocaelia flabellites, Schuchertella sp, Acrospirifer macrothyris, as well as some chonetid and orbiculoid genera. Platyostomid and loxonemid gastropods, rugose corals and a dalmanited trilobite were also collected by the authors.
The lowermost member grades into the black, poorly fossiliferous Lower Mudstone member which in turn grades into a purple sandstone at the north end of the 350 foot exposure. The sandstone is presumably the lower part of the Highland Mills member of the Esopus Formation. The fauna of the lowermost member at the Bowl-O-Fun appears to differ significantly from that of the Highland Mills member of the Esopus Formation found at Bakertown and Highland Mills (described by Boucot, 1959). The fauna should receive some serious study by specialists before the outcrop is demolished by new construction.

STOP 7: Poughquag Quartzite (Lower Cambrian)
Orange Turnpike: Poughquag Quartzite (Lower Cambrian)
Walk 0.16 miles due west over hilltop to the edge of a cliff formed by a 10 foot section of the Poughquag Formation (Lower Cambrian). The section consists of alternating 2 inch to 2 foot thick beds of ferruginous orthoquartzite, conglomerate, and arkose, striking N 75 W and dipping 80 N, overlying the vertically dipping Precambrian autochthon with marked angular unconformity. This represents original sedimentary onlap with only gentle warping or folding in subsequent geologic time. Apparently the Precambrian Monroe Massif (Block 2) was sufficiently rigid throughout the Paleozoic to prevent the deformation of the overlapping embayment of Poughquag quartzite and Wappinger dolomite. This is indicated by both the gentle warping observed and also by the relative sphericity of the quartz pebbles in various Poughquag beds.
Several of the beds are feldspathic, a feature uncommon in the Poughquag of the Poughkeepsie quadrangle (Gordon, 1911). One such bed at the Monroe outcrop is a conglomeratic arkose which is a true high rank arkose in the sense of Krynine (1948). A remarkable textural feature of this rock is the abundance of authigenic feldspar (microcline?) which is the principal cementing medium in sample No. 466. The specimen consisfs of 1-2mm quartz and microcline pebbles (all very round) lying in a matrix of 0.2mm grains of microcline and much less quartz. The microcline grains, each with a dirty outline (Fe and Mn oxides), tend to float in the matrix of authigenic microcline (?) cement which is clear in appearance. Some sawtooth or hacksaw terminations on the detrital microcline cores (Edelman and Doeglas, 1931) indicate that interstratal solution has taken place after deposition, presumably in situ. The authigenic feldspar overgrowths show only weak twinning when grown around detrital cores showing strongly developed microcline twinning.
A mode of such rock is as follows:
Mode Of Lower Cambrian Poughquag Conglomerate Arkose
Specimen No. 466
Microcline
47.4%
Microcline microperthite
+
Quartz | 48.6
Albite-oligoclase | +
Muscovite | +
Rutile, Anatse, Tourmaline (green and brown) | 0.5
Zircon | 0.5
Hematite, Mn oxides | 3.0
| 100.0%
The mineralogical composition of the Poughquag at Monroe leaves little doubt that it was derived from erosion of the granitic gneisses it overlies.
On the return walk to the road, stops may be made at exposures of post-Wappinger lamprophyre dikes which the authors believe to be of Late Ordovician age (Jaffe and Jaffee 1962). The authors have studied the dikes in considerable detail and would suggest a possible age of intrusion similar to that of the ultramafic intrusion of the Cortland Complex at Stony Point, New York (Ratcliffe, 1967). The Cortland Complex has been dated by Long and Kulp (1962) at 435 million years by K/ A isotopic ratios obtained on biotite from the complex, a date close to the accepted Ordovician-Silurian boundary.

G: THE PLEISTOCENE GEOLOGY OF THE WALLKILL VALLEY (2)
G.GORDON CONNALLY
S.U.N.Y. College at New Paltz

G: THE PLEISTOCENE GEOLOGY OF THE WALLKILL VALLEY (2)

STOP 1: Ablation Till
Examine the ablation till exposed in the cut behind the Carrol's stand. Compare this till to the lodgment till exposed at Stop A-2 on trip A. There will be a discussion of weathering profile and soil development.

Cross the Catskill Aqueduct
The aqueduct follows the road on the right for 1/2 mile until it is re-crossed. After re-crossing the aqueduct note the lithology of the stone walls, particularly the absence of Shawangunk boulders.

Ascend the till ridge that trends north-south.
This is a ridge of drumlinized crests that can be traced for about 10 miles east of the Wallkill Moraines.

Flat-topped outwash deposit
This road traverses a flat-topped outwash deposit that has a 400 foot crest on the distal side of the Wallkill moraines. This suggests that the ice occupied the Wallkill position during the development of the 400 foot lake level.

Outermost Wallkill Moraine
Ascend the gentle distal slope of the outermost Wallkill Moraine and then descend the proximal slope into the stagnant ice complex.

Cross the first inner Wallkill Moraine.

STOP 2: Wallkill Moraines
STOP G-2. Here can be seen some of the Wallkill Moraines. Their possible relationships and the relation of the Wallkill River to the glacial deposits will be discussed.

The Wallkill Moraines are well displayed on the right

Second inner Wallkill Moraine
Cross the distal slope of the second inner Wallkill Moraine. This moraine is on a bedrock escarpment and is not nearly as massive as the topography makes it appear. The State Prison Moraine (?) is on the left in the distance.

Cross the Catskill Aqueduct.

A striated bedrock knob is exposed on the right.

State Prison Moraine
The State Prison Moraine (?) is immediately adjacent to the road on the left and will be crossed in the vicinity of Ireland Corners.

Splendid panorama
On a clear day a splendid panorama can be viewed on the left. In the foreground is the Lower Wallkill Valley with the Shawangunk Mountain cuesta in the distance. The Catskill Mountains can also be observed on the skyline behind, and north of, the Shawangunks.

STOP 3: Delta remnant
Leave the cars and walk through the field on the left to the sand pit. Examine the relationship between pro-glacial lakes, deglaciation, and the present course of the Wallkill River. This deposit is the remnant of a delta formed in the final 230 foot lake in the Wallkill Valley.

Floodplain of the Wallkill River
The floodplain of the Wallkill River can be seen on the left. The floodplain evidently extends only to the low escarpment a few hundred feet west of the River with undisected lake plain from the scarp to the west valley wall.

Old stone houses
This street contains the old stone houses for which New Paltz is famous. These stone houses were built by the Huguenots in the late 1600's and early 1700's.

Oxbow Lake
As the road bends right and then left it is following an abandoned meander of the Walkill that now exists as an Oxbow Lake. This oxbow may be seen behind the houses to the left.

Lake shoreline
From this point to Stop G-4 Route 32 follows the shoreline of the 230 foot lake. This may explain the frequently exposed bedrock along the east side of the road.

Bedrock channel on right, lake sediment on left
Route 213 joins from the right just south of the bridge over the Wallkill River. Note that the Wallkill is cutting a bedrock channel to the right while flowing over lake sediment on the left.

STOP 4: Wallkill geomorphology
Here will be discussed the geomorphology of the Wallkill River drainage basin and its relation to the Rosendale sand plain.

Descend from sand plain
Descend from 240' on the sand plain to 65' in the Rondout Creek Valley. Bridge across Rondout Creek.

Channel bars
Note the channel bars in the creek; these did not exist before the recent drought.

Cross a remnant of the 200 foot Lake Albany (?) plain.

Fly Mountain fault scarp.
Bear left on Mountain Road and parallel the Fly Mountain fault scarp.

STOP 5: Wilbur gravel pit
This is the Wilbur gravel pit of the City of Kingston. It is the type locality for the Wilbur limestone member of the Rondout Formation (Silurian). Leave the cars on the road and walk up into the pit to examine the relationship between the ice-contact gravels and the slumped, overlying Lake Albany (?) sands, silts, and clays. Examine the pebble lithologies and compare them with those at Stops A-1, A-6, and A-8 on Trip A.

Lake Albany (?) clays crop out on both sides of the Thruway.

Cross Rondout Creek cutting a bedrock channel at this point.

Cross Wallkill River cutting bedrock channel at this point.

NEW YORK STATE GEOLOGICAL ASSOCIATION GUIDEBOOK
TO
FIELD EXCURSION
S 40TH ANNUAL MEETING
AT
QUEENS COLLEGE
CITY UNIVERSITY OF NEW YORK
FLUSHING, NEW YORK

A: BEDROCK GEOLOGY IN THE VICINITY OF WHITE PLAINS, NEW YORK
By Leo M. Hall, University of Massachusetts
(Approved for publication by the Assistant Commissioner for the New York State Museum and Science Service.)
INTRODUCTION
Stratigraphic relations, including two unconformities, are well displayed by the bedrock in the White Plains quadrangle in Westchester County, New York. Fifteen rock units within the traditional "New York City Group" have been mapped in detail there. At the lower unconformity, Cambrian Lowerre Quartzite or Inwood Marble rest on Precambrian Fordham Gneiss and Yonkers Gneiss. Along the upper unconformity, the lower member of the Manhattan Schist rests on various units of the Inwood Marble as well as the Fordham and Yonkers. In addition, a major thrust fault may occur near the base, and locally at the base, of what has traditionally been mapped as Manhattan Schist.
There is widespread evidence for at least four, and probably five, phases of deformation in the region. The Yonkers Gneiss and Fordham Gneiss were folded at least once before the deposition of the Lowerre Quartzite and younger rocks. The pre-Manhattan rocks were deformed, at least mildly, prior to the deposition of the lower part of the Manhattan Schist. A major thrust fault, correlated with Taconic thrusting, may separate member A of the Manhattan Schist from members Band C of the Manhattan Schist. Finally, all of the rocks and previously formed structural features were involved first in major nappe-like isoclinal folds and second in folds with steeply dipping axial surfaces.
The main purpose of this field trip is to illustrate the stratigraphy of the region. In doing so, some of the main structural features will also be shown.

A: BEDROCK GEOLOGY IN THE VICINITY OF WHITE PLAINS, NEW YORK

Inwood Marble
The road log begins at the northbound New York Thruway exit in Ardsley and the route is indicated on Figure 2. The contact between member B and member C of the Inwood Marble is exposed along the west (left) side of the exit ramp. Member C is exposed along the east (right) side of the ramp as well. The Inwood here is in the west limb of a north-plunging syncline with Manhattan Schist in the trough of the syncline underlying the hills on the east and Fordham Gneiss under the hills on the west. Leave the exit ramp and turn right (north) onto route 9A (Saw Mill River Rd.) and then proceed northward along the west limb of the syncline.

Manhattan Schist
Turn right (east) onto Ashford Ave. and proceed southeasterly over the hill, across the synclinal trough. The exposures along the roadsides are Manhattan Schist.

Sprain Brook valley
Ashford Ave. enters Sprain Brook valley which is underlain by Inwood Marble. The ridge ahead to the east is Fordham Gneiss in the center of a north-plunging anticline. There are some small exposures of Lowerre Quartzite along the west limb of the anticline in this vicinity. The gneiss plunges out at the anticlinal nose less than a mile north of here.

West Limb of Anticline
Turn right (south) on Sprain Rd. and proceed southwesterly along the west limb of the anticline. The unpublished field notes of E.C. Eckel (New York State Museum and Science Service, Geological Survey files) report Lowerre Quartzite and Fordham Gneiss behind the houses on the east (left) side of the road but, apparently due to construction, only quartzite float exists there now.

STOP 1. New road cuts on Sprain Brook Parkway Construction site.
The road cuts are along the left (north) side of Jackson Ave. on the approach to the new Jackson Ave. bridge that is now under construction and along the west side of the southbound lane of the Sprain Brook Parkway which is also presently under construction. We will walk north along the southbound lane of the Parkway and be picked up by the bus at Ardsley Rd. Those not wishing to walk may reboard the bus here and ride to Ardsley Rd. Be careful of traffic on Jackson Ave. when disembarking.
Start at the west end of the road cut on the approach to the new Jackson Ave. bridge; in traversing eastward several varieties of rock types in the Fordham Gneiss will be seen in the center of the north plunging anticline. Minor structural features are abundant and many of the linear elements plunge northward apparently parallel to the anticlinal axis. Although this area has not been mapped in detail, it appears that these rocks might be grouped into three mapping units from west to east as follows:
1. Brown to rusty weathered sillimanite-garnet-biotite gneiss and smaller amounts of gray biotite-quartz-feldspar gneisses.
2. Light gray, locally pinkish, biotite-quartz-feldspar gneiss with sparse garnet. This rock looks somewhat like the Yonkers Gneiss in places.
3. Dark gray biotite and/or hornblende gneiss and amphibolite.
It would be necessary to map this area in detail to determine whether or not the above subdivision is meaningful.
After traversing to the west end of the new Jackson Ave. bridge, walk northward along the deep road cuts in subdivision 3, proposed above, and down into the Sprain Brook Valley. Walk north along the west side of the valley to Ardsley Rd. and observe several road cuts in subdivision 3. Drilling data obtained at several places along the Grassy Sprain Valley in conjunction with the highway construction now in progress reveal the predicted presence of Inwood Marble beneath the valley fill.
The contact between dark gray biotite gneiss and light gray to pinkish-gray gneiss is exposed in the road cuts at the west end of the new Ardsley Rd. bridge which is now under construction. This contact projects into the Sprain Brook Valley where it is truncated by the Inwood Marble along an unconformity. The west contact of the light gray or pinkish-gray gneisses has been mapped in detail here and it is truncated by the Inwood Marble approximately three quarters of a mile north of here. Reconnaissance indicates that these gray gneisses are very likely the same as subdivision 2 proposed above.

East Limb of Anticline
Turn left (north) onto Grassy Sprain Rd. and proceed along the east limb of the anticline. The road is near the contact between the Inwood Marble and Manhattan Schist. The hills to the east are underlain by the Manhattan in the trough of a syncline.

Manhattan Schist Member B
Turn left (northwest) onto Ardsley Rd. (A good exposure of member B of the Manhattan Schist is in the road cut along Ardsley Rd. approximately 0.1 mile southeast of this intersection.) Proceed northwest along Ardsley Rd. entering the floor of Grassy Sprain Valley.

Crossing anticline
The bus will stop here in order to allow the group to board and then will continue northwesterly on Ardsley Rd. crossing the anticline.

Recrossing the syncline
Proceed straight through the dangerous intersection where the street name changes from Ardsley Rd. to Ashford Ave. Continue northwesterly on Ashford Ave. re-crossing the syncline.

Have traversed Manhattan, Inwood down into Fordham Gneiss
Proceed through the major intersection and onto the bridge that overpasses the Saw Mill River, New York Thruway, New York Central Railroad tracks, and the Saw Mill River Parkway. In so doing we have traversed from the lower part of the Manhattan Schist through members A, B, and possibly part of C of the Inwood Marble down into the Fordham Gneiss.

Fordham Gneiss Member A
Many exposures of member A of the Fordham Gneiss are present in the hills on the west (left) side of Northfield Ave.

Cyrus Field Rd., named after "the father of the first transatlantic cable".

STOP 2. Harriman Road Reservoir.
Park in the driveway on the right (north) side of the road that leads into the watershed area of the reservoir. We have been allowed to visit this area through the courtesy of the Village of Irvington, Department of Public Works. This is a water supply reservoir, please conduct yourself in accordance.
This is the area of a steeply plunging structural syncline that is defined by the contacts between various members of the Fordham Gneiss (Figure 3). Minor structural features and the orientation of foliation indicates that the syncline plunges 50° to 60° toward the south. It has been possible to map a separate amphibolite within member B of the Fordham Gneiss here (Figure 3) but the amphibolite cannot be separately mapped elsewhere. We will study the syncline by traversing along and across the amphibolite-garnet gneiss contacts (see walking route, Figure 3). Disembark from the bus and proceed southeast along the northeast side of Harriman Rd. to station a.
Station a - Dark amphibolite and biotite-hornblende gneiss along with some garnetiferous gneiss are exposed here on the east limb of the syncline. The contact between the amphibolite and garnet gneiss appears gradational here and it is very difficult to map the amphibolite separately from here south. The apparent gradational nature of this contact may be due to minor folds which are abundant here. Note the pyroxene (green-weathering) rimmed by hornblende (black) indicating retrograde metamorphism. Thin sections of similar rocks in member B of the Fordham reveal amphibole lamellae within the pyroxene and these lamellae are apparently retrograded exsolved pyroxene. The textural and mineralogical relations in this rock are open to various interpretations.
Station b - The exposure of typical gray garnet-rich gneiss in the trees on the north side of the road occupies the keel of the syncline here. Elsewhere in this rock type sillimanite is locally abundant, particularly as inclusions in garnet, but only traces of sillimanite have been observed here.
Station c - Dark amphibolite in steep south-plunging minor folds. Note the trend of the foliation here and then look toward the northeast corner of the reservoir where the amphibolite-garnet is present at station d. The strike obviously changes and this contact outlines a minor fold here on the larger syncline.
Station d - We have progressed northward along the west limb of the syncline and across the garnet gneiss-amphibolite contact. This outcrop of gray garnet gneiSS is structurally beneath the amphibolite.
Station e - The garnet gneiss here is in the keel of the syncline. Note the foliation athwart the trend of the amphibolite-garnet gneiss contact. This foliation is apparently parallel to the axial plane of the syncline.
Station f - The amphibolite is in the keel of the syncline here and the foliation is parallel to the amphibolite-garnet gneiss contact. If time permits we will walk along the north shore of the reservoir across many exposures of rocks typical of member C of the Fordham Gneiss.
Station g - This is an exposure of member C of the Fordham Gneiss that here consists of biotite and/or hornblende-quartz-feldspar gneiss, with many quartz-feldspar layers, and amphibolite. These rocks are complexly deformed with many examples of refolded folds as well as boudinaged amphibolite.

Fordham Gneiss-Inwood Marble contact
Proceed north more or less along the Fordham Gneiss-Inwood Marble contact

Sunnyside
Turn left (west) onto the entrance road to Sunnyside (West Sunnyside Lane). Sunnyside is the former country home of Washington Irving who designed and remodeled the house himself and is responsible for its unique architecture.

Inwood Marble Member B
Member B of the Inwood Marble is exposed in the stream on the right (north) side of the road.

STOP 3. Sunnyside.
NO HAMMERING PLEASE!
The contact between the Lowerre Quartzite and member A of the Inwood Marble is exposed here. This same contact is exposed at STOP 2 on Trip H (Ratcliffe, this guidebook).
Sunnyside belongs to Sleepy Hollow Restorations, Incorporated. This is a non-profit organization that has allowed us free access to Sunnyside for purposes of this field trip. Visitors are normally charged an admission fee. Please show your gratitude by being careful.
Proceed through the reception center to the outlet of the pond, "Little Mediterranean". Lowerre is exposed in the brook beneath the bridge and extends upstream. Here, the Lowerre consists of typical tan to buff weathered quartzite, micaceous quartzite, feldspathic quartzite and granulite. More Lowerre is exposed downstream from the bridge and a large fold is clearly displayed at the waterfall. This fold is large enough to be outlined by the Lowerre-Inwood contact on the regional geologic map (Figure 1.). Bedding attitudes indicate that the fold plunges 60° to 65° toward the southeast. A white quartz vein one to two feet thick is present in the axial region of the fold.
The contact of the Lowerre with member A of the Inwood is exposed below the waterfall and the Lowerre is relatively clean quartzite near the top. The Inwood consists of coarse white dolomite marble and a few calcite-bearing beds are also present. A bright green chromium-bearing chlorite is locally present in the coarse white dolomites. Paleontologists have assured me that the siliceous "box work" present here does not represent organic remains.
There is a fine view of the Palisades across the Hudson River. The cliffs are marked by the Palisades Sill which is in contact with the Triassic Stockton Formation at the base of the cliff a little above the surface of the river (Figure 1). An unconformity, somewhere beneath the river, separates the Paleozoic and Precambrian rocks in the vicinity of Sunnyside from the overlying Triassic rocks. This unconformity dips westward and thus projects above the ground surface at Sunnyside. Evidence for the unconformity is clear in the vicinity of Stony Point on the west side of the Hudson River, see Figure 1, Trip H, (Ratcliffe, this guidebook).
There is at least one small exposure of member A of the Inwood on the grounds of Sunnyside. We will not visit the small exposures of member C of the Fordham that are present in the wooded area north of Sunnyside, but the unconformity at the base of the Lowerre must be present somewhere in the vicinity of the northern boundary of the grounds.

Fordham Gneiss Members A and B
Turn left (east) onto Ashford Ave. and proceed east across member A and member B of the Fordham Gneiss.

Fordham Gneiss-Inwood Marble-Manhattan Schist contacts
Start across the bridge that overpasses the Saw Mill River etc. and in so doing, cross the Fordham Gneiss-Inwood Marble-Manhattan Schist contacts.

West limb of syncline
Turn left (north) onto Route 9A (Saw Mill River Rd.) and proceed north along the west limb of a syncline.

Outcrops of Manhattan Schist are on the right (east).

STOP 4. REA Express Terminal.
This is a good exposure of rocks that are typical of member B of the Inwood Marble. It consists of interbedded gray and white dolomite marble; tan, cream colored, and locally pinkish-weathering dolomite marble; tan calc-schist and granulite. There are several north-plunging sinistral folds with half wavelengths of three to four feet outlined by beds in the vicinity of the corner of the cut and the side of the cut parallel to the east side of the building. These are interpreted to be later stage folds and evidence for an earlier stage of Paleozoic folding is revealed locally by folded mineral lineation. There are many other minor folds throughout the exposure. It is noteworthy that the syncline at STOP 2 is very close (Figure 3) and that its orientation is apparently unrelated to the folds present here. This suggests that the syncline at STOP 2 is a structural feature that was developed due to deformation in the Precambrian.
A zone of closely spaced fractures that dip 65° west is present at the corner of the cut. This is probably related to late (Triassic?) minor fault movement.

Inwood Marble Member B
Several exposures of member B of the Inwood Marble are along the right (east) side of the road.

Inwood Marble-Manhattan Schist contact.
Turn right (northeast) onto Route 100B and proceed northeast across the Inwood Marble-Manhattan Schist contact.

Inwood Marble in center of anticline
Turn left (north) onto Route 100A (Knollwood Rd. ). The broad valley to the northeast (right front) is underlain by Inwood Marble in the center of a south plunging anticline. Proceed northward along the west limb of this anticline.

Proceed east across the anticlinal valley.

Manhattan Schist Members A, B, and C
Large road cuts expose members A, B, and C of the Manhattan Schist on the east limb of the anticline.

Manhattan Schist Member C
The extensive road cuts on the left (north) side of the expressway expose member C of the Manhattan Schist in the trough of a south plunging syncline.

Inwood Marble contact with Fordham
The expressway overpasses the Bronx River Valley which is here underlain by Inwood Marble. We cross the Inwood-Fordham contact and proceed down through the upper limb and across the axial surface of an early stage nappe-like fold.

Fordham Gneiss and Yonkers Gneiss
Extensive road cuts expose multiply deformed Fordham Gneiss and Yonkers Gneiss in the core of the early stage fold.

Calcite marble and schist
A road cut on the right (south) side of the expressway exposes interbedded calcite marble and schist at the base of member A of the Manhattan Schist. The contact of these rocks with the Fordham Gneiss is essentially exposed here and is an example of a place where the Middle Ordovician rocks rest directly on Precambrian. We are on the lower limb of the early stage nappe-like fold which has been refolded into an anticline and we are here located on the west limb of this later stage anticline. The lower part of the Manhattan exposed here compares favorably with the fossil bearing beds at Stop 5 and Stop 7 on Trip H (Ratcliffe, this guidebook).

East limb of the later stage anticline.
All of this maneuvering has allowed us to cross the axial plane of the later stage anticline to the east limb but we remain on the lower limb of the early stage nappe-like fold. Proceed northward along the east limb of the later stage anticline.

Proceed along the west limb of the later stage anticline.

STOP 5. Silver Lake.
We are permitted to use this park through the courtesy of the town of Harrison. Please don't litter the area with trash.
An exposure of member A of the Inwood Marble is present near the entrance to Silver Lake Park. Walk northward along the east side of Silver Lake and, in so doing, proceed along the east limb of the northerly plunging later stage anticline and at the same time along the lower limb of the earlier stage nappe-like isoclinal fold. (Figure 4). The steep topography on the west side and at the north end of the lake is underlain by Fordham Gneiss and the ridge on the east by Yonkers and Fordham. We are located on the Paleozoic rocks and the contact at their stratigraphic base projects in the air above our heads so that the stratigraphy is completely inverted here. Walk to the north end of the lake where the hinge of the later stage anticlinal fold is located (Figure 4). Walk northward, up the hill and down the stratigraphic section through the Lowerre Quartzite into the Fordham Gneiss. Note that the bedding in the Lowerre dips northward and thus projects beneath the older Fordham. In walking up the hill we are proceeding across the lower limb of the earlier stage nappe-like fold and essentially along the axial trace of the later stage fold.
The Lowerre here consists of tan to brown weathering gray feldspathic granulite, tan-weathering quartzite and micaceous quartzite, interbedded half-inch to two-inch thick beds of white quartzite and feldspathic granulite. Brown to rusty-weathering feldspathic granulite and feldspathic schist with local sillimanite nodules characterize the basal Lowerre here. The Fordham consists predominantly of gray biotite-quartz-feldspar gneiss.
Minor structural features abound in these rock exposures. Most of the linear elements plunge at 40° to 60° northwestward and apparently are parallel to the plunge of the later stage anticline.

Lowerre Quartzite
There is an exposure of Lowerre Quartzite behind the milk plant on the northwest side of Silver Lake.

Axial surface of nappe-like fold
Proceed north across unexposed Fordham Gneiss and up through the axial surface of the nappe-like fold to the upper limb.

Exposures along either side of the road are Fordham Gneiss.

Kensico Dam
The rock facing on this dam is Yonkers Gneiss that was quarried from the hills to the east of the Kensico Reservoir called "Quarry Heights". Fordham Gneiss is at the east end of the dam, Manhattan Schist is at the west end and the Inwood Marble, though not exposed, is in between.

The New York City Water Supply aerators are on the right.
The aeroators are gone, and the site is being used for fill.

Interbedded calcite marble and schist
Interbedded calcite marble and schist at the base of member A of the Manhattan Schist are exposed in the road cut on the right (northwest) side of the road.

STOP 6. United States Post Office in Thornwood.
Member A of the Manhattan Schist is exposed in the cuts alongside and behind the buildings. Characteristic gray and dark-gray sillimanite-garnet muscovite-biotite schist of member A is present here. Before the recent construction and paving, there was an exposure of interbedded white calcite marble and schist here. These rocks compare favorably with the lower portions of the Manhattan Schist that are to be visited on Trip H (Ratcliffe, this guidebook).

STOP 7. Exposures along the east side of Elwood St.
The exposures of member A of the Manhattan Schist behind the buildings as well as on the wooded slope consist of the typical fissile schist and some gray and white calcite marble beds. Definite interbedding of marble and schist cannot be proven here although there are at least two exposures that strongly suggest such a relationship.

STOP 8. Member E of the Inwood Marble.
Park beyond the United States Post Office at the end of the street. Walk south over the hill toward the Taconic State Parkway. An exposure of member E of the Inwood is on the west side of the hill along the east edge of the Taconic State Parkway. The contact between gray-weathering calcite marble (member D?) and tan-weathering calcite marble, typical of member E, outline a tight isoclinal fold.

Inwood Marble Member D
The large roadcut on the south side of the intersection is in member D of the Inwood and there are exposures of member E up on the hill south of the road cut. Proceed southward on Route 9A along the west limb of a syncline with Fordham Gneiss underlying the hills on the west and Manhattan Schist those on the east.

STOP 9. Member E of the Inwood Marble.
These exposures are typical of member E of the Inwood Marble and consist predominantly of tan and gray-weathering calcite marbles. Note the many northeast plunging folds.

Proceed southward continuing in the Inwood Marble.

Unconformity at the base of the Lowerre Quartzite
There is an excellent exposure of the unconformity at the base of the Lowerre Quartzite in a cut behind the A & P warehouses west of Route 9A. There are extensive exposures of Lowerre on the hillside extending all the way across the Saw Mill River Parkway to the west. Continue southward through Elmsford more or less along the Inwood-Manhattan contact.

STOP 10. Warburg Campus.
Park in the parking lot north of Woodlands High School. This 160 acre campus is a former estate of Felix Warburg that was given to the town of Greenburgh for educational purposes. The classroom buildings on the campus accommodate 3000 students from kindergarten through high school. We have been granted permission to visit this area by the administration of Greenburgh School District No.8.
The rocks here are at the nose of a southwest-plunging later-stage anticline (Figure 5). Evidence for two, and possibly three, phases of deformation is displayed by minor structural features. The contacts between amphibolite (member B of the Manhattan) and schist, schistose gneiss and granulite that are typical of member C of the Manhattan outline the fold (Figure 5). Note that member B is above the base of member C here.
Some areas of particular interest are indicated on the map (Figure 5) by lower case letters. The upper and lower contacts of the amphibolite are easily identified in the vicinity of point "a" where gray to brownish-weathering feldspathic garnet-muscovite-biotite schistose gneiss, gneiss and granulite with local white sillimanite nodules is below as well as above the amphibolite. Trace the contacts south-eastward by walking across the valley to exposures on the steep slope west of the classroom building in the vicinity of point "b" on Figure 5. The lower amphibolite contact is folded here and though there are several examples of the results of multiple deformation, a particularly fine example of a refolded fold is present near the north end of these exposures. Evidence for three stages of deformation is found here where the slip cleavage that deforms an earlier foliation appears to be folded.
Proceed southeast over the top of the hill where amphibolite is well exposed. An unusual occurrence of magnetite with white quartzfeldspar rims is present in the amphibolite on the southeast side of the hill. Many interesting minor structural features are present in the rocks on the hill in the vicinity of "c" (figure 5). Toward the north between the gym and the classroom building is an exposure of schist with particularly good examples of sillimanite nodules.

Inwood Marble Member B
Road cuts here expose member B of the Inwood Marble and a particularly good exposure of member B is present on the east (left) side of Route 9A between the Thruway overpass and the southbound Thruway entrance.

Manhattan C on the left (east).

Manhattan C on both sides of the highway.

Road cuts in the Fordham Gneiss.

Yonkers Gneiss on the left (East).

Fordham Gneiss is on the right (west).

Fordham Gneiss is on both sides of the highway.

Yonkers Gneiss
Yonkers Gneiss is exposed in the old quarry on the right (west) and there are active quarries in the Yonkers a little further west. This is in the area specified by Merrill (1890, p. 388) as typifying the Yonkers Gneiss.

Yonkers Gneiss
Yonkers Gneiss is exposed in a cut along the Thruway exit ramp on the left (east).

Highview Reservoir is on the left (east).

STOP 11. Type locality of the Lowerre Quartzite.
This is the type locality of the Lowerre Quartzite designated by Merrill (1896, p. 26). The portion of the Lowerre now exposed here is predominantly well bedded gray and tan-weathering feldspathic granulite and gray feldspathic muscovite-biotite schist that weathers tan to brown. Typical tan-weathering quartzite is present about forty to fifty feet above the base but is subordinate. It seems likely that more of the characteristic quartzite was exposed here when Merrill originally defined the Lowerre but that it has since been removed through the work of man. It also appears that Merrill used the modifier "quartzite" in the name Lowerre Quartzite because the most distinct rock types that characterize the assemblage of rocks in this formation are tan weathering quartzite and feldspathic quartzite.
The Fordham Gneiss beneath the Lowerre consists mainly of amphibolite with some gray garnet-biotite-gneiss. This is another place, similar to STOP 5, where the base of the Lowerre is "dirty". There are other places, such as the cut behind the A & P warehouses at mileage 36.3 (this field trip), where clean quartzite and feldspathic quartzite are directly in contact with Fordham.
The unconformity here is deformed into a series of northeast plunging sinistral folds. This is in accord with the map pattern in this vicinity (Merrill and others, 1902) which indicates the rocks here are on the west limb of a stratigraphic syncline.

B: CRETACEOUS DELTAS IN THE NORTHERN NEW JERSEY COASTAL PLAIN
By James P. Owens, James P. Minard, and Norman F. Sohl.
U. S. Geological Survey, Washington, D. C. 20242
(Publication authorized by the Director, U. S. Geological Survey.)
INTRODUCTION
In recent years there has been a growing recognition of the importance of deltaic deposits in many sedimentary basins. The extensive investigation of modern deltas has resulted in the isolation and description of many of the subenvironments of this very complex sedimentation system. On this field trip, some of the subenvironments of an ancient deltaic system will be examined.

B: CRETACEOUS DELTAS IN THE NORTHERN NEW JERSEY COASTAL PLAIN

STOP 1. Woodbridge clay of the Raritan Formation (Figure 8).
Section as follows:
5-10 feet of sand and gravel of the Pensauken Formation.
30-40 feet of interbedded sand and clay of the Woodbridge unit of the Raritan Formation. Numerous layers of siderite and iron oxide-cemented sand are present. Some sand layers contain marine fossils. Interpreted as prodelta-bottomset beds.
5-6 feet of sand and clay containing much wood. Some wood appears to be in an upright position. Probable marsh deposits.
20 feet of dark-gray clay which is weathered at the top. Possible lagoonal origin.

STOP 2. Sayreville Sand Member of the Raritan Formation (Figure 9).
Section as follows:
20-40 feet of cross-stratified sand exposed in the pit walls. Interpreted as channel-fill and spit facies.

STOP 3. Laminated beds of sand and clay of the Morgan beds
Laminated beds of sand and clay of the Morgan beds (Berry, 1906) in the lower part of the Magothy Formation (Figure 10). Section as follows:
15-25 feet of alternating beds of yellow-brown to light-gray micaceous quartz sand and clay. A considerable amount of carbonaceous matter is present throughout. Interpreted as natural levee deposits.

STOP 4. Magothy Formation
Magothy Formation overlain by several feet of Merchantville Formation and Pleistocene sand and gravel (Figure 11). Section as follows:
5-6 feet of Pleistocene silt, sand, and gravel.
5-6 feet of dark-greenish-black quartz-glauconite sand of the Merchantville Formation. Interpreted as prodelta to open shelf deposits.
8 feet of dark-gray clay with some sand partings.
12 feet of alternating dark-gray to black clay and light-gray quartz sand layers. Layers are about 1/4 to 1/2 inch thick. Pyrite nodules are present throughout.
12 feet of white to light-gray quartz sand with some lignite and clay layers. The above 32 feet of the Magothy is interpreted as top set and foreset beds.
1 foot of gray-black clay with light-gray quartz sand and siderite concretions (exposed at low tide). Fossils are present in the siderite. Interpreted as prodelta and bottomset beds.

STOP 5. Merchantville Formation
Merchantville Formation overlain by several feet of Pleistocene sand and gravel and spoil from the Woodbury Clay (Figure 12). Section as follows:
5-10 feet or more of Pleistocene sand and gravel and disturbed Woodbury Clay. Apparently was disturbed and intermixed during excavation or subsequent pushing aside.
20 feet, plus or minus, of dark-greenish and grayish-black sandy silt and clay and sandy clay of the Merchantville Formation. Contains abundant mica, glauconite, and layers of siderite. Interpreted as prodelta and bottomset deposits.
Several feet of the upper, weathered sand and clay layers of the Magothy can be seen near the entrance of the pit.

STOP 6. Upper Navesink Formation
Upper Navesink Formation overlain by lower part of the Red Bank Formation (Figure 13). Section as follows: 25 feet of the lower part of the Red Bank Formation (Sandy Hook Member). Mostly fine-to medium-grained quartz sand with considerable feldspar, much mica (green and colorless), and some glauconite, particularly in the base. The upper part of the section is weathered to brown, the lower part is dark-gray. Micro-fossils and small megafossils and shell fragments are abundant in the dark basal part, and this unit is more clayey and compact.
15 feet of greenish-black, clayey, glauconite sand of the Navesink Formation. Several shell beds are present. Exogyra, Pycnodonte, Ostrea, Choristothyris, and Belemnitella are common. (The total thickness of the Navesink is about 25 feet here).
These sediments are interpreted as open shelf marine deposits heyond the laminated prodelta beds. Except for the shell beds there is a lack of conspicuous bedding. The abundance of glauconite is suggestive of deeper water and more uniform sedimentation.

C: THE TRIASSIC ROCKS OF THE NORTHERN NEWARK BASIN
By E. Lynn Savage, Brooklyn College of The City University of New York
INTRODUCTION
Objectives of the Field Trip.
Outcrops to be visited on this trip have been selected to illustrate some of the problems involved in the interpretation of Triassic rock units and facies in the northern Newark Basin. (Figure 1). Where possible emphasis is directed toward general Triassic problems, as well as to those which are unique to the northernmost area of this basin.
Although it is generally accepted that much of the Triassic has been removed by erosion, there are two contrasting ideas as to whether the present northeastern end of the Newark Basin marks the former extent of the sediments:
(1) The present outcrop area is almost the same as the original extent (McLaughlin, 1957, p. 1498; Glaeser, 1966, p. 101).
(2) The sediments were once much more extensive, covering the area between the New Jersey-New York Trough and the Connecticut Trough (Sanders, 1963, 1960; MacLachlan, 1957, p. 13; Wheeler, 1938).

C: THE TRIASSIC ROCKS OF THE NORTHERN NEWARK BASIN

Southwest end of fault
Tunnel plaza and portal to north (left) are at southwest end of fault (Figure 12 A, B) cutting diagonally across Palisade Sill. Downdropped block is on east (right) side. There are many such faults along the Palisades.

Jointed diabase on left.

Regional erosion surface levels top of sill
Small park on right (east) commemorates duel between Aaron Burr and Alexander Hamilton. Regional erosion surface levels top of sill (Figure 13).

Olivine zone in Palisade Sill on left (see Figure 15A).

Stockton arkose on left
Metamorphosed rather well-sorted yellowish-gray to very pale orange Stockton arkose and overlying chilled border of sill on left.
Coarse-grained arkose at contact, locally cross-bedded with dispersal to S or SW, contains abundant plagioclase and orthoclase, some quartz, pale green diopside and vermiculite,. and minor sphene and talc. Finegrained arkose within 12 inches of the contact consists mainly of albite, with minor vermiculite and talc, and a trace of chlorite.

Stockton arkose on left.

Large columnar joints with smaller joints in lower part of sill. Talus.

Stockton arkose and cliff of sill
Stockton arkose and cliff of sill on left (just south of Lever Brothers Research Center). Bedded, coarse to very coarse-grained arkose with 2-foot unit of tabular cross-bedding with dispersal to SW.

Well-bedded, very dark, fine-grained Lockatong hornfels.

STOP 1 Gorge and River Roads. Lockatong Hornfels
Gorge and River Roads. Lockatong Hornfels. Time here: 30 minutes. Park in lot of Celatex Corp. (Allied Chemical).
A composite section of Lockatong hornfels and interbedded stockton arkose is exposed in the excavation (watch for falling rock) on River Road (Figure 14A) opposite the Mobile Service Center and in the roadcut on the west side of Gorge Road (Figure 14B). This sequence (strike N 40° E, dip 15° W) consists of (1) about 18 feet of dark gray, well-bedded Lockatong hornfels in 3 well-developed cycles, overlain by (2) about 15 feet of bedded, rather well-sorted yellowish-gray Stockton arkose, which is in turn overlain by (3) about 50 feet of dark gray, well-bedded Lockatong hornfels below the Palisade Sill.
1. The asymmetrical cycles in the excavation are analcine-bearing "chemical" cycles like those found in western New Jersey and adjacent Pennsylvania (Van Houten, 1964, 1965). Because of their unique composition, these deposits were easily altered by isochemical thermal metamorphism. In contrast, the arkose 50 feet below the sill is virtually unaltered. In pattern, each cycle (Figure 14C) originally consisted of a lower very dark gray to black shaly to platy carbonate-rich feldspathic mudstone (converted to a biotite-albite hornfels) with thin laminae and local beds (1 to 3 cm) of calcite and dolomite, a middle platy carbonate-rich portion with abundant disruption by shrinkage, converted to a calc-silicate hornfels, and an upper massive analcine-rich argillite, now commonly with a splotched fabric produced by metamorphism to a biotitealbite-analacine hornfels.
2. The slightly metamorphosed arkose 50 feet below the sill consists mainly of plagioclase, orthoclase and quartz, some vermiculite, and a trace of talc.
3. Spotted Lockatong hornfels of a tetrital cycle within 5 feet of the sill consists mainly of biotite and plagioclase, some orthoclase and andalusite, and a trace of chlorite and magnetite. Lockatong hornfels 15 to 20 feet below the sill contains minor analcime.
The following additional accessory minerals have been found in this hornfels facies (Lewis, 1908, p. 136-147): pale green augite, apatite, cordierite, epidote, hornblende, sillimanite, scapolite, dark-green spinel, sphere, tourmaline, and vesuvianite.
The variations in mineral assemblages found here and in the Granton Quarry (STOP 8) resulted largely from differences in composition and amount of water present, and not from major differences in temperature and pressure.

Large xenolith of Lockatong hornfels
Large xenolith (15 feet by 30 feet) of Lockatong hornfels about 15 to 20 feet above base of sill, exposed behind Virginia Lee Lace Co. Baking produced coarse-grained biotite-plagioclase hornfels with chlorite, pale green and colorless pyroxenes, and more coarsely crystalline stringers of chlorite, biotite, calcite, diopside, albite and very pale green muscovite.

Sill exposed on left (west), hornfels in cut to east (right).

Lockatong hornfels below sill behind Edgewater Welding Co.

Stockton arkose and Lockatong hornfels
Stockton arkose and Lockatong hornfels behind Edgewater sewage treatment plant.

STOP 2. Palisade Sill and Lockatong Hornfels
Palisade Sill and Lockatong Hornfels along abandoned trolley route. Time here: 1 hour. Park on east side of Undercliff Avenue, opposite small park with 3 benches.
Traverse through Palisade tholeiitic diabase sill (Figure 15 A, B, C) - up (southwest) an abandoned trolley route along a brook, behind houses:
Lockatong Hornfels below sill, as at STOP 1.
Irregular cross-cutting contact (Figure 16A).
Xenolith 2 feet thick, 15 feet above base of sill; unusually coarse-grained biotite-plagioclase hornfels.
Olivine diabase, generally about 15 feet thick, 50 feet above the base at switch-back on trolley route. Dr. S. Bhattacharji will discuss its origin.
Normal diabase throughout the middle of the sill.
Upper coarse diabase with pegmatitic schlieren.
Upper chilled border.
Hypotheses proposed to explain differentiation of the diabase sill and to account for the layer of olivine diabase are:
1. Gravitational settling of early-formed olivine and later pyroxene crystals (F. Walker, 1940). Although widely cited as such, the Palisade Sill probably is not a good example of gravitational differentiation. -
2. Fractional crystallization (Figure VH 2, C) by ionic diffusion and convection circulation of magma, supplemented by minor gravitational settling of large olivine crystals (Hess, 1956, p. 1960).
3. Fractional crystallization, with late-stage injection of a new pulse of magma into the partially crystallized mush. Large olivine crystals concentrated by gravitational settling (K.R. Walker, 1962; 1967 in press).
4. Mechanical or hydrodynamic flow differentiation, with central concentration of early-formed olivine crystals during intrusion of the magma. Crystal mush then settled as a result of fluctuation of velocity and pressure (S. Bhattacharji, 1967).

Olivine zone halfway up cliff on left.

Olivine zone is at road level.

Outcrop of sill on right.

Phytosaur was found below the bridge
A phytosaur, Clepsysaurus (Rutiodon) was found in the stockton arkose below the bridge.

Outcrops of sill on both sides of road.

Outcrop of sill.

Outcrop of sill on left.

Outcrop of sill on right. Lipton Company on left.

Glacially polished diabase on right.

Jointed diabase on both sides of road.

Glaciated diabase on right

Stocton arkose, dikes
Along Hudson River at Sneden's Landing approximately 45 feet of light gray thick-bedded and locally cross-bedded Stockton arkose is interbedded with reddish-brown to pale lavender baked mudstone. Dispersal was to the northwest (Figure 11). Locally dikes of arkose have been injected into the mudstone. The arkose contains angular pebbles of quartz and pink feldspar as much as an inch in diameter; in contrast to sandstone found north of Piermont (and higher in the stratigraphic sequence) zircon, rutile and authigenic anatase are abundant, tourmaline and garnet are rare, and metamorphic rock fragments are absent (Savage, 1967).

Outcrops of diabase at entrance to Tallman's State Park. Olivine zone.

Sparkill Gap.
Sparkill (formerly Overpeck) Creek in the gorge is the only stream that flows eastward across the Palisade Sill into the Hudson River. Presumably it flows along a cross-fault (such as seen at Lincoln Tunnel plaza) that has offset the sill more than 900 feet westward on the north side.
According to Johnson (1931) the Hudson River originally flowed southwestward on the Schooley erosion surface above the position of the sill, was superposed on it and cut a water gap (Figure 17). Later a subsequent stream flowing on relatively non-resistant rocks east of the sill captured the ancient Hudson drainage by headward erosion. Overpeck Creek then reversed the original drainage direction. This explanation does not account for the coincidence of the gap and a cross-fault (see Thornbury, 1954, p. 234-240, for discussion of the problem).
Between Piermont and Nyack Beach State Park (STOP 3), there are many outcrops and abandoned quarries of "brownstone" which was used extensively for building-stone more than 50 years ago. Most of the rock is a dark brown to reddish brown well-sorted medium to fine-grained arkose, commonly interbedded with reddish brown mudstone. Some of the lighter colored arkose is coarser grained, but conglomerate is rare. Presumably these deposits are a gradational sequence between the uppermost part of the Stockton Formation and the lower part of the Brunswick Formation, and differ in heavy mineral content, sedimentary-metamorphic rock content and dispersal direction from those in the upper part of the Stockton Formation to the south (Savage, 1967, p. 34).

Glacial till overlying diabase on right.

More till on diabase on right.

Outcrop of diabase on left.

View of south end of Verdreitege Hook
View of south end of Verdreitege Hook (Hook Mountain) portion of Palisade Sill above Nyack Beach state Park.

Large glacial erratic on right, on lawn of library built of "fieldstone. "

South end of Verdreitege Hook with spectacular talus slope.
5 minute stop for photographs.
North of Nyack the Palisades are as much as a mile west of the Hudson River because the sill intruded a higher part of the west-dipping Newark sequence. Then it swings back to the river at Nyack Beach state Park, cutting across somewhat lower Newark strata (Figure 3). At its north end the intrusion is a dike that intrudes successively higher Brunswick beds (Figure 2) and turns sharply to the west almost perpendicular to strike; at its western end it completes a sickle-shaped arc. Diamond-drilling in a quarry at Little Tor near Haverstraw shows that the intrusion dips about 45° SW (Lowe, 1959).
A distinct olivine-rich zone is absent at the northern end of the Palisade intrusion as it is at its southwestern end in west-central New Jersey. Nyack Beach state Park.

STOP 3. Lower Brunswick deposits.
Nyack Beach state Park. Lower Brunswick deposits. Time here: 1 hr. 45 min.
LUNCH will be served after a 1 and 1/3 mile walk to outcrops in the lower part of the Brunswick Formation.
The Park authorities have made this convenient stop available to us. Do not disturb the foliage or the crops. Please collect specimens only in those areas where there has been recent blasting of ledges. Watch out for copperhead snakes, yellow-jacket wasps, poison ivy and poison sumac.
Traverse along footpath leading north from north end of parking area.
Distances noted below were measured from beginning of the path.
200': 15 to 20 feet of yellowish-gray arkose crop out 40 inches above the path.
895-950': Picnic tables; old quarry in reddish-brown mudstone and yellowish-gray arkose.
1450-1570' : Outcrop exhibiting rapid facies changes, especially at north and south ends:
7': Massive reddish-brown mudstone; cross-bedded; marked channelling. 8': Reddish-brown shale.
13' : Micaceous reddish-brown siltstone and shale; cross-bedded. Scattered pebbles of quartzite and quartz, and pieces of shales.
8': Reddish-brown shale.
2' 0 Massive reddish-brown mudstone. Path level
2215-3745': More talus; columnar joints in diabase. Note sinuous joint surfaces. Pass fireplaces.
3745-3925': Tree-clad slope.
4040-4405': Outcrop near open stone shelter:
10': Massive light gray arkose, locally cross-bedded.
2': Reddish-brown mudstone.
4': Thin-bedded, pale reddish-brown arkose, interbedded brown mudstone.
8': Massive, tough light-gray arkose, rare cross-bedding and coarse layers with pebbles of angular quartz as much as 2 1/2 inches in diameter, pieces of feldspar as much as 1 inch long and intraformational mudstone clasts.
Path level.
Continue along winding path. Diabase above is conspicuously jointed. Sing-Sing prison across river to east.
5571-6039': At south end diabase is at path level. Rises to north to reveal contact with arkose which has not been metamorphosed more than a few feet from the sill. Beware of yellow jacket nests in brush near this contact.
6039-6080': Covero Beyond retaining wall 10 feet of cross-bedded light-gray arkose overlies reddish-brown mudstone.
6445-6465': Arkose with rare gray limestone and quartz clasts to 1 inch in diameter; pink feldspar to 2 inches in diameter, and rare pebbles of pegmatite.
6570': Arkose in large block is cross-bedded, contains clasts of quartz, red sandstone, pink feldspar, shale, mica schist, and relatively abundant almandine garnet.
6575': Excellent outcrop extends northward for about 1000 feet. Exhibits rapid facies changes and variety of sedimentary features characteristic of fluvial sedimentation (Figure 18A). N62W, 13° W.
5': Yellowish-gray arkose with large scale chamleling and cross-bedding.
6': Interbedded yellowish-gray arkose and reddish-brown mudstone. Unit pinches out to north.
11': Reddish-brown to lavender mudstone with irregular upper contact. Cross-bedding, with scour and fill, burrowing, mudcracks, and ripplemarks (2 inch crests, N68W), as well as load and flute casts. Interbedded with layers of medium to coarsegrained micaceous reddish-brown arkose grading (Figure 18A) into lensing buff and lavender arkose with pebbles of limestone and feldspar. The lower part of the mudstone also contains pebbles of quartzite, quartz and feldspar. About 5 feet above the base at the south end of the outcrop a greenish-gray layer consists largely of rounded grains of silty mudstone. Some may be Paleozoic lithic grains, but many with concentric structure, elongate shape and calcite cores apparently are intraformational mud pellets.
6580': Very coarse arkose with angular quartz as much as 1 inch in diameter, pieces of shale parallel to bedding, and clasts of limestone and feldspar, interfingers with reddish-brown mudstone.
6665': Well-developed tabular cross-bedding, rare in Newark rocks in Rockland County.
6755': Upper contact of lower reddish-brown mudstone unit is about 5 feet above the path.
6755-6770': Arkose scoured by channels. Reddish-brown mudstone dikes at north end probably was injected during burial (Figure 18B).
6775':
5': Massive yellowish-gray arkose.
5': Interbedded reddish-brown mudstone and tan arkose.
11': Reddish-brown mudstone.
Northward the top of the extensively burrowed lower unit is 8 feet above the path and is overlain by mottled arkose 11 feet thick which in turn is overlain by 4 feet of yellowish-gray arkose with large scale cross-bedding (Figure 19A).
6930': Slumped mudstone 3 feet above path.
6980-7015': Six inch layers of reddish-brown mudstone interbedded with reddish-brown silty sandstone a few inches thick with marked cross-bedding and scour and fill (Figure 19B).
7185': Well-developed cross-bedding in yellowish-gray arkose. Return to Park. LUNCH will be served at tables south of the parking area. Time here: 30 minutes.

Metamorphosed arkose and mudstone
Thermally metamorphosed yellowish-gray arkose and reddish-brown mudstone (as seen at STOP 3) in excavation on left.

Beginning of roadcut through Verdreitege Hook
Beginning of roadcut through Verdreitege Hook to inner side of the "sickle" (Figure 1).

Fault controlled gaps?
Gaps to east (right) and northeast (ahead) across Palisades may be controlled by faults (Thompson, 1959) or are former superposed stream valleys (Kummel, 1898, p.24).

Erratics on shore of Rockland Lake.

Gneiss and diabase erratics in till on right.
Some are more than 6 feet long.

Excavation in till.

Polygonal jointing
Unusually well-developed polygonal jointing in diabase at right, and in New York Trap Rock Quarry at Little Tor above road to left. North side of "sickle."

Talus slope up hill on left.

Arkose above tough reddish-brown mudstone on left,
Arkose above tough reddish-brown mudstone on left, on northern and outer side of the "sickle. "

Talus with very steep angle of repose.

Scarp has receded to the west.

North rim of High Tor
Road follows the north rim of High Tor and progressively crosses younger strata to the west.

Ramapo Mountains visible to the west.

Glacial erratics common.

Deposit of meltwater delta (?) on right
Deposit of meltwater delta (?) on right; in lowland between sill (left) and Ramapo Mountains (right).

Sand and Gravel quarry
Mt. Ivy Sand and Gravel Company quarry in Mt. Ivy meltwater delta dispersed to the south or southwest. About 5 feet of steeply dipping, light tan fore set beds above 8 to 10 feet of horizontal dark brown and reddish-brown to dark gray beds, and overlain by very poorly-sorted glacial (?) deposits.

Ramapo Mountains rise to west.

Outcrop of Ladentown diabase.
The Ladentown diabase extends for about 2 miles along the road, forming a series of low hills. It is crossed by several streams and is locally covered by glacial drift. The rock varies from fine-grained diabase to medium-grained vesicular basalt with intersertal texture, and structures like pahoehoe have been reported.
This igneous mass may connect with the Palisade diabase across the 2-mile drift-covered stretch to Mt. Ivy (Kummel, 1898, p. 41). The flow-like features of the Ladentown sheet and its position high in the stratigraphic sequence suggest that here the northwest end of the Palisade intrusion may have reached the surface.

Steep hill of diabase on left (east).

Closely-spaced, curved joints in diabase
Closely-spaced, curved joints in diabase on left differ markedly from the large-scale vertical jointing in the sill along the Hudson River.

East-dipping poorly-sorted conglomerate
East-dipping poorly-sorted conglomerate with clasts of Paleozoic rocks. In lower part some clasts are 1 to 2 feet in diameter.

Limestone conglomerate underlying hill.

Hill steepens on left. Ladentown diabase.

Hill of Ladentown diabase
Hill of Ladentown diabase and outcrop at road level on left (north). Fine-grained vesicular diabase with intersertal texture, but without flow texture in specimen examined. Interstices filled with very dark devitrified glass; scattered patches of iddingsite, amygdules of wordenite with a slender vein of quartz in some.

Abandoned quarries in limestone conglomerate
One of several abandoned quarries in limestone conglomerate on farm on southeast corner of intersection. Exposure of conglomerate on glaciated surface between old barn and house, just west of the private driveway.

STOP 4. Border Conglomerate in Upper Brunswick Formation.
Time here: 20 minutes.
This spectacular border conglomerate consists of rounded clasts as much as 4 feet in diameter in gravelly reddish-brown sandstone. Most of the clasts are gray cherty limestone, formerly quarried for burnt lime. Clasts of quartzite and sandstone are also present. The conglomerate is remarkably closely packed with little matrix. Conglomerate in this area east of the Ladentown diabase dips about 5° west (Klimmel, 1898, p. 40). See Figure 20 A, B.
This fanglomerate facies occurs at several places along the western boundary of the Triassic basin and is well-known as the "Potomac Marble" from Point of Rocks, Maryland.

Drive along the fault zone at the western border of the Triassic basin.
Ramapo Mountains to the west. The road parallels the Mahwah River which flows along the fault zone at the western border of the Triassic basin.

STOP 5. Border Conglomerate in uppermost Brunswick Formation.
Time here: 30 minutes.
The section exposed along the west side consists of about 10 feet of boulder conglomerate interbedded with, and overlain by reddish-brown gravelly sandstone. The clasts consist largely of a variety of Paleozoic limestones, together with red sandstone and Green Pond (Silurian) conglomerate and quartzite.
On the east side of US 202 the deposits are less coarse, and exhibit well-developed cross-bedding with dispersal direction to the south. The regional dip of the sequence is to the southeast, toward the Ladentown diabase (Figure 20 A, B).
A 12-foot limestone boulder has been reported just south of here.

Gneiss of Ramapo Mountains exposed on right

Exposure of slickensides in the Ramapo Fault zone.
Present relief between Precambrian crystalline rocks and Triassic sedimentary rocks is due to differential erosion. Top of hill on gneiss; quarry in diabase of Union Hill seen to the southeast.
At Union Hill, the trap is associated with dark purplish-red cobble conglomerate which contains clasts of quartzite, reddish-brown, greenish-gray and gray limestone, and amygduloidal basalt. The largest clasts present are as much as 1 foot in diameter and one 3 feet in diameter has been reported. About 30 percent of the clasts here are limestone.

Glacial erratics on right.

Glacial drift on right.

STOP 6. East end of Cherry Hill - NY 59. Brunswick Formation.
Time here: 30 minutes.
The Clarkstown Police will conduct our group across the highway to the best outcrops on the north side of the road.
This section in the lower part of the Brunswick Formation is about 0.2 miles long and consists of about 125 feet of strata (N30E, 6°W) composed of interbedded buff to reddish-brown feldspar-rich sandstone and reddish-brown mudstone. Many of the layers have well-developed crossbedding (Figure 21) commonly in the 1 to 2-foot sets; one cross-bedded unit is 11 feet thick. Dispersal direction generally is to the southeast, although some cross-beds dip westward (Figure 11). Unbedded mudstone and fine-grained sandstone apparently were mottled by burrowers.
The feldspar-rich sandstones here, as in much of the Stockton Formation, contain relatively abundant sodic plagioclase.
The traverse proceeds from east to west along the outcrop:
Top of Sequence (west end).
50'+: Reddish-brown mudstone, variably silty and fissile, with local sandy layers, On south side of road, at about this level, a 1-foot pebbly layer contains quartz clasts as much as 1/2 inch in diameter.
20': Reddish-brown sandstone interbedded with mudstone that is variably fissile. Base is marked by scour and fill, or flutes, and the basal bed contains intraformational mud chips. Lowest sandstone unit is conspicuously parallel-bedded, with convolutions overturned to the east. Local ripple-marks have crests trending N27°E. Scour and fill is common throughout the sequence.
Mudstone in the lower part of the unit contains a thin layer of drab mudstone with calcareous pellets. An ll-foot silty mudstone with thin layers of sandstone in the middle unit is conspicuously crossbedded.
15': Reddish-brown, cross-bedded mudstone, commonly weathers into slivers and chips. Drab calcareous nodules in upper part.
4': Reddish-brown sandstone with very thin mudstone interbeds, and a 3-inch layer of mudstone in the middle. Round mudstone clasts on some bedding planes; scattered quartz pebbles, locally in small lenses.
2.5': Reddish-brown fissile mudstone, with interbedded sandstone
10.5': Reddish-brown feldspathic sandstone. Commonly medium-grained with rare pebbles and locally cross-bedded.
5': Reddish-brown fissile mudstone.
East end of Outcrop.

STOP 7. Conglomerate in lower Brunswick Formation
Low ridge on lawn 157 Sickletown Road (Wright's property) consists of reddish-brown quartz pebble conglomerate and sandstone, locally crossbedded. Clasts are principally rounded quartz as much as 1 inch in diameter, a few pebbles are as much as 4 inches in diameter. This conglomerate, about 1/2 mile from STOP 6, emphasizes the lateral variation in Triassic deposits in Rockland County.

Outcrop of Palisade Sill on left.

Hill of cross-bedded calcareous arkose on right (west).
This sandstone with an interbedded 2-3 inch limestone unit (Kindle, 1944, p.4) overlies the Lockatong strata exposed in the Granton Quarry 1/2 mile to the south (see Figure 15A).

STOP 8. Lockatong Hornfels and subsidiary sill.
Enter driveway at south end of Diana Stores property. Drive to rear, turn right and drive to north end of property and south face of escarpment (see Colbert, 1966, Figures 1,2).
About 60 feet of Lockatong hornfels lies between the top of the Palisade Sill to the east and a subsidiary sill at Granton Quarry, North Bergen (Figures 15A, 16B, 22). The excellent exposure at the north end of the Diana Stores parking area consists of five complete hornfelsed "detrital" cycles (Van Houten, 1964), two of which are exposed along the east wall of the lower quarry. In contrast to the "chemical" cycles in the River Road excavation (STOP 1) each of these is thicker, shows extensive evidence of burrowing as well as shrinkage cracking, and contains cross-bedded siltstone and very fine-grained arkose pervaded by diopside in the upper part. The presence of prehnite and recrystallized feldspathized arkose in the middle and upper part of each cycle suggest metamorphism in presence of water vapor.
The overlying subsidiary sill, more than 20 feet thick, has been reported to contain an arkose xenolith a maximum of 10 feet thick and 100 feet long (Lewis, 1908, p. 135).
In spite of the extensive hornfelsing of the Lockatong rocks they still yield fossils of reptiles, fish, estheriids and plants (Colbert, 1965, 1966).

D: EXCURSION TO THE STERLING AND FRANKLIN AREA IN THE HIGHLANDS OF NEW JERSEY
By Eugene A. Alexandrov
Queens College of The City University of New York
GEOLOGY ALONG THE ROAD BETWEEN LONG ISLAND AND THE HIGHLANDS OF NEW JERSEY
The Geological trip to the Highlands of New Jersey starts at Queens College in Flushing and crosses the western part of Long Island in Queens County, the East River, Manhattan, the Hudson River, the Palisades, and the Lowlands of New Jersey.

D: EXCURSION TO THE STERLING AND FRANKLIN AREA IN THE HIGHLANDS OF NEW JERSEY

Crossing the Ronkonkoma terminal moraine.

Outwash Deposits
Grounds of the 1964-1965 New York World's Fair. Science Museum. The outwash deposits of Wisconsin age underlie the area between the terminal moraine and the East River.

Midtown Tunnel
Entrance to the Midtown Tunnel under the East River. The tunnel crosses ridges formed by Fordham Gneiss and Manhattan Schist, and depressions between the ridges eroded in Inwood Marble. The depressions are filled with Recent overburden.

Crossing Manhattan Schist
Crossing Manhattan along 34th St. , the underlying formations are mainly Manhattan Schist.

Entrance to Lincoln Tunnel
Entrance to Lincoln Tunnel under the Hudson River excavated in Recent sediments.

Western part of the tunnel crosses Upper Triassic continental seds
Boundary between the States of New York and New Jersey. The western part of the tunnel crosses the Upper Triassic continental sedimentary sequence underlying the diabase sill.

Crossing the escarpment of the diabase sill.

Fault in the diabase sill
Fault in the diabase sill (a narrow valley developed along this fault north of the road).

Leaving the diabase sill.
Leaving the diabase sill. The area is underlain by Upper Triassic shales, sandstones, and argillites. Turn northwest on Route 3 crossing the Hackensack Meadows.

Land rises because of harder sandstone
The land rises at the entrance to Rutherford because of the appearance of harder sandstones.

First Watchung Mountains formed by Triassic lava.

Lava with columnar jointing on the left side of the road.

Pillow lava structure on the left side of the road.

Triassic lava of the Second Watchung Mountains.

Triassic lava of Hook Mountain near Pine Brook. Third Watchung Mountains.

Escarpment formed by fault zone
Escarpment formed by the fault zone between the Precambrian Highlands and the Triassic basin (mantled by glacial till).

Entering Dover. Outcrops of Precambrian gneiss.

Crossing an inlier of Silurian rocks north of Dover.
Turning north on Route 15. Crossing an inlier of Silurian rocks north of Dover.

Visit to the mining property.
Sterling Hill Mine office of the New Jersey Zinc Co. Visit to the mining property.

Gerstmann's Private Museum of Franklin and Sterling Hill minerals, 14 Walsh Road, Franklin, N. J.

Oak Ridge Reservoir.
Northwestern border of graben in Precambrian gneiss -- inlier of Silurian and Devonian rocks. Southeast of Charlottesburg the rocks are Precambrian. The fault line separating the Highlands from the Triassic basin is crossed at Riverdale.

Triassic diabase sill.

E: TACONIAN ISLANDS AND THE SHORES OF APPALACHIA
By Robert M. Finks, Queens College of the City University of New York
Within the Precambrian Highlands of northern New Jersey and adjacent New York are several infolded and infaulted belts of Paleozoic sediments. The easternmost of tnese belts, e the Green Pond - Schunemunk outlier; preserves Silurian and Devonian rocks as well as Cambrian and Ordovician. The mid-Paleozoic sediments lie some 25 miles farther southeast than the main outcrop belt of the miogeosyncline, and represent a sampling of material deposited approximately that much nearer the source. They provide a record of those tectonic events and geographic conditions in the source area whose influence did not spread far enough to become manifest farther west.

E: TACONIAN ISLANDS AND THE SHORES OF APPALACHIA

Start of a spectacular new cut in the Palisades Diabase.

End of new cut
End of new cut, now overlying baked shales of the Newark Series may be seen, parallel to the top of the sill.

Meanders of the Hackensack River on its flood plain.

Road follows Passaic River flowing south.

Cut in First Watchung Basalt
Cut in First Watchung Basalt, an extrusive lava. Note curvicolumnar jointing.

Fanned columnar jointing
Fanned columnar jointing followed on LEFT by pillow-lava.

Passaic River flowing north in subsequent valley
Passaic River flowing north in subsequent valley between First and Second Watchung ridges. This is upstream from where we last saw it. It crosses First Watchung Ridge at Paterson Falls.

Second Watchung Basalt.

Third Watchung (Hook Mountain) Basalt.

Wisconsin terminal moraine.

Third Watchung (Hook Mountain) Basalt again.
Third Watchung (Hook Mountain) Basalt again. This has been bent around as part of a syncline in the Newark Series.

STOP 1. Pompton Lakes. Triassic Border conglomerate.
Turn left into Moyias Road and park. Walk across road (CARE!) and north along grass (STAY OFF PAVEMENT!) to outcrop.
(Wanaque, N.J., 7 1/2 - minute Quadrangle.)
This outcrop provides a sampling of the exposed bedrock that lay immediately to the west of here during late Triassic time. Coarse conglomerates such as this are confined to the immediate vicinity of the Triassic border fault and were apparently deposited as alluvial fans at the base of the fault scarp by east-flowing streams. No Precambrian pebbles can be recognized in this outcrop and presumably the Precambrian, now exposed in the hills immediately to the west, still lay covered beneath Paleozoic sediments. Large rounded cobbles, some more than a foot across, of a conglomerate of white quartz pebbles in a red quartzite matrix, closely resemble existing outcrops of the Silurian Green Pond Formation or the Devonian Skunnemunk Formation, both exposed in the outlier some ten miles west of here. Of more interest for the reconstruction of the paleogeography of the pre-Silurian uplift, is the abundance of white-weathering dolomite cobbles that could only have come from the Cambro-Ordovician carbonate sequence. These cobbles are sometimes less well rounded than the quartzite cobbles and must have been transported for no very great distance. The base of the Silurian rests directly on the Precambrian ten miles to the west. The CambroOrdovician carbonates were probably exposed somewhere between there and here in Triassic times and therefore could not have been removed during the pre-Silurian uplift. We will see at STOP 2 that the Trentonian phyllites are still preserved in this vicinity. These data place the eastern border of the pre-Silurian uplifted and eroded area as somewhere between here and STOP 3, only ten miles to the northwest.

STOP 2. Riverdale - Pomton. Annsville Phyllite.
(Pompton Plains, N. J., 7 1/2 - minute Quadrangle. )
After looking at the outcrop we will take a short REST STOP in the Riverdale Diner.
Walk east a little more than a block on the south side of the Hamburg Turnpike, crossing the bridge over the Wanaque River, and descend to the south side of the east abutment of the bridge. Here is exposed a small, but apparently genuine, outcrop of black phyllite; the outcrop is submerged at high water.
This outcrop was mapped as Hudson Schist in the USGS Passaic Folio (Darton, et al. , 1908) a name applied to the rocks now called Manhattan Schist, as well as to the metamorphosed pelites of the upper Hudson Valley now referred to the Normanskill - Snake Hill sequence (Ordovician, Trentonian). I see no reason to question these correlations. This outcrop is called Annsville here because it occurs in the same structural position as the type Annsville at Peekskill, 30 miles to the northeast along the Triassic border fault, and because it resembles the type Annsville lithologically. It also resembles lithologically ( and structurally: refoldedfoliation) the phyllitic phase of the Mount Merino Formation in Balk's classic area in Dutchess County, as at Noxon near Lagrangeville. Near Clinton, New Jersey, 40 miles to the southwest along the border fault, a sizeable patch of the Cambro-Ordovician sequence is exposed between the Triassic and the Precambrian. The Ordovician pelites in it were mapped as Martinsburg Shale (Bayley et al., 1914).
The present outcrop was interpreted in the Passaic Folio as a faultsliver, or "horse, " along the Triassic border fault. It is also possible that the pre-Triassic basement is generally much closer to the present surface along the border fault than usually reconstructed, and that much of the Triassic subsidence was taken up by faulting or warping farther east beneath the basin. The Cambro-Ordovician area near Clinton was mapped in the USGS Raritan Folio (Bayley et al., 1914) as lying uncomformably beneath the Triassic, and the present outcrop may have the same relationship.

Glacial lake delta on left. We have crossed Triassic border fault.

Outcrops of Precambrian gneiss.

Cut in Wisconsin till on left.

STOP 3. Newfoundland: South end of Kanouse Mountain.
Green Pond Formation. (Newfoundland, N. J., 7 1/2 minute Quadrangle. )
Walk north across old highway to nearest outcrop on north side of road. These are the lower conglomerate beds of the Silurian Green Pond Formation dipping steeply northwest. The conglomerate occurs in rhythmically repeated, upwardly-fining, 2 or 3 foot, cross-bedded units. Most of the pebbles are rounded milky-quartz, but red chert, dark shale, and other rock types occur.
Walk uphill, northeastward into the woods, paralleling the base of the cliffs but keeping about 50 feet east of them. About 100 feet or so into the woods large talus blocks of the lowermost beds are passed. They are more coarsely conglomeratic, and contain many angular or subangular pebbles, a few inches across, of green chert, red chert, quartzhematite phyllonite, quartzite, dark shale or slate, along with milky-quartz.
Another hundred feet or so further will bring you to the first outcrops of Precambrian Gneiss. An interval of 25 feet or so, covered with large talus blocks of Green Pond separates the nearest Precambrian outcrops from the exposures of Green Pond in the base of the cliffs. The contact is not exposed.
Return, following the base of the cliff as closely as talus and underbrush permit. At a point opposite the first ledges seen near the road, climb up to a broad rock surface on top of these ledges to observe spectacular Liesegang rings of hematite developed in the finer-grained layers of the rhythmic sequences. (WATCH YOUR STEP.)
Return to the road, cross the old highway and continue west across the grass plot to the main highway. Walk west along the shoulder (STAY OFF HIGHWAY! WATCH TRAFFIC!) to a cut in the Upper Quartzite Member of the Green Pond. The cut shows a small anticline and syncline parasitic upon the main synclinal structure (drag folds). A prominent thin pebble bed makes a convenient stratigraphic marker. Note well-developed quartz-filled gash-fractures along minor shear zones. At the westernmost end of the cut the lowermost red arkose beds of the Lower Arkose Member of the Longwood Formation are exposed in contact with the top of the Green Pond. These beds will be seen in the same stratigraphic position at Highland Mills (STOP 6-A).
(Note: A complete section between the basal beds and the Upper Quartzite Member is exposed in the woods along the south end of Kanouse Mountain, but we will not take the time to visit it. The Middle Arkose Member seen at the north end of the outlier (STOP 5) does not seem to be present here. )

Oak Ridge Reservoir.
Crossing high-angle fault between outlier and precambrian forming west boundary of outlier. Fault-line scarp visible to left along west shore of reservoir.

Flood plain of Pequannock River.

Entering small outlier of Cambro-Ordovician.

Outcrop on right of Cambro-Ordovician carbonate.

Dump of old Buckwheat zinc mine on right.
Franklin minerals may be collected here (fee). Outcrops of Precambrian Franklin Marble.

STOP 4. Hardyston - Precambrian Unconformity and Stissing Dolomite.
(Franklin, N.J., 7 1/2 - minute Quadrangle.)
Walk east from Wildcat Road toward golf course just south of point where wooded ridge intersects road obliquely. Walk northeast along east base of ridge facing golf course about 25 feet to first outcrops. Here Lower Cambrian Hardyston Formation rests on light colored Precambrian gneiss. The Hardyston dips 550 NW. The basal five feet or so of the Hardyston contains pebbles of quartz and fresh feldspar up to an inch in diameter. About 20% of the pebbles are feldspar. PLEASE DO NOT HAMMER ON THIS OUTCROP. Exposures of the Cambrian - Precambrian unconformity are rare and should be preserved as an exhibit for students.
The type locality for the Hardyston is 2 miles to the northeast at Hardystonville along this sarrie continuous outcrop belt. The Hardyston here is in one-foot beds that are internally cross-bedded in smaller units. The five feet or so of conglomerate grades upward into dark-gray, flaggy, quartz-sandy dolomite that underlies most of the ridge and totals about 100 feet in thickness. The dark-gray dolomite may represent the Lower Cambrian Stissing Dolomite.
Climb over the ridge across strike to Wildcat Road and walk north along the road past a covered swale to the next outcrops. These may be the base of the Upper Cambrian Pine Plains Formation. The light-weathering dolomite is interbedded with thin, ripple-marked beds of quartz-sandstone. Oscillation and interference ripples are beautifully displayed both on bedding surfaces and in cross-section. An extensive section of higher carbonate beds is exposed along the road for several hundred feet.
The base of the Hardyston represents a shore, but not a shore of Appalachia. The Early Cambrian sea transgressed westward onto the craton. The importance of this outcrop is to show that the Precambrian which was exposed at the surface at Newfoundland, during the Silurian, is still covered by the Cambrian at Franklin, only 10 miles to the west.

STOP 5. Gould Quarry. Unconformity of Silurian on Cambrian.
Although here called STOP 5, because of the addendum, it was originally called STOP 4A.
(If time permits.)
(Newfoundland, N.J., 7 1/2 minute Quadrangle.)
Walk west into woods following old dirt road to abandoned . and overgrown Gould limestone quarry. The first exposures are of Precambrian gneiss. A few feet of covered interval are succeeded by ledges of Hardyston Sandstone outcropping on the east side of a low ridge. The Hardyston dips steeply northwest and grades upward from a few feet of pebbly quartzite to a quartz-sandy dolomite, that fonus the top of the ridge. Walcott (1893) found 01enellus in this dolomite a mile or so to the north, and it is presumably the equivalent of the Lower Cambrian Stissing Dolomite of New York. Just over the crest of this ridge, on its western slope, and about 60 feet stratigraphically above the Hardyston QuartZite, the dolomite is succeeded abruptly by a coarse quartz-pebble conglomerate that rests on the irregular upper surface of the dolomite and includes clasts of dolomite just above the contact. This coarse conglomerate appears to be the base of the Green Pond Formation, for it is exposed intermittently from this point westward, across a narrow valley to the main mass of the. formation in Kanouse Mountain. The upper surface of the dolomite, on which the Green Pond rests, is a karstlc surface, for pockets of the same conglomerate appear in the basal part of the dolomite, on the east side of the ridge toward the south end of the old quarry, not far above the Hardyston Quartzite. Kfunmel and Weller (1902" po 7) were apparently the first to interpret these pockets as solution cavities filled from above. The pockets are lined with a thin layer of shaly sediment between the dolomite and the conglomerate. These solution fissures extended some 30 feet below the pre-Silurian surface.
This locality is about three miles north of STOP 3 where the Green Pond rested directly on the Precambrian. The Cambrian first appears beneath the Silurian a half-mile south of here at the north end of Echo Lake. The obvious unconformity here, barely 70 feet above the base of the Cambrian, is the strongest evidence for the unconformable nature of the less well exposed Silurian-Precambrian contact to the south~ We are here on the northerly flank of the pre-Silurian uplift.
Dr. Barnett has discovered Ordovician shales on the west side of the outlier northwest of Bowling Green Mountain. Inasmuch as the Silurian rests directly on the Precambrian at Bowling Green Mountain, the northern limit of the exposed Precambrian lay just north of there. A line connecting that point with the corresponding contact at the north end of Echo Lake should be parallel to the axis of the pre-Silurian uplift. It has an ENE-WSW trend that is at variance with the axis of the outlier, though one that corresponds with late folds in the New York City group in Westchester County (see Trips A and H as well as Fisher et al., 1961.) This m~ be a late Taconian fold direction. I~ also parallel with the Cambrian-PreCambrian contact on either side of the outlier south of Monroe (see Figures 1 and 2.) Unfortunately the Silurian is faulted out of the outlier at that point so that the trend cannot be demonstrated to be pre-Silurian there.

Outcrop of Cornwall (Pequannock) Shale (Middle Devonian).
Outcrop of Cornwall (Pequannock) Shale (Middle Devonian). The road follows the strike of the Upper Silurian-Lower Devonian. On the right is the ridge of Green Pond Conglomerate, on the left the ridge of Bellvale Sandstone.
This comment was on the original trip before the new stop was added. Hence the route no longer comes this way...

Greenwood Lake
To the right is Greenwood Lake. Beyond it to the east are hills of Precambrian forming the east boundary of the outlier. The Green Pond has been faulted out. To the left are nearly continuous outcrops of the lower beds of the Bellvale Sandstone (or the upper part of the Cornwall shale). The ridge to the left (west) is Bellvale Mountain, the type locality of the Bellvale Sandstone.

Woodbury Falls
Woodbury Falls, where railroad trestle crosses road. Marine beds of Bellvale sandstone in bed of Woodbury Creek on right, non-marine beds on left (west) side of road.

Precambrian hill on left (north) and Siluro-Devonian hill on right.

STOP 6. North end of Pine Hill. Green Pond Formation.
Although here called STOP 6, because of the addendum, it was originally called STOP 5.
(Popolopen Lake, N. Y., 7 1/2 - minute Quadrangle.)
Outcrops near the road, at turn-off of private dirt road, are of Lower Conglomerate Member, dipping steeply northwest. The pebbles are almost entirely milky-quartz.
Walk into the woods across strike. About 100 feet NNW are outcrops of the Middle Arkose Member. Fresh, angular, cleavage fragments of feldspar, up to 1/2 inch across, are common along with quartz pebbles in a fine reddish matrix. This unit can be recognized 2 1/2 miles to the southwest along strike near Highland Mills (Figure 4 and Table 1).
Continue 200 feet or so further northwest to the base of ledges that expose the Upper Quartzite Member. (Some care should be exercised to avoid Copperheads in climbing over these ledges.)
Beyond this the Longwood is poorly exposed on the top of the ridg3. We will see a better section at the next stop.
Return to the road.

STOP 7. South end of Pine Hill.
Although here called STOP 7, because of the addendum, it was originally called STOP 6.
Green Pond - Longwood - Decker Ferry. (Popolopen Lake, N. Y., 7 1/2 - minute Quadrangle.)
Walk north along Skyline Drive from intersection with Pine Hill Road. The first outcrops on the right (east) side of road are of the Upper Quartzite Member of the Green Pond, with characteristic Liesegang rings of hematite, and quartz-filled fractures.
Farther on the Lower Arkose Member of the Longwood is exposed in poor outcrops. If time permits, climb the hill to the well-exposed ledges on top of the ridge. The lower part of the measured section (Figure 4 and Table 1) was made here, from the Lower Arkose Member of the Longwood down to the Middle Arkose Member of the Green Pond; the section in the Green Pond was measured with several jogs northeastward along strike to preserve continuity of section. The intergrading contact of the Green Pond and Longwood is well exposed here. Do not go further up-section (northwest) than the lower beds of the Lower Arkose Member of the Longwood: the ground slopes downward to the unprotected edge of a sheer 100-foot cliff that drops vertically into the shale quarry to the northwest. STAY AWAY FROM THE EDGE OF THE CLIFF!
Continue north on Skyline Drive to the entrance to the shale quarry and turn right into the quarry. steeply northwest-dipping bedding planes of the Upper Shale Member of the Longwood form the southeast wall of the quarry, higher beds being exposed stepwise toward the north. A zone of contorted bedding is exposed just above the first large bedding plane. Mud-cracks and curious spheroidal pits one to six inches in diameter, are common on some of the higher bedding planes.
The remainder of the section was measured at the northeast end of the quarry, where the Decker Ferry Formation is exposed, separated from the highest beds of the Longwood by a 40-foot interval covered with red shale debris. Some of the Decker Ferry is covered by a few inches of soil, but can be exposed by digging with the hammer. The beds seem to be in place and were measured inch-by-inch with a tape. Most of the formation consists of interbedded quartz-sandstone and dolomite. Quartz-sandstone predominates in the lower beds and this part is here called informally the "Binnewater" Member because it is homotaxial with the type Binnewater of the High Falls area, 40 miles to the north. A prominent outcrop (Unit R) of this lower part of the Decker Ferry is exposed half-way up the slope at the northeast end of the quarry, to the right of a grassy embankment.
Higher in the section thinly laminated (stromatolitic?) mud-cracked, somewhat argillaceous dolomites predominate, with minor quartzsandstone interbeds. Intraclasts are common. This part of the formation is designated informally as the "Waterlime" Member. It resembles lithologically the waterlimes of the Rondout Valley which lie above the Binnewater Sandstone at its type locality. Outcrops may be seen lower on the slope and towards the northwest.
The continuous alternation of the two rock types, sandstone and dolomite, with mud-cracks in the dolomite often being filled with quartz-sandstone, suggests that the two types of sediment were being deposited contemporaneously in adjacent, spatially shifting areas, perhaps sandy beach and tidal mud-flat. (Southard, 1960, mapped the "Binnewater" and "Waterlime" units together as his sandy-claystone unit, emphasizing their continuity. )
The highest beds of the Decker Ferry are lithologically quite distinct, though sandstone & dolomite interbeds indicate their relationship to the underlying units. This unit is separated as the Skyline Calcarenite Member of the Decker Ferry Formation (new name). It includes all the calcarenite beds exposed in the quarry, its type section (see measured section, Table I). Minor interbeds of sandstone and dolomite are present. The principal lithology is a red to blue-gray coarse crinoidal clastic limestone, full of whole shells (see faunal list), cross-bedded, and heavily charged with hematite, which frequently partially replaces some of the fossils. The fauna has not been completely studied but the following have been tentatively recognized:
Bryozoa:
Ptilodictya sp. cf. P. frondosa Weller
massive trepostome, cf. Monotrypa corrugata Weller
Brachiopoda:
Atrypa "reticularis"
rhynchonellid, cf. Camarotoechia sp.
Coelenterata:
Favosites sp.
horn coral
Arthropoda:
ostracode, cf. Dilbolbina sp.
Echinodermata:
pelmatozoan (Probably crinoid) columnals
This fauna is hardly diagnostic of age, but is consistent with the Decker Ferry of New Jersey (Weller, 1903). Neither the fauna nor the lithology are anything like either the Wilbur Limestone or the Glasco Limestone, which fall into this part of the section in the Rondout Valley. Neither is it like any of the higher limestones of the Helderberg Groupo The Becraft is the closest lithologically, and probably environmentally, but the fauna is certainly not the same. This appears to represent a shallow-water shell-bank environment. The name of the member is derived from the nearby Skyline Road.
Thicknesses of the members recorded in this section are as follows:
| Feet | Inches
Decker Ferry Formation | |
Sky line Member | 7 | 8
"Waterlime" Member | 28 | 9
"Binnewater" Member | 22 plus |
Longwood Formation | |
Upper Shale Member | 88 | 2
Lower Arkose Member | 80 |
Green Pond Formation | |
Upper Quartzite Member | 222 | 10
Middle Arkose Member | 82 plus |
Walk back out of the quarry, south on Skyline Road and west on Pine Hill Road. At the bridge over the Thruway one can see the Lower Arkose Member of the Longwood exposed north of the east abutment. On the west side of the Thruway, the first visible outcrop is that of the Connelly Conglomerate. When the writer first visited this cut in 1954, just after it had been partly blasted through, a white-to-violet-mottled, friable, clayey, fine sandstone, with characteristic thin inter laminae of dark-gray shale crumpled to give the rock a "zebra-stripe" appearance, was exposed to, the south of the Connelly. It has since been grassed over. Boucot (1959) named this unit the Central Valley Sandstone, and this is its type locality. North of the Connelly, on both sides of the Thruway, is a nearly complete section of the Onesquethawan Series. Access to the Thruway cut is prohibited and the prohibition strictly enforced by State Police.
Continue west on Pine Hill Road to the first black-top road on the right and walk up this road to its dead end.
STOP 6-B. Connelly Conglomerate.
Low ledges on the east side of the road expose the rather well-sorted quartz-pebble conglomerate (2 to 6 mm clasts) of the Connelly. Oriskany fossils establish its age. It is equivalent to an argillaceous limestone 25 miles to the west and to a similar conglomerate followed by an argillaceous limestone 40 miles to the north. This represents a shoreline facies, a pebbly beach on the temporarily stable shore of Appalachia. Most of the fines have been winnowed out.
It may be possible to find Central Valley float on the ground to the south.
Walk back to Pine Hill Road and turn right. At the bend in the road is a stone fence made of Connelly boulders, resting on small outcrops of the Connelly. Where road bends sharply to the left, turn right on private road, then take short path down to railroad tracks opposite abandoned station. Turn right and walk to first outcrops on east side of tracks.
STOP 6-C. Highland Mills. Highland Mills Sandstone and "Middle Member" of the Esopus Formation. (Popolopen Lake 7 1/2 - minute Quadrangle. )
WATCH OUT AND LISTEN FOR TRAINS. DO NOT SIT ON TRACK OR PLACE OBJECTS ON TRACK. TRAINS COME THROUGH FAST AND WITHOUT WARNING. If a train comes stand well back; there is plenty of room on either side of the track.
This stop demonstrates near-shore and off-shore deposits under conditions of strong influx of terrigenous clastics. The series of beds at the south end of the cut are of the upper part of the Highland Mills Sandstone of Boucot (1959). These light-blue-gray, light-brown-weathering, subgraywackes are dominated by evidences of shallow-water deposition. A prominent set of bedding planes display oscillation ripples of various sizes. The ripples tend to be uniformly oriented, roughly NNW - SSE when rotated back to horizontal. (The beds here strike N 500 E and dip 600 NW.) Just north of the ripple-marked layers are lenses of closely packed, jumbled, disarticulated shells. The lenses pinch out within a few feet, from thicknesses of a foot or so. (Preservation on the weathered surfaces is in the form of molds; the most common fossil is Leptocoelia flabellites, but besides the many other brachiopods described by Boucot (1959) there occur gastropods, pelecypods, horn corals, trilobites and other fossils.) Associated with the shell-lenses are shaly beds packed with the ichnofossil Phycodes. All these features are characteristic of the Cruziana-facies of Seilacher (1964) representing shallow-water above wave-base, littoral or sub-littoral.
The "Middle Member" on the other hand, exposed farther north along the tracks, represents Seilacher's deeper-water, sublittoral to bathyal Zoophycos-facies. Bedding planes are covered with the ichnofossil Zoophycos (= Taonurus, = Spirophyton). The rock is massive-bedded and the bedding planes very even. (The rock weathers brown to orange, the fresh rock is almost black.) Although described in the literature as a mudstone, most beds are poorly-sorted graywacke sandstone with about 55% to 85% quartz-grains of fine-sand size, and the rest chiefly finegrained matrix (data from Miss Janice Lumnitz and Mr. Maury Morgenstein). Fossils are sparsely scattered on the bedding surfaces, mainly the brachiopods Leptocoelia flabellites and Spirifer macra. On many bedding-planes concave-up valves outnumber concave-down valves (from Miss Janice Lumnitz) suggesting settling-out through water followed by rapid burial without further reworking. The unsorted nature of the sediment also points to rapid sedimentation and the sparseness of fossils suggests dilution by rapid influx of terrigenous material.
Feldspar may be less abundant here than in the underlying Highland Mills Member, but the whole Esopus sequence is strongly suggestive of a pulse of erosion of the source area (Appalachia).
The Esopus sequence starts with deep-water Zoophycos-bearing beds (the Mountainville Member of Southard, 1960). The upper part of the Highland Mills Member (restricted Highland Mills Member of Southard) is mostly shallow-water. The "Middle Member" is· again mostly deeperwater. The Woodbury Creek Sandstone appears to be mostly shallower water again. It is more fossiliferous than the "Middle Member" (dominated by the pelecypod Cypricardinia and the brachiopod Schuchertella). The fossils are evenly spread on the bedding planes, rather than in lenses as in the Highland Mills Member, and ripple marks are not well-developed. Also Zoophycos has been observed on some beds. It would thus seem to be of a depth intermediate between that of the Highland Mills Member and that of the "Middle Member".
The succeeding Kanouse Sandstone, a clean, somewhat pebbly, orthoquartzite, again marks a stable shoreline deposit, with a falling off of terrigenous influx permitting better sorting of the material. It appears to be the shoreward equivalent of limy deposits to the north and west (Schoharie and/or Onondaga).

STOP 8. Monroe. Bellvale Formation.
Although here called STOP 8, because of the addendum, it was originally called STOP 7.
(Monroe, N. Y., 7 1/2 - minute Quadrangle.)
Between here and the Monroe-Washingtonville exit are exposed about 2000 feet of the Bellvale Formation, essentially a complete section. Details of the section are given in the measured section, Table II and Figure 5.
The lowest beds at the east end of the outcrop are shaly siltstones that are close to the base of the Bellvale, if indeed they are not to be considered the highest beds of the underlying Cornwall Shale. The beds immediately above are graywackes that carry Mucrospirifer and Spinocyrtia, thereby demonstrating their Hamilton age and marine nature. A small Chonetes is also common. This entire lower part of the section here is identical, lithologically and faunally, to the section exposed in the bed of Woodbury Creek, at Woodbury Falls, north of Highland Mills, where the railroad trestle crosses Route 32.
As one goes up-section, intercalated beds of uncleaved sandstone increase in thickness and ultimately dominate the section by the time one reaches the abutment of the overpass. Up to here the beds are evenly laminated without any indication of large scale cross-bedding or channeling.
Just at the east side of the overpass is a zone of ball and pillow structures and load-casts. These structures are widely recognized in the Catskill Delta rocks as marking the transition-zone from marine to non-marine beds. The beds beneath the overpass are still marine, however, as brachiopods have been found in them. Nevertheless, the nature of the bedding changes from the preceding even lamination, to evidence of channeling, cut-and-fill structure, and cross-bedding. The rock becomes lighter and coarser, a subgraywacke. Load-casts are present intermittently, and at least one zone of pebbles scattered in subgraywacke is present. It would appear that we have passed from the evenly laminated prodelta and foreset beds to channeled 3l1d irregular top set beds.
West of the overpass the subgraywacke becomes still coarser and lighter. Thin interbeds of shale become more common and numerous shale chips appear in the sandstones. Many of the smaller grains appear to be shale clasts or perhaps phyllite. Obscure plant remains and possible wood-fragments appear. No marine fossils have been found, and these deposits may have been made on the subaerial part of the delta.
Beyond the culvert the rock becomes even coarser and more lithic. Here unmistakable plant fragments are present including pieces of branches of scale-trees or related lycopsids a half-inch or so in diameter and clearly shoWing the leaf scars and internal woody fibers. (The first such were found by Mr. Harvey Zeiss; I have since found others.) Note the well-developed glacial striae and chatter-marks on some of the outcrop surfaces.
Beyond this point is a long succession of massively cross-bedded subgraywacke sandstones with shale interbeds. There are also four prominent units of highly cleaved mudstone, decreasing in thickness from 31 feet for the first such unit, to 11 feet for the last. These are probably flood -plain muds. The last of these units is clearly channeled and filled by the succeeding sand , probably a stream-channel deposit.
The Bellvale section ends with coarse pebble beds at the center of the syncline, just at the Monroe-Washingtonville exit. These beds have the character of the overlying Skunnemunk Formation, except that they lack the red color characteristic of that formation. The pebbles include besides milky-quartz, rocks such as chert, quartzite and shale or slate, not too unlike the pebbles included in the base of the Green Pond at STOP 3. We are probably dealing here with Piedmont alluvial deposits.

Return to the hotel
Return to the hotel via Route 17, New York State Thruway, Major Deegan Expressway, etc.

F: THE PLEISTOCENE GEOLOGY OF THE MONTAUK PENINSULA
By Walter S. Newman, David L. Thurber, David H. Krinsley,
Queens College of the City University of New York;
and Leslie A. Sirkin, Adelphi University.
Long Island is a long narrow island reaching east-northeastward from New York City to form a "fish-like" extension of New York State. The island lies south of and is approximately parallel to the Connecticut shore of New England and is separated from it by Long Island Sound. Long Island forms the north shore of an Atlantic Ocean reentrant known as the "New York Bight". Although part of the Coastal Plain Physiographic Province, Long Island features a topography almost completely modified by glacial and proglacial processes. Two conspicuous end moraines extend from west to east along the axis of the island. The older Ronkonkoma moraine, probably Wisconsin in age, makes up a major portion of the Montauk Peninsula. The younger Harbor Hill moraine generally follows close to the north shore of Long Island east to Orient Point. The island abounds in other glacial and proglacial features such as the coalescing outwash fans and aprons which form much of the southern portion of the island.

F: THE PLEISTOCENE GEOLOGY OF THE MONTAUK PENINSULA

Flushing Meadow
Flushing Meadow-the site of the two New York World's Fairs. The geology of this swale has been described by Newman (1966).

Queens College
To your right (south) the campus of Queens College of the City University of New York.

Alley Creek Valley
A drowned and then partially filled embayment of Long Island Sound.

Lake Success on your right
The lake has an area of 60 acres, a maximum depth of 72 feet, no surface outlet, and is one of the larger kettles on Long Island. Note the (both) Ronkonkoma and Harbor Hill morainal topography.

Descend from Ronkonkoma moraine
Plainview(!)-Here we descend for a short distance from the Ronkonkoma moraine onto the outwash plain. Note the relief contrast.

Descend to the Huntington Plain
After crossing West Hills, one of several central Long Island areas where pre-Pleistocene strata rise considerably above sea level and approach the surface, we descend to the Huntington Plain which may be the site of a proglacial lake overlain by a thin veneer of outwash (Lubke, 1964).

Half Hollow and Dix Hills
We rise again into the Half Hollow and Dix Hills, areas similar in structure to West Hills. The Ronkonkoma End Moraine lies on the north flanks of these hills.

Outwash plain then Ronkonkoma moraine
Sunken Meadow-Sagtikos State Parkways. Here we descend once again for a short time onto the outwash plain. Pilgrim State Hospital forms the large building complex on the right (south). We then once again mount the Ronkonkoma moraine.

Descend from Ronkonkoma Moraine to outwash plain
We descend almost immediately from the Ronkonkoma Moraine onto the outwash plain. Note the distinctive "pine barrens" vegetation of scrub-oak and pine. This area is underlain by a podzol soil having a bleached lower "A" horizon. This area of Long Island is devoid of agricultural potential because the outwash lacks the loess cover which is conspicuous in farming areas on outwash further east.

Continue east through "pine barrens" on outwash plain.

Eastport: temporary terminus of Sunrise Highway.
Northeast on Route 51. Note farming activity on outwash plain. The surficial loess makes the difference! Route 51 climbs onto the Ronkonkoma moraine and then descends towards Riverhead and the pitted outwash plain between the Ronkonkoma and Harbor Hill End Moraines.

Riverhead: at the Peconic River mouth.

Reeves Bay on left (north).

Cross Shinnecock Canal. We mount the Ronkonkoma Moraine once again.

Bluff Road
Bluff Road marks the crest of an abandoned wave-cut marine cliff cut into Ronkonkoma outwash. Progradation due to the construction of the Napeague Tombolo has separated the bluff from the sea for distances of up to 1.5 miles.

Descend from bluff
We descend from the bluff, now on our left onto the Napeague beach-and-dune-complex Tombolo.

Abandoned wave-cut bluff on left
Note the abandoned wave-cut bluff on left as well as the dunes on glacial drift. Drive half-left onto the New Montauk Highway mounting the Ronkonkoma Moraine at Hither Hills.

The village of Montauk built, for the most part, on a double tombolo.

STOP 1. Montauk Point State Park, Montauk Point.
45 minutes. REST ROOMS ARE IMMEDIATELY ADJACENT TO THE PARKING LOT ENTRANCE. Montauk Lighthouse was built in the years 1795-1797 about 300 feet from mean high water. It is now only about 60 feet from the water's edge. Following the field trip leaders, walk southeast crossing the road (WATCH OUT FOR TRAFFIC!) and follow the trail which commences at the lighthouse reservation entrance and skirts the south boundary down to the water's edge. To your left, towards the lighthouse is the section sketched by Fuller (1914, fig. 159, p. 144) which probably includes the type Montauk Till section. Starting from the base, Fuller identified the units in the bluff as "(a) Till phase of Montauk till member; (b) boulder pocket; (c) sand and clay phase of Montauk member; (d) clayey sand phase of Hempstead gravel member; (e) normal sandy phase of Hempstead gravel member". We interpret this section as consisting of Ronkonkoma (=Montauk) Till; a lag concentrate; laminated, probably lacustrine, silt, sand and clay; grading upwards into eolian silt and sand. Over towards the northeast, the section includes some stratified drift. The laminated unit appears to occupy a swale (kettle?) in the till. Listen (sic!) to the geomorphology and sedimentology. Returning to the busses, climb the bluff and look southwest. The bluffs are usually fringed by steep shingle-beaches and extend four miles southwestward to Ditch Plains.

Montauk Air Force Station.
Stop! We are now under military jurisdiction and supervision. Proceed under Air Force direction to south shore.

STOP 2. South Shore Beach
1 hour. Leave the buses and enter upon the south shore beach. Immediately to the west is a mass of laminated silt and fine sand which Fuller considered "possibly" Gardiners. We believe this unit represents a proglacial lacustrine deposit. Walk southwest for 0.5 mile. Here we find the exciting section described by Perlmutter and DeLuca (1963). The major unit is the Montauk Till forming a 0.5 mile long open anticline. The Montauk Till overlies stratified drift consisting of interbedded gray and brown clay, laminated green and gray silt and clay, and some thin lenses of fine brown sand. Perlmutter and DeLuca found neither forams nor diatoms in the lower stratified drift which represents the oldest unit we will view on this trip. Immediately above the Montauk Till is stratified drift which ranges in thickness from a featheredge to about 30 feet and is composed chiefly of beds and lenses of brown and gray silt, fine to medium sand, and clayey sand. We interpret this unit as likely to be proglacial lacustrine in origin. Perlmutter and DeLuca report 5 to 20-foot-thick till unit on top of the upper stratified drift. However, Newman fails to note it. Occasional pockets of loess cap the section.

Note the morainal topography and surface erratics on right.

STOP 3. Montauk Airport Archeological Site.
30 minutes.
Geologically, this site includes a medley of till and ice-contact deposits including lenses of red-brown clay, silt and fine sand which Fuller would have referred to as Gardiners Clay. Overlying the drift is a lag concentrate, including occasional ventifacts, while the entire section is capped by loess. Pelecypod valves, including Crassostrea virginica, Venus mercenaria and Pecten irradians, form a "shell midden" associated with the upper portion of the loess blanket. The absence of artifacts suggests the midden dates from the "Archaic Stage" of aboriginal development and is thus some 4000 to 6000 years old. These aborigines probably harvested the lagoon or bay that existed immediately to the north of the site which has since been filled by the tidal marsh sere and then covered with sand dunes.
LUNCH STOP! Perhaps. It depends upon the wind direction. If conditions are unfavorable here, we'll eat at STOP 4.

STOP 4. Ditch Plains Stratigraphic Section.
45 minutes.
Enter upon the beach and walk west 0.2 mile. At this point, the bluff presents a rather simple section consisting of the Montauk Till, a lag concentrate, with loess on top. However, further to the east, additional units are found beneath the loess. These new units of stratified drift appear to have an easterly dip component. At the east edge of the bluff, accentuated by a morphological reentrant at the back of the beach, the stratified drift clearly takes on the aspect of a delta built into a standing body of water. However, this critical exposure is frequently obscured by slump from the still younger unit, aeolian sand comprising dunes, found above the loess. At about this point, the Montauk Till surface dips below the beach and two additional units are found which outcrop near the upper edge of the beach. The lower unit is composed of laminated silt, clay and fine sand. The upper unit is a peat. Both of these units can be traced for about 0.4 mile towards the east although occasionally interrupted by drift, mostly till, cropping out at beach level. Still further towards the east, the bluffs, composed for the most part of Montauk Till, reappear.
Rooted stumps are occasionally found on the peat layer. About a mile to the northeast, adjacent to East Lake Drive and Montauk Harbor, the U. S. Geological Survey notes 98 feet of clay commencing at elevation 0 (Well S010041). The evidence so far developed suggests the entire Montauk Harbor swale was at one time a lake basin. A pollen section from the beach exposure worked up by Maurice Kalisky, one of our graduate students, indicates the sampled section straddles the B (pine) and C-1 (oak-hemlock) Pollen Zones. In this and other aspects, this pollen section resembles that of Donner's (1964) site 2 section from a bluff 0.3 mile west-northwest of Montauk Point. Apparently, a proglacial lake developed a bog sere in postglacial times which was terminated by the Flandrian transgression. The rise in sea level breached the basin rim and littoral and aeolian sand encroached upon portions of the original basin.

Fort Pond
Fort Pond on your left is dammed on both its north and south side by tombolos.

Montauk Station: eastern terminus of the Long Island Railroad.

STOP 5. Ice contact kame
30 minutes.
This excavation illustrates the internal structure of a morphologically well-defined ice-contact kame. Till is exposed at the north side of the pit while a lag concentrate and loess overlie the glacial drift.

STOP 6. Montauk Sanitary Landfill Project
Both the topographic maps and aerial photographs (see Plate 1) of the Hither Hills area feature several dozen northeast striking ridges. Fuller (1914, p.48), referring to the swales between these ridges, called them "inner-fosse channels". He considered them to be erosion channels which were outlets for waters issuing from the ice margin at successive halts and escaping parallel to the ice front. The structure of the stratified drift exposed in this excavation, however, suggests these ridges are ice-thrust moraines. On the west side of the excavation access road, coarser stratified drift, a lag concentrate, and loess are exposed.

View of the Ronkonkoma moraine
In clear weather, the view towards the west gives an excellent view of the Ronkonkoma moraine as well as many grosser shoreline features.

Wave cut bluff and migrating dunes
Continuing west along Route 27, note the wave-cut bluff to your right (north) now isolated from the sea by a prograding shore. The bluff section consists of stratified drift overlain by dune sand now cascading down onto the Long Island Railroad right-of-way. These dunes appear to have migrated in from the north shore.

STOP 7. "Walking Dune".
At the terminus of the paved road, follow path to top of "Walking Dune".
These magnificent parabolic dunes are the present result of a series of morphological developments. Initially, a spit was built westward out from the north shore of Hither Hills. Foredunes were then built behind the beach associated with the spit. Meanwhile, a tidal marsh sere developed in the lagoon behind the spit and the dunes encroached upon and, in large measure, covered the tidal marsh. An oak forest sere developed within the dune swales but were subsequently covered and still later exhumed. Note the dune slip faces currently burying the existing forest.

Crossing Napeague Meadows, a ditched tidal marsh.
UNGUARDED RAILROAD CROSSING-CAREFUL!

Roadcut through Promised Land Chenier.

Chenier on left (south).
Promised Land fish-rendering plant on right; chenier on left (south). The road parallels the chenier for 1. 5 miles.

The chenier ties into the Ronkonkoma Moraine
The chenier ties into the Ronkonkoma Moraine at the east end of the wave-cut bluff marked by Bluff Road. Presumably, the chenier marks the location of a former spit built eastward at the time the sea was eroding along the line of bluff road.

Wave cut cliff
Bluff Road follows the crest of a wave-cut cliff cut into outwash. Some might suggest that the flat below the bluff represents a mid-Holocene three-meter terrace in the sense of Fairbridge. However, it is more likely that the flat is due to prograding Atlantic shore in this vicinity. The present shore cuts the bluff out at Easthampton village.

STOP 8. Bluff Road.
Plate 2 depicts the morphological relationships of the locality. Time permitting, we will walk the 0.4 mile to the Atlantic shore beach.

G: STRUCTURE AND PETROLOGY OF PELHAM BAY PARK
By Carl K. Seyfert, Department of Geology, Buffalo State University College,
and David J. Leveson, Department of Geology, Brooklyn College.
Location and Geologic Setting.
Pelham Bay Park is located on Long Island Sound in The Bronx in New York City (Figure 1). The area mapped in detail (Scale 1 inch = 10 feet) includes North Twin and South Twin Islands which are located in the eastern part of Pelham Bay Park (Figure 2). Both North Twin and South Twin Islands are underlain by highly deformed and intensely metamorphosed gneisses, schists and amphibolites which have undergone a complex tectonic and metamorphic history involving extensive boudinage, tight isoclinal folding and metasomatism. Pleistocene glaciation and recent wave action provide excellent exposure of bedrock and permit detailed field study of these rocks. The units of Pelham Bay Park were mapped as Hudson Schist (now Manhattan Formation) in the New York City Folio (Merrill et al., 1902). However, on the New York State geological map (Fisher et al., 1961), the rocks are deSignated as undivided schists and gneisses of unknown age.
Acknowledgments.
The authors wish to thank Professor Kurt Lowe of the College of the City of New York who first introduced them to this area, and the late Professor Arie Poldervaart of Columbia University who provided early encouragement and funds for initial thin sections. Thanks are also due the Society of the Sigma Xi for a Grant-in-Aid of Research that permitted continuing investigation, and the Department of Parks of the City of New York for their courtesy and cooperation.

G: STRUCTURE AND PETROLOGY OF PELHAM BAY PARK

STOP 1. Orchard Beach Park (STOPS 1 - 11)
Turn left and follow the road to the parking lot for Orchard Beach and park in the northeastern corner of the lot.
Distance Between Points.
Take the path which leads to the beach and follow the path along the beach to the northeastern end of the beach. The first stop is on the outcrop just east of the Breakwater on the southern end of South Twin Island (Plate 1).
2400'   STOP 1. The rocks here include felsic gneiss, sillimanite schist, and amphibolite. Note the rootless fold in an amphibolite at the north end of the outcrop (STOP I-A. see Plate 1)0 This amphibolite continues along strike into mafic biotite schist on the west limb of the fold. The west limb of the fold was stretched and thinned during the third phase of deformation. A plagioclase-quartz border is present on the amphibolite near the trough of this synclinal fold.
The amphibolites on the eastern side of the outcrop pinch and swell along strike. Note the presence of pegmatite (Table 1, number IS) replacing the amphibolite and mafic biotite schist (Table 1, number 10) in a thin amphibolite layer which has been separat ed by boudinage (STOP I-B). Mineralogy of the pegmatite: plagioclase, quartz and biotite.
The amphibolite in the center of the thicker amphibolite layer (STOP I-C) contains little biotite (Table 1, number 6), but biotite increases in abundance toward the contact of the amphibolite (Table 1, number 9) with felsic gneiss.
Isoclinal folds can be seen at the south end of the outcrop (STOP l-C, see Plate 1) especially at low tide. The axial planes of these folds strike N200 E and dip SOOE. Fold axes have an average bearing of N440 E and plunge of 620 NE.
Where folding during the third phase of deformation was particularly intense (STOP I-D), biotite within sillimanite schists was rotated parallel to the axial planes (S3) of the latest set of folds (F3)'
Proceed northeastward along the shoreline.
300'   STOP 2. Rootless fold in amphibolite (See Plate 1). A Plagioclasequartz border (Table 1, number 11) is present at the ends of the amphibolite which have been separated by boudinage. Near the contact with the plagioclase-quartz border, the amphibolite contains diopside, epidote, calcite and scapolite.
Continue northward along the shoreline.
100'   STOP 3. Small normal fault (Plate 1). Slickensides on the fault plane at the western end of the outcrop indicate that the motion was dominantly dip-slip. Erosion of breccia along the fault has produced a small "rift".
Continue north along the western side of the outcrop.
50'   STOP 4. Pegmatite replacing amphibolite. Note the very irregular, gradational contacts. Mineralogy: plagioclase, quartz and biotite. Continue northeastward along shoreline.
100'   STOP 5. En echelon amphibolite layers suggesting the amphibolites were originally dikes or sills. Note replacement pegmatite in the amphibolite.
Proceed northward along shoreline.
200'   STOP 6. Injection pegmatite dike. Walls are generally sharp, but local assimilation of the felsic gneiss has caused some irregular contacts. Mineralogy: microcline, quartz, plagioclase, with minor tourmaline (black), garnet and apatite.
Note large eratics and glacial striations on bedrock.
75'    Another injection pegmatite (STOP 7 -A). Note straight, parallel walls. Layers of sillimanite schist are offset indicating dilation of the wall rocks during emplacement of pegmatite. Contacts are very sharp and muscovite crystals near the contacts tend to be oriented normal to the walls of the dike. This pegmatite almost certainly crystallized from a granitic melt.
Proceed eastward along the shoreline.
225'   STOP 7. Thick amphibolite layer with calcite-diopside-scapolite pods. This mineralogy is similar to that of the diopside-epidote amphibolites of North Twin Island. Cross the tombolo (which may be covered at high tide except for stepping stones) which connects North Twin Island with South Twin Island (Plate I), Continue to large fold just east of the center of the island.
400'   STOP 8. Folded diopside-epidote amphibolite, plagioclase-rich layers (Table 1, number 15), and calcite-rich layers (Table 1, number 16). Folding is somewhat disharmonic within the calcite-rich and plagioclase-rich layers. These layers grade along strike into diopside-epidote amphibolite on the limbs of the fold (Figure 4). Changes in mineral assemblages going from diopside-epidote amphibolite on the limbs of the fold to plagioclase-rich layers along strike at the crest of the fold are:
(a) hornblende-plagioclase with minor pyroxene, scapolite, epidote and calcite;
(b) plagioclase-hornblende-epidote with minor quartz and pyroxene; and
(c) plagioclase with minor quartz and magnetite.
The plunge of the fold is to the south, indicating that it is an antiform (up-arched foliation surface). However, along strike to the north on both limbs of the fold, the plunge of the folds changes to vertical and then to plunging northward. Thus, there are two antiforms along the continuation of the amphibolite layer, with no intervening synform. Sl foliation has been folded about the antiforms.
Just east of the fold, there are several plagioclase-biotite gneiss layers within the diopside-epidote amphibolite (STOP 8-B). Ellipsoidal hornblende nodules occur within diopside-epidote amphibolite near the contact with plagioclase-biotite gneiss on the eastern side of North Twin Island (STOP 8-C). The nodules are 2 to 4cm. in length and 1 to 2 cm. across 'and lie in a calcite matrix. They are separated from the calcite by a 2 to 5mm. wide zone of medium-grained pyroxene and scapolite. A thin rind of epidote surrounds some scapolite grains and separates them from adjacent calcite. Intermediate axes of the ellipsoids are parallel to the foliation and long axes are parallel to mineral lineations in the surrounding mafic gneiss.
Diopside-epidote amphibolite grades along strike into normal amphibolite (STOP 8-D) suggesting that it formed by metasomatism of amphibolite.
Proceed northward.
STOP 9. Replacement Pegmatite. Plagioclase and microcline porphyroblasts are abundant within plagioclase-biotite gneiss near the contact with replacement pegmatite (Table 1, number 17). In fact, the replacement pegmatite is simply a coalesced mass of porphyroblasts. Contacts are gradational and extremely irregular.
Note the plagioclase-biotite selvage surrounding a diopside-epidote amphibolite boudin at the contact of the boudin with replacement pegmatite (STOP 9-A).
A plagioclase-epidote-quartz border is present at the end of a layer of diopside epidote amphibolite which has been separated by boudinage (STOP 9-B). This border grades abruptly along strike into amphibolite (very thin border) and then into diopside-epidote amphibolite. Relict foliation (Sl) is present in the plagioclase-epidote-quartz border. The border, which is 87% plagioclase, 5-1/2% quartz and 4% epidote, developed by metasomatism of diopside-epidote amphibolite. The composition (Table 1, number 12) is similar to that of an anorthosite.
Proceed to the northwest.
75'   STOP 10. Boudins of diopside-epidote amphibolite within plagioclasebiotite gneiss. There are several areas where diopside-epidote amphibolite can be traced along strike into plagioclase-biotite gneiss suggesting that the plagioclase-biotite gneiss was produced by metasomatism of diopside-epidote amphibolite. Steps involved are:
(a) feldspathization of diopside-epidote amphibolite;
(b) conversion to feldspathic amphibolite; and
(c) replacement of hornblende by biotite, forming plagioclasebiotite gneiss.
Calcite-rich layers and pods are present within diopside-epidote amphibolite boudins. Calcite-rich layers are also abundant at the ends of the diopside-epidote amphibolite layers which have been separated by boudinage (STOP 10-A). The zone containing calciterich layers is 25 feet wide, but it grades along strike (to the south) into diopside-epidote amphibolite containing no calcite-rich layers. This suggests that the calcite-rich layers were produced by metasomatism of diopside-epidote amphibolite.
Note the curved mineral lineations and curved fold axes within the boudins (STOP 10-B). The rotation of lineations and fold axes occurred during "necking" prior to separation of the boudins.
Return to South Twin Island and follow the western shoreline to a gravel road near the center of the western shoreline of the island.
1000'    Take gravel road westward across the bridge to Hunter Island.
900'     Turn right (north) along the east shore of Hunter Island to a small outcrop of felsic gneiss and sillimanite schist just south of a thick amphibolite layer (Figure 2).
1000'   STOP 11. Open fold. Felsic gneiss, sillimanite schist, and biotite amphibolite show evidence of 3 phases of deformation because in this area the last phase of deformation was not intense enough to obliterate signs of the earlier deformations. Biotite and amphibole crystals are oriented parallel to compositional layers within the biotite amphibolite. This foliation (S1) is probably an axial plane foliation formed during an early period of intense deformation. This foliation has been folded about a set of fold axes (L,z) which plunge steeply to the southeast. Large amphibole crystals are oriented parallel to these fold axes. A second foliation (S2) is defined by biotite crystals oriented parallel to the axial planes of the F2 folds within the felsic gneiss. Within sillimanite schist, biotite and sillimanite are oriented parallel to the axial plane (S3) of the latest set of folds. Axes of these folds plunge steeply to the northeast in this area. The relation between the folds and foliations is shown in Figure 5.
Return to the gravel road by taking path southward along the shoreline.
1000'   Take gravel road south to fork in the road.
800'     Take right hand fork and return to the parking lot. We will eat LUNCH on the tables just north of the parking lot.

H: STRATIGRAPHIC AND STRUCTURAL RELATIONS ALONG THE WESTERN BORDER OF THE CORTLANDT INTRUSIVES
Nicholas M. Ratcliffe
City College of New York
INTRODUCTION AND PURPOSE OF TRIP
The New York State Geological Association as recently as 1958 dealt specifically with the problem and areas outlined in this discussion. Recent discoveries by Hall (1965, and this volume), however, have brought the stratigraphic problems of the New York City Group much more clearly to light and have encouraged re-evaluation of the field evidence in this critical area.
The stratigraphic age and correlation of the rocks surrounding the western edge of the Cortlandt intrusives has been clouded by the personal prejudices of individual workers for many years. Because definitive evidence of a stratigraphic kind is difficult to come by in an area as complexly deformed as this, this correlation problem of regional importance is not resolved at the present time.
This trip will focus on one major problem: are the rocks called Manhattan Schist and Inwood Marble south of the Cortlandt intrusives correlative with fossiliferous rocks at Tomkins Cove and Verplanck Point? Lithic and structural arguments will be presented to support this correlation. As in all metamorphosed areas, we must rely primarily on lithic characteristics and stratigraphic succession as well as on structural continuity to solve this kind of problem. The answer is to be found in the rocks; all we must do is look for it.
The purpose of this field trip is to present new stratigraphic and structural data from the western border of the Cortlandt intrusives. This area is critical because it is the locality where correlation of Manhattan Schist and Inwood Marble with the low-rank carbonate rocks and phyllites at Tomkins Cove can best be accomplished. Bucher (1951) demonstrated the lower Paleozoic age of the Tomkins Cove section on the basis of pelmatozoan fragments in a calcareous zone at the base of the phyllite section there (STOP 7-A).
A similar fossiliferous zone rich in pelmatozoan remains has been discovered at Verplanck Point Quarry, on the east side of the Hudson River, demonstrating a Lower Paleozoic age for these rocks (Ratcliffe and Knowles, 1968) (STOP 5). A very similar "crinoidalll limestone is interbedded with the base of the type Annsville Phyllite in the Peekskill Hollow Creek at Van Cortlandtville 1-3/4 miles north of Peekskill. Identifiabie fragments of pelmatozoan columnals were found in this rock by participants in the NYSGA excursion of 1958, thus supporting the correlation of Annsyille Phyllite with the phyllites at Tomkins Cove proposed on lithic grounds by Bucher (1951). It is here suggested that the lower unit of the Manhattan formation is correlative with the combined Balmville Limestone and Annsville Phyllite and that both are Mid-Ordovician in age.

H: STRATIGRAPHIC AND STRUCTURAL RELATIONS ALONG THE WESTERN BORDER OF THE CORTLANDT INTRUSIVES

Large outcrops of Yonkers-type gneiss
Note large outcrops of Yonkers-type gneiss with large apparently folded pegmatites.

Numerous exposures of Xma
Continue north along 9A around west end of Prickly Pear Hill. Numerous exposures of Xma (Upper Manhattan, here staurolite grade). Just entering map, Figure 1.

STOP 1. Brinton Bird Sanctuary.
North flank Prickly Pear Hill, NE 1/9 Haverstraw Quad.
This stop is located on the southeast flank of the Tomkins Cove Crugers F1 anticline (Figures 1 and 3), and exposes granitic gneisses of the Fordham Gneiss in near contact with the Lower Manhattan (Oma).
Walk northeast up the path into the bird sanctuary approximately 800 feet to large glaciated exposure of Manhattan schist.
Garnet-quartz-biotite-muscovite-schist and garnet-biotite-muscovite-plagioclase-quartz granulites are the dominant lithologies. Staurolite is a diagnostic mineral in much of Unit B of the Manhattan in this area. This is typical of the Upper Manhattan exposed to the southeast on Prickly Pear Hill and resembles the type Manhattan of New York City despite the lower metamorphic grade.
Closures of F1 folds may be seen in the outcrop with the F1 axial surfaces (with bedding parallel in most cases) trending N45°-50° E and dipping steeply to the east. Late F2 folds with a related crenulation cleavage trend S75°-80°E and have near vertical axial planes and fold the F1 axial surfaces.
An F3 fold system is weakly developed in the north-central portion of the outcrop with axial planes trending S45°-50° E.
Note the several generations of quartz veins, parallel to S1, S2, and S3. S3 quartz is located in short gash-like fractures, suggesting the brittle behavior of the late F3 structure. Note the habit of the large post-kinematic metacrysts of biotite (plates are not oriented in S1, S2, or S3), S1 foliation is developed largely by the orientation of the white mica and lenticular quartz grains.
Walk north into open field to small outcrops of Lower Manhattan. Black, sooty appearance is typical of the Lower Manhattan. Minor dark siliceous layers are common.
Continue north across field noting scattered small outcrops of Lower Manhattan.
Near the edge of the field to north and by stone wall are outcrops of granitic gneiss of the Fordham. Foliation having the orientation of S1 in the schist is present in the gneiss. Compositional layering is difficult to see in the gneiss at this locality, but it commonly is not parallel to S1 (i.e., S1 is superposed on an earlier, probably Precambrian, foliation in the gneiss). There is little room here for the Inwood formation. This gneiss - Lower Manhattan contact has been mapped along the north side of Prickly Pear Hill to a point east of the lake where compositional layering in the gneiss demonstrates the anticlinal closure (see Figure 3).

Outcrops of layered gneisses of Fordham Gneiss
Overpass to Oscawanna on left (roadcut N. Y. 9) outcrops of layered gneisses of Fordham Gneiss dips are north at moderate angles. Granitic gneiss of Fordham can be seen at north end of cut. Underpass for N.Y. 9. Pass exposures on right (east) of layered norite.

Pass outcrops of Manhattan (Xmb) in woods above road.

STOP 2. Maiden Lane Sand Pit.
This stop is located on the opposite (north) limb of the major F1 fold from STOP 1 (Figure 3). Walk into the sand pit starting from the intersection of Maiden Lane and Cortlandt Street.
Layered biotite, plagioclase gneiss is exposed at corner. Foliation and compositional layering dip steeply to the north. Granitic gneiss of the Fordham is exposed in stream bed and on the hill to the south of the stream.
Enter sand pit east of house. The sand pit exposes a section that is a maximum of 50 feet thick, from Fordham Gneiss to the base of the Manhattan Formation.
Walking north into pit, one encounters the various rock units.
Biotite-plagioclase-quartz-gneiss (Fordham)
Lowerre quartzite (right-side-up) 15 ft.
Unit A Inwood white dolomitic marble 10-15 ft.
Unit B Inwood - impure siliceous dolostone with phyllitic layers 20 ft.
Manhattan (Oma) - calcareous, siliceous black metagraywacke, biotite-quartz-plagioclase schist, and lustrous garnet-staurolite-muscovite, biotite quartz schist.
The lower units of Oma are characterized here by concentrations of pale green tourmaline with khaki green overgrowths. Similar zoned tourmalines are present in Oma at STOP 3 and again at Verplanck Quarry (STOP 5).
The dominant foliation S1, sub-parallel to bedding, varies from N80°-90 °E and dips 70°-80° to the north. S2, here a well developed foliation (N80°E, 85°S), folds S1 producing east-plunging folds of S1 and S0.
A locally well-developed S3 crenulation cleavage, (N45°-50°E, 90°) cuts S2 and S1 surfaces on a small exposure of Lower Manhattan above the sand pit.
Typical Upper Manhattan (Xmb) can be seen above the sand pit to the northeast. Note abundant refolded F1 folds; east plunging F2 folds dominate the structure. Staurolite-garnet-muscovite-biotitequartz-plagioclase schists and typical garnet-muscovite-biotite-plagioclase-quartz granulites of the Upper Manhattan are exposed. Kyanite has been found with staurolite in exposures of this unit 300 feet east of this outcrop.

STOP 3. Crugers.
The purpose of this stop is to visit excellent exposures of B type Inwood and to see the Manhattan - Inwood contact.
Begin by walking down to Hudson River behind houses to sandy dolostones of Unit B. Compound folding is common here. Thin orange weathered quartzites are common in the dolostone. Rocks similar to this will be seen at Stony Point on STOP 7. Dolostones of Unit B are best exposed in the railroad cut.
Walk north to the FDR Hospital grounds and northwest along Hudson River to small point.
Here is an excellent exposure of the Inwood formation and Lower Manhattan (Oma) contact. Note the lithic characteristics diagnostic of Lower Manhattan seen on STOPS 1 and 2. A thin 2 to 3 inch coarsely crystalline calcareous marble occurs at the contact with the schist. Beneath this a zone of interlayered gray and white, crystalline, calcitic dolostone and calcite marble is exposed before massive, beige-weathered dolostones at the waters edge. Thin orange quartzites in the beige-weathered dolostones suggest this is Unit B. A thick section (200-300 ft.) of Unit C mapped to the east is not present here.
Walk east along contact. Note minor transverse faults and tectonic breccias filling fault planes (late state effects of Cortlandt intrusions, perhaps). Isoclinal F1 folds are common along the contact zone to the east.
Walk up section to foot path. Note here black and white striped calcitic schists of Manhattan Unit A. This is a very distinctive lithology seen in many places just above the base of Unit A . An excellent exposure of this can be seen at the north end of a roadcut on new Route 9 at Prickly Pear Hill (NE 1/9 Haverstraw Quad. ). Common mineral assemblages and texture in Oma at this locality are lepidoblastic muscovite and biotite (parallel to S1)-quartz-plagioclase-calcite-garnet.
Upper Manhattan is exposed above on a hill. Note change in color of the rock and in bedding characteristics. Lepidoblastic biotite and muscovite are common along with garnet, quartz, and plagioclase. Staurolite is present in some layers.

STOP 4. George's Point.
Excellent exposures of Upper Manhattan (Omb) granulites and schists. F1 folds are well exposed and dip steeply to the northeast and are mildly folded by late northeast plunging F2 folds.
This point is located between a large dioritic mass to the east and a pyroxenitic-noritic mass to the northwest (Montrose Point). The late F2 folds may be a result of shouldering aside of the country rocks by one or both plutons. These schists belonging to the Upper Manhattan will be seen at Verplanck on STOP 5 and again at Stony Point on STOP 7.
Garnet-biotite-muscovite-plagioclase-quartz is the common mineral association. No staurolite has been found here.

STOP 5. Verplanck Point Quarry (for location see Figure 1).
The contact between Unit A of the Mmhattan Formation (compare with STOPS 1, 2, and 3) and the Inwood Formation is exposed in the east wall of the quarry.
Climb over the wall carefully. a few at a time. Pelmatozoan fragments are abundant in a blue-gray crystalline limestone at the base of the Manhattan. Abundant isoclinal (F1) folding repeats this zone several times. One excellent stem plate is preserved in the crest of a small S1 isocline beneath the overhang. NO HAMMERING PLEASE! F1 axial planes strike N35°-40°E and dip 50°-60° SE. F1 plunges are moderately steep to the southwest. F2 crenulation cleavage is incipient and weakly folds the F1 axial planes. Axes of F2 plunge S25°-30° E at 45°-50°.
The intensity of F2 folds increases toward the complex.
Note the distinctly phyllitic texture of the rock. Biotite-muscovite-quartz- calcite-plagioclase-garnet is the common assemblage. Biotite usually predominates over muscovite. Both are perfectly oriented in S1 and folded by S2. An interesting bed two feet from the marble contains abundant red-brown biotite, garnet, and minor amounts of staurolite. Very distinctive green tourmaline with khaki overgrowths is an accessory mineral in most specimens of Oma here.
Walk north along rim. Excellently exposed F1 folds are shown by limy interbeds in the Lower Manhattan.
The north face of the quarry exposes white dolostone closest to the schist, assigned tentatively to Unit C of the Inwood Formation. The main layered dolostone in the quarry is characterized by dark dolostones with black phyllitic partings and thin quartzite stringers. Weathered surfaces are cream or beige. These rocks are assigned to Unit B of the Inwood Formation.
If time allows, we will walk west to the Hudson River down cliffs of sandy dolostones of Unit B to white crystalline dolostones exposed at the river's edge that probably belong to Unit A of the Inwood Formation.
A change from the staurolite-almandine subfacies of the almandine-amphibolite facies (at Verplanck quarry) to the quartz-albite-epidote-biotite subfacies of the greenschist facies (Tomkins Cove) takes place over a distance of 1.5 miles. This is a rather steep metamorphic gradient in regionally metamorphosed areas. For example, from biotite to staurolite isograds in Dutchess Co. is three miles (Balk, 1936).
Staurolite generally is ascribed to regional metamorphism because of the relatively high pressures thought to be necessary for its formation (Winkler, 1965). However, staurolite has been reported from the aureole of a shallow level granitic pluton (Rastall, 1910). Moreover, Winkler (1965, p. 109) believes staurolite with almandine might be expected in restricted areas bordering deep level plutons.
Metacrysts of staurolite and almandine in the Lower Manhattan Formation at Verplanck Point Quarry have textures indicative of post F1 crystallization and may have formed synchronous with or later than the F2 fold system. These observations are consistent with an hypothesis attributing the garnet and staurolite to contact effects induced by intrusion of the Cortlandt intrusives. Contact metamorphism under high confining pressure might be the cause of the steep metamorphic gradient seen here.
LUNCH STOP

STOP 6 (end of road). (Beware of dogs.)
Small outcrop of Upper Manhattan (Omb) - typical granulites very similar to George's Point (STOP 4). Note folded F1 folds and strong development of F2 structures. Fracture fillings in S2 probably are related to increased grade of contact metamorphism as Cortlandt intrusives are approached. Compare intensity of F2 structures with STOP 5, and note the similar orientation.

STOP 7. Tompkins Cove - Stony Point (see Figure 4 for location).
A. Railroad cut by DarkSeaGreen and Rockland plant north of quarry. Exposed on west wall is interbedded Lower Manhattan (Oma) and "crinoidal" limestone unit seen at STOP 5. Isoclinal F1 folding is common. Note refolded F1 fold and steep plunges of F1 folds.
B. Walk into main quarry. The contact of the "crinoidal" limestone unit with underlying (stratigraphically) white dolostones is exposed on the west slope of the quarry. Adventurous ones may climb up to see a truncation of S0 in the dolostone by the limestone. Is this sedimentary, or tectonic and the result of flowage? Be very careful of those following you; do not dislodge loose blocks.
From the quarry walk east to the railroad tracks and walk south toward Stony Point. Exposures of sandy dolostones, perhaps Unit B of the Inwood Formation (tops east?).
C. First outcrops are biotite diorite of the Cortlandt Complex. Climb up hill to exposure of contact with Lower Manhattan. Note discordant contact and nonfoliated igneous rock and apophyses.
D. Walk south along ridge toward Cortlandtite pluton to contact with Oma. Note brecciated rock close to Cortlandtite. Fragments of foliated biotite schist float now in a matrix of K-feldspar-sillimanite-garnet and quartz. This sillimanite zone is very thin, perhaps 10 feet thick. Closest to schist is a green hornblende-rich contact phase developed around the pluton at the contact with either diorite or schist.
E. Walk down to road to west. Follow road south. Note small outcrops of limestone. Exposures of calcitic marble and Lower Manhattan (Unit B) on slopes above pond. This is metamorphosed equivalent of the crinoidal zone exposed on the west flank of the anticline. The very distinctive Oma here is a biotite-muscovite-quartz-plagioclase phyllite.
F. Continue to the south to road. Cross swamp to base of ridge to south. Exposures of carbonate rock on hillside. Probably Unit B of the Inwood Formation. Note the position south of the intrusives and its relation to STOP 3 at Crugers. The carbonate rocks close around the south side of the Cortlandt rock at Stony Point.
Walk east along carbonate outcrop to railroad tracks. Then head north along railroad toward intrusives.
G. Railroad cut in Upper Manhattan (Unit B). Shown here are dikes cross-cutting F1 and F2 folds. The contact with Cortlandtite pluton is exposed at the north end. Follow cross-section, Figure 6, for location on east wall. If a train comes, you will be warned. Please move promptly to the west side of the cut where there is plenty of room. Don't panic!
Continue north to see near vertical contact of the Cortlandtite with the schist. Note contact zone with minor drags, indicating north-up rotation sense. The hornblendite zone seen at STOP 7-D passes into typical north-dipping layered Cortlandtite 20 feet from the contact. Immediately above to the east on the slopes (see light colored soil zone) are exposures of calc-silicates of the basal Manhattan, exposed in an F1 isoclinal fold that is truncated by the Cortlandtite pluton. F2 folds are E-W perpendicular to Cortlandtite contact. The type locality of Cortlandtite (Williams, 1886) is located on the north shore of Stony Point near the swimming pier.
In the time remaining feel free to wander into the Park where there are excellent exposures of the biotite diorite with late cross-cutting lamprophyres and still later aplitic dikes. Flow structure and xenoliths can be seen in the biotite diorite. No hammering on exposed surfaces in the Park, please.
Meet bus at Stony Point Park.

I: DEEP-WELL INJECTION OF TREATED WASTE WATER--AN EXPERIMENT IN RE-USE OF GROUND-WATER IN WESTERN LONG ISLAND, N. Y.
By N. M. Perlmutter, F.J. Pearson, and G.D. Bennett
U. S. Geological Survey, Mineola and Albany, N.Y.
Publication authorized by Director, U.S. Geological Survey
Work done in cooperation with the Nassau County Department of Public Works.
No Road Log

J: GEOLOGY, GEOMRPHOLOGY, AND LATE-GLACIAL ENVIRONMENTS OF WESTERN LONG ISLAND, NEW YORK
OR
SUBURBAN PLEISTOCENE GEOLOGY: WHO BUILT A PARKWAY ON MY BOG?
By Leslie A. Sirkin, Adelphi University.
The glacial geology and geomorphology of western Long Island were first studied in detail by Woodworth (1901) and Fuller (1914). Supplementary and more recent work has been contributed by de Laguna and Perlmutter (1949), Swarzenski (1963) and Perlmutter and Geraghty (1963), among others. The reconstruction of late-Wisconsin and postglacial environments in western Long Island is based mainly on the relationships between the glacial deposits, geomorphology, and radiocarbon dated pollen stratigraphy. The pollen stratigraphy and chronology for this region (Sirkin, 1965) show consistent similarities to the late-glacial and postglacial pollen stratigraphy and chronology of southern New England (Deevey, 1958) with notable exceptions: (1) a longer and presumably more nearly complete late-glacial record is found in the vicinity of the terminal moraine (i. e., near the southern limit of late-Wisconsin glaciation), (2) deglaciation began earlier in the terminal moraine region than to the north in New York and New England, (3) the pollen record-begins with pollen spectra indicative of parktundra vegetation, rather than the high Arctic tundra suggested in southern New England (Leopold, 1956; Ogden, 1959), and (4) the pollen zones, at least through subzone B2 (pine, oak), begin earlier in western Long Island and are time transgressive into southern New England. Finally, correlation between the pollen record, glacial geology, and geomorphology provides a means of interpreting the late-glaCial physical environment.

J: GEOLOGY, GEOMRPHOLOGY, AND LATE-GLACIAL ENVIRONMENTS OF WESTERN LONG ISLAND, NEW YORK

Flushing Bay
Note crossing Flushing Bay, a glacial trough which may be linked to the Bronx River valley on the Bronx side of the East River.

STOP 1. Alley Pond Borrow Pit.
This exposure provides an opportunity to observe the lithology and structure of the Harbor Hill Moraine, (Plate 1, figure 1), the till (upper 5+ feet), the Little Neck Bay trough, and from the top of the cut, the New York skyline. Long axes of pebbles from the till point generally NNW, Note: The extension of Little Neck Bay with Eastchester Bay and the Hutchinson River in the Bronx to the north; the drumlinoid hills - Fort Totten on the west side and Douglaston on the east side of Little Neck Bay. Occassionally, the stratified drift below the till is exposed in gullies. A section is also exposed at the northeastern corner of the Korvette shopping center, below 251st st. North of the L.I.E. a small lobe projecting from the valley wall on the east side was dissected in construction. It may have been a small kame. Alley Pond bog is on top of the moraine on the west side of the valley.

LOOK STOP. Lake Success.
A kettle lake about 0.4 miles across and about 75 feet deep; several small kettles are located on the west and south sides of Lake Success.

STOP 2. Lakeville Road - Northern State Parkway.
A recent cut for widening of the parkway has exposed a section of the Harbor Hill Moraine comprised of about 5 feet of Harbor Hill till overlying 20+ feet of stratified lacustrine sands with thin clay partings (Plate 1, figures 2,3 and 4). A lake history is suggested since the results of examination for marine microfossils was negative. No other evidence for a high marine stand effecting deposition along the moraine has been found, other than the suggested wave cut cliff along the distal slope of the moraine (Woodworth, 1901). The kettle topography north and east of this site suggests that the stratified fine grained section was deposited in an ice dammed lake on the distal slope of the moraine at the junction of the outwash plain. Other large kettles developed on the pitted outwash just south of the moraine. This section is located near the junction of the Harbor Hill and Ronkonkoma moraines which may have some relationship to the stratigraphy if ice movement pivoted at this point, calving-off large ice blocks.

STOP 3. Willis Avenue - Northern State Parkway.
In this cut, northeast of the intersection, a section of 4 to 8 feet of till overlies 10+ feet of cross bedded sands and gravels and very coarse cobbles. (Plate 1, figure 5) This section is in the Ronkonkoma moraine and demonstrates the superposed till (cf.the Harbor Hill Till) over outwash and the kame like nature of the moraine.

STOP 4. Roslyn Road - Northern State Parkway.
Another cut into the Ronkonkoma Moraine, on the northeast side of the road, has exposed the lower till (cf. the Montauk Till). Approximately 10 to 15 feet of till are overlain by 25 to 30 feet of coarse cobbly, outwash (or Kame) deposits (Plate 2, figures 1 and 2). The till when exposed in a drainage trench appeared to grade downward and southward into sandy lenses.

STOP 5, Harbor Hill, Roslyn.
Harbor Hill is the type locality of the Harbor Hill Moraine and the Harbor Hill Till. The contact between the till and the outwash may be examined here (Plate 1, figure 6). The hillside just northeast of Route 25A (on the east side of the bridge) is underlain by a kame (Swarzenski, 1963). Observe the Hempstead Harbor trough and the borrow pits along the west side of the Harbor in Port Washington. Flower Hill bog is above the borrow pits and is being cut into at this

ALTERNATE STOP 6. Garvies Point.
Described at STOP 6, ahead, and in text.
The Preserve, a Nassau County facility, is set aside for archaeologic studies, and in addition to exposures of Cretaceous and Pleistocene deposits in the cliff sections, contains paleo-Indian shell middens and a possible Indian fishing site in the Cove. Typically, red, gray, and white clay with lignite lenses, marcasite nodules, and fossiliferous (plants) siderite nodules are exposed at the base of the cliffs. The plant fossils include woody fragments and leaves of fig and magnolia. Preliminary pollen and spore analysis of the clays indicates Raritan or possibly Magothy age. The clays are overlain by a white sand section and/or outwash and/or till (Harbor Hill ground moraine or recessional till) (Plat8 2, figures 3 and 4). The attitude of the slump blocks is evident here.

STOP 6. Police Rifle Range, Port Washington.
A stratigraphic section, measured in detail by students of Dr. David Krinsley, Queens College (Dr. Krinsley, personal communication) include from the base: 14 feet 2 inches of poorly sorted, pebbly, medium grained sands, 40 feet 10 inches of white sands, which are often pebbly and streaked with iron and manganese oxide stain, and about 15.5 feet of alternating light and dark sands and gravels. The age of the "white sand" layer is questionable, since it is reportedly unfossiliferous (although Dr. Walter S. Newman reports one Cretaceous spore from this horizon).
Observe Mosquito Cove - Glen Cove Creek to the ENE across the Harbor. This inlet and the low break in the cliffs north of the Rifle Range constitute a portion of the east-west drainage along the glacial stillstand referred to in the text. The Cretaceous crops out at Garvies Point on Mosquito Cove and in the Morgan Park north of that site, but it is not exposed north of the borrow pit. The cliffs to the north in Sands Point are composed of 20 to 40 feet of outwash overlain by a thin layer (5+feet) ground moraine.

STOP 7. Manhasset Valley Park - Manhasset.
At this stop, one, or possibly two, separate kames (or kame deltas) are found mantling the moraine consisting of thin till over outwash. The outwash is apparently folded or has flowed (Plate 2, figure 5) and is occasionally exposed in building excavations on Northern Boulevard (Route 25A). The till is probably recessional or ground moraine of late-Harbor Hill age. The kames exhibit striking ice contact structures (Plate 2, figure 6) and indicate a late Harbor Hill glacial advance which sent tongues of ice up the troughs. This advance is supported by several lines of evidence:
(1) the presence of kames at the valley heads.
(2) sculpturing of peripheral deposits (i.e. the drumlinoid hills) and deformation of cliff sections (although the outwash may also have been deformed during the initial Harbor Hill advance).
(3) Oscillation in the pollen record: The subzones W2 - W3 sequence indicating the stillstand and the return of cold indicators in subzone T1.
(4) the stillstand evidence including the "deltas" of Woodworth (1901) and the E-W drainage lineation (Figure 1).
Tracing the deposits clockwise around the exposure, observe the kame, next (above the wall) outwash (thin till at top) and kame (fronting on 25A behind gas station).

Note the drumlin (possible) south of lake on east side of road.

Note cuts into the moraine
Note cuts into the moraine while ascending the trough on the proximal slope of the Harbor Hill Moraine.

GUIDEBOOK
to
Field Excursions
at the
41st Annual Meeting of the
May 1969
Stockton G. Barnett, Editor
Host:
Department of Physics and Earth Sciences
State University College
Plattsburgh, New York

A: SEDIMENTARY CHARACTERISTICS AND TECTONIC DEFORMATION OF MIDDLE AND UPPER ORDOVICIAN SHALES OF NORTHWESTERN VERMONT NORTH OF MALLETTS BAY
David Hawley
Hamilton College
Clinton, New York
The central lowland of the Champlain Valley is underlain by Cambrian and Ordovician sedimentary rocks, bordered on the west by the Adirondack Mountains of Precambrian crystalline rock upon which Cambrian sandstone lies unconformably, and against which sedimentary rocks have been dropped along normal faults. The lowland is bordered on the east by low-angle thrust faults on which massive dolomite, quartzite, and limestone, as old as Lower Cambrian, from the east over-rode weaker Ordovician shale and limestone. The westernmost thrusts, the Highgate Springs thrust in the north, and the overlapping Champlain thrust in the south, trace an irregular line a few feet to 3 1/2 miles inland from the east shore of Lake Champlain. For most of the distance between Burlington and the Canadian border, the high line of bluffs marking the trace of the Champlain Thrust are composed of the massive, Lower Cambrian Dunham dolomite.
The shales, youngest rocks of the autochthonous lowland sequence, outcrop on most of the islands in Vermont, and the mainland between the thrusts and the lake. Although exposures on almost continuous shore-line bluffs are excellent, there are few outcrops inland because of glacial cover and low resistance of the shales to weathering. Fossils are rare in the older calcareous shale (Stony Point) and absent in the younger noncalcareous shale (Iberville). The lithic sequence was established almost entirely on structural criteria. Where it can be found, the Hathaway submarine slide breccia structurally over lies the Iberville

STOP 1. West shore of South Hero Island
West shore of South Hero Island, extending for one mile southward from the breakwater at Gordon Landing. The lower 215 feet of the Stony Point formation is exposed between the breakwater and the top of the Cumberland Head formation, 2900 feet to the south. In the next 2300 feet of shoreline, the upper 145 feet of the Cumberland Head formation is exposed. These sections are described in the text article. The south end of this section is cut off by a right lateral wrench fault striking N 59° W, dipping 79° NE. South of the fault the interbedded limestone and shale (about 79% ls., 30% sh.) have been mapped as the Shoreham member of the Glens Falls formation (Erwin, 1957) on the basis of lithology and the presence of Cryptolithus.

STOP 2. Road cut on east side of U.S. 2
Road cut on east side of U.S. 2 halfway between City Bay (North Hero Beach roadside park) and Carrying Place. This outcrop shows the interbedded laminated argillaceous limestone and calcareous shale typical of the middle section of the Stony Point formation. It lies close to the axis of a major, northeastward plunging anticline.

STOP 3. Middle point on north side of Carry Bay
Middle point on north side of Carry Bay, North Hero, 2000 feet east of Blockhouse Point. Typical Iberville cyclic bedding is exposed for about 1500 feet along this shore, extending eastward from the place where the access road meets the shore. From west to east are: an asymmetrical syncline, an asymmetrical anticline, and to the east of a covered interval is the east, overturned limb of a large syncline. These folds are in the axial area of a large, northeastward plunging, overturned syncline. Relationships of cleavage to bedding, axial surfaces, and direction of plunge are well shown. Small-scale current cross-lamination on some beds indicates southwestward flow.

STOP 4. Quarry in Iberville
Quarry in Iberville (mislabelled "gravel pit" on No. Hero Quad. map), 1.6 miles S 10° E from east end of North Hero-Alburg bridge. The beds are almost flat-lying, and only about 15 feet of section is exposed, but it is typical cyclic deposition, and the details are well shown, as described in the text.

STOP 5. Unnamed promontory
Unnamed promontory 1300 feet WNW of Coon Point, south Alburg. Upper-middle Stony Point beds measuring 258 feet (Hawley, 1957, p. 60, 89-91), with the base of the section on the southern tip of the point. It is composed of: olive-gray weathering, dark-gray argillaceous limestone, frequently silty, with light olive-gray weathering bands and laminae, in units of 3 inches to 40 feet, making up 96 percent of the section; light olive-gray weathering, dark-gray fine-grained limestone in beds of half an inch to 12 inches, making up 4% of the section. There are four thin (1/4 inch to 1 1/4 inch) beds of medium light-gray weathering, medium gray fine-grained crystalline limestone. Pyrite concretions are common. Trilobites (Triarthrus becki) are fairly common on a few bedding surfaces, and a few unidentifiable graptolite fragments were found. This stop is relatively inaccessible, may be cut off by high water, and may have to be omitted.

STOP 6. A small quarry, 3.3 miles north of Alburg - North Hero bridge
A small quarry, 3.3 miles north of Alburg - North Hero bridge on the west side of highway U.S. 2. Stony Point argillaceous limestone-rich section as described for Stop 5, including a fair scattering of Triarthrus becki.

STOP 7. Upper Iberville beds on the south and west sides of Clark Point
Upper Iberville beds on the south and west sides of Clark Point, at the south end of Hog Island (Vt. Hwy. 78 crosses Hog Island), west Swanton. A 304-foot section has been measured here (Hawley, 1957, p. 91-92). It is 97.8 per cent thin-cleaving noncalcareous shale (1 to 3 inch beds) with thin laminated dolomitic siltstone (1/4 inch to 2 inch beds, occasionally thicker) and homogeneous fine-grained dark gray dolomite, weathering yellowish-brown, in beds up to 14 inches, at intervals of 3 to 50 feet. Cyclic deposition is prominent here, with an estimated 1215 cycles in this section. The thin dolomitic siltstone beds commonly show cross-lamination and ripple drift, with southwestward currents indicated.

STOP 8. Upper Iberville beds in quarry
Upper Iberville beds in quarry (mislabelled "sand and gravel pit" on East Alburg Quad. map) 1800 feet north of Vt. Hwy 78 and 600 feet west of Campbell Road, northern Hog Island, west Swanton. The rock is similar to that described for Stop 7. The quarry exposes an overturned anticline, thrust faulted on the upper, eastern limb, with adjacent syncline immediately westward, also faulted.

STOP 9. Southernmost tip of St. Albans Point
Southernmost tip of St. Albans Point, on property of Camp Kill Kare. Northeastward plunging asymmetrical anticline with linked small syncline northwest of it, in Iberville noncalcareous and calcareous shale with dolomitic interbeds.

STOP 10. Between Camp Kill Kare's access road and the lake
Between Camp Kill Kare's access road and the lake, about halfway between the private cottages and the Camp buildings. There are 31 feet of white weathering, grayish-black chert in beds of 2 to 6 inches, dipping steeply (69° ) southeastward on the southeast flank of the anticline at Stop 9. Structurally overlying the chert beds is black siliceous argillite in which bedding is not apparent because of its irregular, chippy foliation. The argillite contains rounded pebbles (avg. 1 by 2 inches) of gray dolomite and fragments of chert. Some graptolites were found in the argillite, but smearing precluded identification. This is part of the Hathaway formation. It is likely that the chert beds here represents a larger mass involved in a submarine slide.

STOP 11. Hathaway Point, at the south end of St. Albans Point.
This is the type locality for the Hathaway formation. It has a matrix of pale-greenish-yellow weathering rock seen on a polished surface to be composed of small, irregular, curdled masses of greenish-gray to olive-gray argillite. Streamed and isoclinally folded in the matrix is black siliceous argillite similar to that associated with the chert beds at Stop 10. "Floating" in the matrix are small masses of grayish-black radiolarian chert which are commonly angular, as well as masses of bedded chert measurable in tens of feet. Fragments of dolomite and dolomitic siltstone occur in the western part of the Hathaway point exposure. Numerous slickensided tectonic shears are present in a variety of orientations. One 40-foot wedge between shears is composed of isoclinally folded calcareous and noncalcareous shale with occasional boudinaged masses of fine-grained limestone, resembling the transition beds at the base of the Iberville. Both of the islands east of Hathaway Point, in the middle of the bay, are composed of chaotically deformed argillite and chert. It is assumed that St. Albans Bay may lie over a deep synclinorium.

STOP 12. Lime Rock Point, on the southeast side of St. Albans Bay.
At the base of the bluff composed of the Beldens (Upper Canadian) crystalline limestone with buff-weathering dolomitic beds, there is a dramatic exposure of the Highgate Springs overthrust; lower Ordovician Beldens Limestone over upper Ordovician Iberville calcareous and noncalcareous shale with occasional beds of yellowish-brown weathering fine-grained dolomite and silty dolomite. At the base of the high, steep bluff about one half mile to the east is the Champlain overthrust, on which the lower Cambrian Dunham dolomite is thrust westward over the Beldens. South of Lime Rock Point the Highgate Springs thrust slice is overlapped by the Champlain thrust for two and a half miles. It reappears for four miles, and then disappears again under the Champlain thrust, southeast of Beans Point. This is as far south as the Highgate Springs slice can be traced.

STOP 13. Beans Point, east shore of lake in northwest Milton.
The Hathaway crops out intermittently for 1200 feet north from Beans Point. This is in a zone of intense deformation close to the Highgate Springs thrust, the trace of which is covered, probably about 600 feet back from the shore. The base of the steep bluffs 2000 feet back from the shore marks the trace of the Champlain fault, on which lower Cambrian Dunham dolomite has been thrust over Beldens crystalline limestone and dolomite of the Highgate Springs slice.
The Hathaway is composed of boulders and fragments "floating" in mashed argillite. The argillite is mottled olive gray to dark greenish gray to greenish black. On a polished surface cut perpendicular to foliation the mottled colors are seen to represent original bedding which has been folded most intricately, and sheared with no development of slickensides or breccia. The small-scale shearing has completely healed, and some minute fold crests merge into the adjacent bed, a streaming of one bed into the next with no sharp boundary. Included in the argillite are rounded fragments of moderate-yellowish-brown weathering, dark gray fine-grained dolomite and cross-laminated dolomitic siltstone, sub-angular to rounded, up to 4 by 7 by 20 inches in size. The long axes of the boulders are approximately parallel, plunging about 55° toward S 45° E. Foliation causes the argillite to split into irregular tapered chips. Thirty-six feet of cover separates the north end of the Hathaway outcrop from cyclic-bedded upper Iberville which lies overturned, dipping 46° northeastward.

STOP 14. Camp Watson Point, 3/4 mile south of Beans Point (Stop 13).
The core of a large, overturned syncline is exposed on the point, plunging 18° toward N 56° E. The overturned limb, dipping 29° southeastward, is exposed for 200 feet or more along the shore to the south. The rock is lower Iberville transition, with interbedded calcareous and noncalcareous shale, argillaceous limestone, and silty laminated dolomite.

STOP 15. Clay Point, between Malletts Bay and the Lamoille River
Clay Point, between Malletts Bay and the Lamoille River, east shore of lake. THIS PROPERTY IS POSTED, AND PERMISSION MUST BE OBTAINED. In the transition beds in the lower Iberville (interbedded calcareous and noncalcareous shale, with argillaceous limestone, argillaceous dolomite, fine-grained dolomite, and silty-laminated dolomite with current crossbedding) there is a small, overturned anticline cut by small thrust faults. The relationship of cleavage to bedding, plunge of the fold, identification of tops by cross-bedding, and the faulting make this a worthwhile stop for a structural geology class.

STOP 16. From Kibhee Point southeastward along the shore
From Kibhee Point (northeastern South Hero) southeastward along the shore for 2500 feet, is exposed the transition from Stony Point to Iberville formations. With a few minor rumples the dip is southeastward all the way to a deep gully and small bay which separate a steep bluff-point to the east from the shore northwestward to Kibbee Point. This bluff, 2800 feet SE of Kibbee Point is composed of Stony Point argillaceous limestone and calcareous shale, overturned and dipping 55° southeastward. Thus, the gully conceals the faulted core of an overturned syncline. The fault is very likely a thrust, east side up.
West of the gully is Iberville, about 90% finely cleaved noncalcareous shale, with interbedded silty cross-laminated dolomite. Northwest from here to Kibbee Point the proportion of noncalcareous shale and silty laminated dolomitic interbeds decrease and the proportion of calcareous shale increases. About 220 feet southeast of Kibbee Point the southeastward-dipping beds are massive calcareous shale (Stony Point fm.). About 900 feet south of Kibbee Point on its west shore the Stony Point beds still lower in the section are predominantly argillaceous limestone, interbedded with calcareous shale.

B: RECENT SEDIMENTATION AND WATER PROPERTIES, LAKE CHAMPLAIN
Allen S. Hunt and E. B. Henson
University of Vermont
Purpose
Within the last few years a considerable amount of research has been done on Lake Champlain. The purpose of this trip is to show what type of work is being carried out on the lake and to report some of the findings.

STOP 1. First stop of west-east traverse
This stop, along with stops 2 and 3, will constitute a west-east traverse designed to show differences in thermal patterns, benthos, and sediment types across the lake. At stop 1, a bathythermogram will be taken to demonstrate water temperature differences with depth. A grab sample will be taken and sieved for macro-organisms, and a core sample will be collected. The sediments at this stop are organic muds which contain no gravel, less than 10 percent sand, and equal amounts of silt and clay. The mean phi size is about 8, the standard deviation 2.5 phi.

STOP 2. Middle stop of west-east traverse
A bathythermogram and core will be taken and a grab sample will be sieved for benthos. The sediment at this stop is described under "sediment properties" as a pebbly sandy clay. An average sample contains 25 percent sand and gravel, 10 percent silt, and 65 percent clay. The mean grain size is 8 phi, the standard deviation 4.5 phi.

STOP 3. Last stop of west-east traverse
A bathythermogram will be taken at this station to complete the traverse profile, the benthos will be sampled, and a plankton haul will be made. Water samples will be taken from selected depths and analyzed for alkalinity, pH, and dissolved oxygen. The sediments at this stop consist of organic muds. The mean grain size is 8 phi, and the standard deviation just over 2 phi. Sand makes up less than 5 percent of the sample with silt and clay equally divided among the remaining portion.

STOP 4. This is a shallow-water stop at the mouth of the Winooski delta.
Grain-size analysis has shown sediments to be about 90 percent sand, 10 percent silt, and 1 percent clay. The mean grain size is 2 phi, the standard deviation just over 1 phi. Note the absence of an interface on the sediment surface.

STOP 5. This stop is to collect sandy clay sediment.
The sandy clays have much in common with the pebbly sandy clays of stop 2 in that both are poorly sorted, and both have a high percent of sand and clay with only a small percentage of silt. The pebbly sandy clay and the sandy clay may be facies of the same sediment.

C: BEDROCK GEOLOGY OF THE SOUTHERN PORTION OF THE HINESBURG SYNCLINORIUM
Rolfe S. Stanley
University of Vermont
Purpose
The geology of west-central Vermont has attracted the attention of geologists since the early work of Hitchcock, et al. (1861), and Logan (1863), to mention only two. During this century notable contributions have been made by Perkins (1910), Keith (1923, 1932, 1933) and, in particular, Cady (1945, 1960). The mapping of Welby (1961) west of the Champlain thrust, and Stone and Dennis (1964) in the Milton quadrangle just north of Burlington, completes the present state of knowledge of the Hinesburg synclinorium and immediate surrounding areas (Fig. 1, inset map). These works are incorporated in the Centennial Geologic Map of Vermont (Doll, et al., 1961).
Among several major problems still rema~n~ng to be resolved is a clearer understanding of the effects of the Acadian and subsequent orogenies or disturbances on the structures of west-central Vermont. Inasmuch as rocks of Upper Ordovician through Devonian age are not present in western Vermont, it becomes most difficult to evaluate the relative importance of Taconic and younger events. Answers to this central problem with its many corollaries can hopefully be provided by detailed studies involving a combination of stratigraphic, petrologic, geochronometric, and structural approaches. It is the purpose of this trip to examine the geology of the Hinesburg synclinorium and to show how recent work may be helpful in answering these problems in the future.

STOP 1. Champlain thrust at Long Rock Point, Burlington
(Note: The Episcopal Diocesan Center has been kind enough to allow us to visit this locality. Please do not litter.) This locality is perhaps one of the finest exposures of the Champlain thrust in Vermont and Canada. Here the Dunham Dolomite (Conners facies) of Lower Cambrian age overlies the Iberville Formation of Middle Ordovician age. The thrust contact is sharp and marked by a thin discontinuous zone of breccia in which angular clasts of dolostone are embedded in a highly contorted matrix of shale. Slivers, several feet thick, of limestone are found along the fault and may represent pieces of the Beekmantown Group (Beldens Member of the Chipman Formation?). The undersurface of the Dunham Dolomite along the thrust is grooved by fault mullions which plunge 15° to the southeast (Fig. 3 diagram 1 and 2a). The average southeastward dip of the thrust is 10°.
A variety of minor structures are found in the Iberville Formation whereas joints are the only structures in the Dunham Dolomite. Faults and joints are oriented in a number of attitudes in the shale, but they have not been analyzed as yet. Many of these fractures are filled with calcite and grooved with slickensides. The minor folds in the shale are numerous, and are easily grouped into two age generations. The early folds have a well developed slaty cleavage which offsets the bedding and attests to differential flow parallel to the axial surface. Although only a few fold hinges are present, the slaty cleavage forms the dominant layering and is concordant to the undersurface of the Dunham Dolomite.
The younger generation consists of asymmetrical drag folds with short gently curved hinges and rather open profiles. The axial surface is rarely marked by cleavage but when it is developed, fracture cleavage, which is commonly filled with calcite, is typical. These folds deform the slaty cleavage of the older generation and hence are younger in age. The orientation of 59 axes with their sense of rotation is shown in diagrams 1, 2a and 2b of figure 3.
Slip line orientations The drag folds of the younger generation can be used to determine a slip surface and direction according to the method described by Hansen (1967, p. 390-397). The analysis assumes that these folds are in the truest sense drag folds and have formed by movement of one layer or zone over another. In this locality the drag folds in the shale presumably were formed by Dunham Dolomite moving over the Iberville Formation. Because the shale is highly anisotropic, consisting of thin layers of compact shale separated by thinner layers of extremely fissile shale, the folds are confined to zones several feet in thickness and are disharmonic in profile.
A slip plane and line were determined for three separate localities at Rock Point (Fig. 3, diagrams 1, 2a, 2b). For each place the 18 to 23 fold axes with their respective senses of rotation were plotted on a lower hemisphere equal area net. The great circle that best approximates the spatial distribution of axes defines the slip plane. In all the diagrams of figure 3, clockwise folds cluster along one part of the slip plane whereas counterclockwise folds cluster along the other. The bisector of the arc separating the two groups of folds is the slip line. The location of clockwise and counterclockwise arrows on either side of the separation arc determines whether the upper layers moved up or down along the slip line. In diagrams 2a and 2b (Fig. 3) the upper layers moved to the northwest along a line striking N 40 W for 2a, and N 54 W for 2b. In contrast the upper layers moved downward along a line striking N 86 E for the southern part of the Champlain thrust at Long Rock Point. (diagram 1, Fig. 3).
Discussion of Results The kinematic basis for this analysis has been worked out in such geologic environments as tundra and sod slides, glacial lake clays, lava flows and metamorphic rocks of all grades (Hansen, 1967; Hansen, et. al., 1967; Howard, 1968). It can be shown that the separation arc contains the movement direction of slip line and that the drag folds which locate this direction are a product of one movement event. One can further deduce the likely position of the principal axes of stress (σ1,σ2, σ3 by analogy to slip systems. σ2 would lie in the slip plane perpendicular to the slip direction. σ1 and σ3 would define the deformation plane which is perpendicular to the slip plane and parallels the slip direction.
σ1would be oriented approximately 45° from the slip plane in a direction permitted by the sense of shear indicated by the drag folds. The slip line would then parallel the direction of maximum resolved shear stress.
In all subsequent discussions σ1 is the maximum compressive stress, σ2 is the intermediate compressive stress and σ3 is the minimum compressive stress.
Diagrams 1 through 3 (Fig. 3) were determined at localities in the Iberville Formation beneath or just west of the Champlain thrust. With the exception of diagram 1, the slip directions indicate movement to the northwest (see diagram 7, Fig. 3 for synopsis). This direction is approximately parallel to fault mullions at Long Rock Point and slickensides on calcite-veneered surfaces at Shelburne Point (diagram 3) and, therefore, suggests that the deformation plane containing σ1 and σ3 for this phase of movement did trend northwesterly. A unique explanation for the easterly slip direction in diagram 1 is not known at present, but several possibilities will be discussed.

STOP 2. Shelburne Access Area
This locality is one of several places in the Monkton Quartzite that displays a sufficient number of joints, faults and feather joints for dynamic analysis. The location and orientation of faults and feather joints are shown on the geologic map (Fig. 4). At each numbered station the orientation, relative abundance, and surface features of approximately 10 joints were recorded. Diagram A of figure 5 shows the poles to 248 joints and diagram B shows four planes corresponding to the maxima in diagram A. The trend of each of the 10 feather joint arrays and their sense of shear are shown in diagram C.
Diagram D shows 13 faults with letters or arrows indicating the apparent movement. All faults trend approximately eastward (hereafter called cross faults) except for one that is striking to the north. As indicated on the map the dip slip displacement of each fault is only several inches whereas the strike slip displacement on one of these faults is 9 feet (fault 13, Fig. 4). (Faults are identified by the station number nearest them on the geologic map (Fig. 4)). Feather joint arrays adjacent to several cross faults further attest to strike slip displacement. This relationship is further emphasized by comparing diagram C and D (Fig. 5). Although Welby (1961, p. 204) assumes that all cross faults are normal faults, the above data definitely supports a wrench fault interpretation. Petrofabric analysis of quartz deformation lamellae in three samples (Ml, M3, M4) further confirms this conclusion (Fig. 6).
Dynamic Analysis Discussion of the stress configurations for each structure is based upon techniques and principles summarized by Friedman (1964). In stress analysis only the direction and relative magnitudes of the principal stresses can be evaluated. Furthermore, it is assumed that the manner in which these structures formed in nature is similar to the way analogous structures are formed in the laboratory.
Joints: The planes in diagram B (Fig. 5) corresponding to the maxima of diagram A can be interpreted in several ways. The acute angle between joints 1 and 3 is 80 degrees and the acute angle between joints 2 and 4 is 83 degrees.
Hypothesis 1: Joints 2 and 4 formed in the shear position. Joints 1 and 3 formed as extension and release joints respectively.
Hypothesis 2: Joints 1 and 3 formed in the shear position. Joints 4 and 2 formed as extension and release joints respectively. In both hypotheses σ2 is defined by the intersection of all joints. In hypothesis 1, σ1 would parallel joint 1 and trend to the east whereas in hypothesis 2 0σ1 would parallel joint 4 and trend to the southeast. Hypothesis 1 is preferred because joint 1 is commonly filled with calcite. Furthermore, this configuration is similar to the stress configurations deduced from the other structures (Fig. 6).
Feather joints: The 10 feather joint arrays in diagram C (Fig. 5) with their respective senses of shear indicate that σ1 is oriented east-west. σ3 is oriented north-south and σ2 is oriented vertically. Because the dip of the feather joint array could not be measured, the inclination of the principal stress axes could not be pinpointed. Although the principal stress directions are not as accurately known for feather joints as they are for other structures, their symmetrical relationship to the cross faults support a wrench fault interpretation and thus suggest that those faults trending north of west are left lateral whereas those trending north of east are right lateral.
Wrench Faults: The apparent vertical movement on all faults trending north of west is up to the north. This movement can be realized on left lateral wrench faults if σ1 dips more steeply to the east than the bedding. Those faults trending north of east that are downthrown to the north would then be right lateral wrench faults.
The apparent vertical movement of faults 4 and 13 trending north of east is up to the north. These faults are right lateral wrench faults if the movement on 4 is assumed to be the same as the displacement of fault 12 by 13. The horizontal and vertical components of the actual movement at these faults could be caused by σ1 trending westward and dipping eastward more gently than the bedding.
North-South Fault: This fault cuts several of the wrench faults and hence is younger in age. It could result from the following two stress configurations: Hypothesis 1: If the fault is a normal fault downthrown to the west, then σ1 would be vertical or steeply inclined to the north so as to produce the right lateral movement. σ3 would trend eastward or dip gently westward. σ2 would trend northward.
Hypothesis 2: If the fault is a wrench fault, then σ1 would trend northeasterly. σ3 would trend northwesterly and σ2 would be approximately vertical.
Quartz Deformation Lamellae: Approximately 380 deformation lamellae from 3 oriented samples have been measured from this outcrop. For each sample 100 (50 for M4) quartz grains were measured from each of three mutual perpendicular thin sections. For each grain the orientations of the c axis and deformation lamellae (if present) were measured. The results were analyzed using methods described by Carter and Friedman (1965), and Scott, et al., (1965). The deduced orientation for σ1,σ2, and σ3 are shown in figure 6. In M3 and M4, 01 lies in the bedding and 02 appears to be equal to 03 in magnitude. In Ml σ1 is inclined 40° to the east, σ2 dips 50° to the west and σ3 trends northward and is horizontal. Although these orientations are not parallel in all samples, they are consistent with the stress positions deduced from the megascopic structures and support the conclusions on the cross faults and joints.
Structural and Stress History Based on the above information it is possible to develop a structural history for this outcrop. This sequence is divided into the following three phases.
Phase 1: During this time all the wrench faults formed except fault 13, 4 and 10 (north-south fault), σ1 was inclined more steeply to the east than the bedding so that faults trending north of west are upthrown to the north and faults trending north of east are downthrown to the north. σ3 was oriented northward and σ2 was inclined steeply to the west.
Phase 2: During this time faults 13 and 4 developed with σ1 either horizontal or inclined more gently eastward than the bedding. This orientation permitted the right lateral faults (13 and 4) to be upthrown to the north. It should be emphasized at this point that the change in orientation of σ1 relative to the bedding in the Monkton Quartzite can equally be attributed to a rotation of the bedding within a stress system of constant principal stress orientation.
Phase 3: During this time the north-trending fault developed and can be interpreted as a normal, wrench, or reverse fault.
The feather joints and deformation lamellae are thought to have formed during phase 1 and 2, although definite evidence for their timing is lacking at present. The formation of the joints shown in diagram A and B in figure 5 could well have spanned the first two phases.
Relationship to the Champlain Thrust Wrench faults are commonly associated with thrust faults. Both can be related to the same σ1 direction and only require a switch of σ2 and 0σ3 in the stress configuration during thrusting to develop wrench or tear faults. In the same manner the small wrench faults in the Monkton Quartzite are thought to bear the same relationship to the Champlain thrust and as such suggests that other cross faults shown on the Geologic Map of Vermont (Doll, et al., 1961), may also be wrench faults.
The different stress orientations deduced at Long Rock Point (stop 1) and the Shelburne access area suggest several explanations. It is possible that they formed under the same stress system but have assumed their present orientation by subsequent deformation. Alternatively, they could have formed at different times under stress systems of different orientations. Future work will resolve this problem.

STOP 3. Winooski Dolomite in fault contact with Monkton Quartzite
This locality is a fine exposure of the Winooski Dolomite in fault contact with the upper portion of the Monkton Quartzite. The bedding in both these units dips gently eastward. The most conspicuous of several northeastward-trending faults is downthrown to the north placing the Winooski Dolomite in fault contact with the upper portion of the Monkton Quartzite south of the fault.

STOP 4. Shelburne Falls just southeast of the village of Shelburne
The Danby Formation dips gently eastward at this locality and is cut by several sets of joints. Ripple marks of varying sizes, cross beds and fossil burrows are well displayed in the quartzite and sandy dolomite on the west bank of the river. Current directions based on current ripples in the upper layers along the southern part of the exposure indicate flow to the southeast (S 10 E to S 40 E) whereas current directions based on cross bedding in the lower layers exposed near the falls to the north indicate flow to the north and west.

STOP 5. Jones Hill
This stop is located just west of the Champlain thrust and shows several large folds and minor thrusts exposed in the Iberville Formation. A lamprophyre dike, striking N 78 W and dipping 75 degrees to the northeast, is exposed in the southern part of the outcrop. The laccolith of syenite on Barber Hill is located approximately a mile southeast of here near the village of Charlotte.
The orientation of fold axes, slaty cleavage and faults is shown on figure 7; most of the faults are thrusts dipping eastward or southeastward at gentle to moderate angles. As shown on plate 1 the trace of the Champlain thrust is sinuous and offset at several places in the area. Welby (1961, Plate la) shows normal faults at each of these places but the orientation of bedding, particularly between Jones Hill and Pease Mountain, suggests that the eastward reentrants can be explained equally well by anticlines plunging gently to the east. Minor folds with this orientation are present on the north side of Jones Hill.

STOP 6. A short traverse through the fields north of the road.
This stop will consist of a short traverse through the fields north of the road. The Clarendon Springs Dolomite, the Shelburne Formation, and the Cutting Dolomite will be crossed. If time permits the traverse will be extended northward into the Bascom Formation. At least two generations of folds are present in this area. Axes of the earlier generation plunge to the southeast, east and northeast and possess a well developed axial surface cleavage which commonly dips eastward except when it is deformed by folds of the younger generation. The slip line orientations of diagrams 4 and 5 (Fig. 3) were determined from drag folds of the earlier fold generation at localities 4 and 5 on figure 1. These slip lines are almost parallel to those to the west of the Champlain thrust discussed under stop 1 and, therefore, strongly suggest that they may have formed contemporaneously as a result of the same stress system. The younger generation of folds plunges northward and folds the cleavage of the earlier fold generation.

STOP 7. Hinesburg thrust northwest of Mechanicsville
This locality is one of the finest exposures of the Hinesburg thrust. The Bascom Formation forms the lower plate and the argillaceous facies of the Cheshire Quartzite forms the upper plate. Minor folds can be found in both these units. Inasmuch as only 4 folds could be found in the Bascom Formation little significance can be attached to southwestward movement direction shown in diagram 6 (Fig. 3).

STOP 8. The Bascom Formation
The Bascom Formation crops out on several small hills just west of Brownell Mountain. To the east the Bascom grades into the Brownell Mountain Phyllite, a member of the Bascom Formation only recognized in the Hinesburg synclinorium. This stop may be cancelled if insufficient time is available.

D: THE LATE PLEISTOCENE OF THE CHAMPLAIN VALLEY, VERMONT
W. Philip Wagner
University of Vermont
Burlington, Vermont
The existing knowledge of Pleistocene events in the Champlain Valley can be discussed in terms of glacial stratigraphy, areal distribution of glacial deposits, and water planes of Lakes Vermont and "New York", (this paper) and the Champlain Sea. The purpose of this field trip is to examine new evidence of glacial and post-glacial events as recently deduced from field study of the Champlain Valley between Burlington and Middlebury, Vermont.
Included in the list of references are recent papers which pertain to the Pleistocene and Recent history of the Champlain Valley. The topographic quadrangles, in order of their first appearance on the field trip, are as follows: Burlington; Fort Ethan Allen; Essex Junction; Mount Philo; Hinesburg; Bristol; Monkton. Acknowledgement is made to Chester A. Howard, Jr. and William R. Parrott, Jr. for data on Stop 16, to Howard for information about surficial deposits near the mountains north of the Winooski River (Fig. 1), to Robert Switzer for field assistance in 1967 and 1968, and to Allen S. Hunt for a review of the manuscript. The work upon which this paper is based was supported in part by funds provided by the U. S. Department of Interior as authorized under the Water Resources Research Act of 1964, Public Law 88- 379.

STOP 1. Champlain Sea beach (No.1, Figs. 1 and 2)
Exposures in gravel pits on both sides of barn show excellent beach structures and marine mollusks.

STOP 2. Lake New York beach-spit and delta (No.2, Figs. 1 and 2)
Gravel pits are in beach material; slightly lower bench to west is composed of deltaic sand which correlates with No.4, Figures 1 and 2.

STOP 3. Lake New York beach (No. 56)
One of the best developed beach landforms known in the area; terrain immediately east of beach is lake clay and west of beach is a lower level Lake New York delta. Note dunic(?) landforms between stops 3 and 4.

STOP 4. Fort Ann delta (correlative with No. 57)
Gravel pit shows channel structures characteristic of deltas in this area.

STOP 5. Oak Hill outlet channel (No. 68)
Gravel pit in channel bottom shows very coarse, poorly sorted gravel; outlet drained a Winooski Valley Lake in post-Coveville (?) time and therefore proves (?) that ice blocked the Winooski Valley during Coveville time.

STOP 6. Ice-contact delta (No. 59)
Numerous gravel pits in vicinity show progressively finer material from stop 5 to stop 6 where cross-bedded fine gravel, sand, and silt are exposed in pit; ice-contact nature of delta is suggested by poorly sorted gravel in nearby vegetated area to southwest; delta was apparently formed by Oak Hill channel water drainage into local lake impounded by continental ice.

STOP 7. Fort Ann bench (No. 27)
Road cut exposes coarse, poorly sorted gravel underlying (?) boulder-strewn (lag?) bench on hillside. A problem exists here in that the topography and the lag (?) suggest an erosional environment whereas the road cut indicates a depositional environment. Possibly mantle material (see text) has been modified by wave action.

STOP 8. Hummocky dead ice terrain (No. 43)
Stop is at gravel pit showing poorly sorted character of deposit; ice contact structures are visible in places in the vicinity from time to time.

STOP 9. Ice-contact delta?
This is a brief photography stop. Large scale cross-bedding is in kame terrace, delta, or ice-contact delta(?). The last named possibility is favored here.

STOP 10. Kame terrace
Gravel pits in vicinity show characteristic ice-contact features.

STOP 11. Pre-Coveville (44, 45), Coveville (46), and upper Fort Ann (47) delta
STOP 11. Pre-Coveville (Nos. 44 and 45), Coveville (No. 46), and upper Fort Ann (No. 47) deltas; 3 miles southeast of Hinesburg along Route 116; deltas were constructed by water from a local Winooski Valley lake which drained through an outlet channel (No. 67) at the divide between Hollow Brook and Huntington River; gravel pits show coarse gravel with large scale foreset bedding and less obvious topset bedding in places.

STOP 12. Coveville (No. 50) and upper Fort Ann (No. 51) deltas
The village of Bristol is located on the Coveville delta and the upper Fort Ann delta just west of Bristol; gravel pits show features similar to those at stop 11.

STOP 13. Lacustrine sediment veneered hummocky dead ice terrain; No. 53
Gravel pit exposes ice-contact material overlain by and interbedded (?) with lacustrine sediment; features suggest glacial and lacustrine sedimentation in close proximity.

STOP 14. Shoreline features of Lakes Fort Ann and New York (Nos. 16-22)
Southwest side of Mount Philo; a spectacular succession of six wave-cut benches and one beach-spit.

STOP 15. Two(?) till locality
Stewart (1961a, Stop 6) reports two till units with intervening lake sediment. The present investigation showed complex vertical and horizontal variations. At the east end of the exposure occurs (bottom to top): gray till (25 feet); till or gravel (30 feet); slumped lake clays. At the west end: gray till (25 feet); lake sediment (25 feet). At the middle of the exposure as many as five till units with intervening lake sediment have been counted. Lateral relationships are difficult to determine due to the steepness of the exposure but facies changes are likely.

STOP 16. Two(?) till locality
Stream bank exposures of a lower gray till and upper brown till; Stewart's (1961a, Stop 4) type locality for the Shelburne (gray) and Burlington (brown) tills. At the time of this writing, fabric and clay mineralogy analyses are being made. This information will hopefully be available for field trip presentation.

E: STRATIGRAPHY OF THE CHAZY GROUP (MIDDLE ORDOVICIAN) IN THE NORTHERN CHAMPLAIN VALLEY
Frederick C. Shaw
Herbert H. Lehman College
Bronx, New York
The Chazy Limestone (the oldest Middle Ordovician Group of the Champlain Valley) was first named by Emmons (1842) from exposures 15 miles north of Plattsburgh at Chazy, New York. Here and elsewhere in the northern Champlain Valley (Fig. 1) the unit outcrops on a variety of normal fault blocks. Given the low dips and heavy cover, Chazy stratigraphy is most easily understood from various shore outcrops around Lake Champlain. Valcour Island, southeast of Plattsburgh, offers perhaps the best section of the Chazy, and has been intensively studied (Raymond, 1905; Hudson, 1931; Oxley and Kay, 1959; Fisher, 1968; Shaw, 1968). The Isle La Motte, Vermont, exposures to be covered in this trip and trip Fare those studied by many of the same authors and, in addition, display the lower contact of the Chazy with the underlying Ordovician dolostones of Canadian age.
In the northern Champlain Valley (Valcour Island and north to the International Boundary), the Chazy Limestone (now Group) consists of about 800 feet of quartz sandstones, calcarenites, dolomitic calcilutites and biohermal masses (Fig. 2). Three formations, Day Point, Crown Point, and Valcour, in ascending order, were proposed by Cushing (1905) and have persisted to the present, albeit with some controversy (Fisher, 1968; Shaw, 1968). Oxley and Kay (1959) further subdivided the Day Point and Valcour into members, those of the Day Point (Head, Scott, Wait, Fleury) coming from southern Isle La Motte in the area to be visited. Shaw and Fisher experienced difficulty in using the Valcour subdivisions outside of their type areas at South Hero, Vermont.

STOP 1. The Head, Isle La Motte, Vermont
PLEASE NOTE: STOPS 1 AND 2 ARE ON PRIVATE PROPERTY WHICH WE HAVE SPECIAL PERMISSION TO ENTER. DO NOT SMOKE IN THE FIELDS, KNOCK OVER FENCES, ETC. OTHERS MAY WANT TO RETURN TO THIS CLASSIC LOCALITY AFTER YOU.
Lakeshore outcrops of the Providence Island Dolostone (Lower Ordovician) and the Day Point Formation (Chazy Group). Dip of both units several degrees to the north. Contact well-exposed and at least locally unconformable. Locality discussed by Shaw (1968), Erwin (1957). Section measured and described by Oxley and Kay (1959).
Approximately 40 feet of Providence Island Dolostone is exposed, being very fine-grained, massive, thinly laminated, am unfossiliferous. Mudcracks and a few ripple marks complete the picture of a unit deposited in very shallow water. Following Laporte (1967), the environment of formation was probably supratidal, closely paralleling modern day environments of dolomite formation described from Florida and the Bahamas. No detailed petrologic work has been done on this unit. In the absence of fossils, the age of this unit is not known. The underlying Fort Cassin Limestone (not exposed here) is known to be Late Canadian.
The Chazy Group begins here with about 20 feet of quartz sand and siltstones together with minor amounts of greenish shale (Head Member of Oxley and Kay, 1959). Ripple marks and cross-bedding are common. The fossils consist primarily of 'fucoids' (probably recording a variety of trails, worm tubes and the like) and Lingula. The succeeding Chazy unit (Scott Member of Oxley and Kay) consists of about 40 feet of echinodermal lime sand, cross-bedded in some places. Brachiopods (Orthambonites?) and indeterminable trilobite scraps are the chief recognizable fossils. The overlying 15 feet of quartz sandstone (Wait Member of Oxley and Kay) appears very similar to the initial sandstone.
This second sandstone is followed by a thick (115 feet) lime sand (Fleury Member of Oxley and Kay) which occupies most of Scott Point and The Head south of the road. Much of the unit is composed of echinoderm fragments, although little is known about the actual morphology of the creatures involved. Both the fragmental nature of the fossils and the frequently observed cross-bedding argue for considerable agitation of the ocean bottom.

STOP 2. Upper Fleury Member of Day Point Fm and overlying Crown Point Fm.
Upper Fleury Member of Day Point Fm and overlying Crown Point Fm. 200 yards south of the right angle bend in the road is locality R 25 (Shaw, 1968) which yielded 12 genera of trilobites, including Sphaeroxochus and Ceraurinella, from a particularly coarse pocket in the upper Fleury lime sands. Gastropods (Raphistoma) and brachiopods (Orthambonites?) are also present. This same stratigraphic level elsewhere, particularly 1 mile to the NE, displays spectacular bryozoan bioherms and the very early tabulate coral Lichenaria (Pitcher, 1964). These will be viewed on Trip F.
About 50 yards north of the road at this same stop, the silty, Maclurites-bearing limestones of the Crown Point appear. The actual contact with the Day Point is not visible but the lithologic change is evident. The Crown Point here contains several modest bioherms which have not been studied in detail. The earliest known stromatoporoids (Pitcher, 1964) are known to be important reef builders nearby in this unit and doubtless are dominant here as well (see Trip F).

STOP 3. Fisk Quarry
Middle Crown Point Formation, consisting of fine-grained, dark, silty limestone with buff-colored dolomitic partings. This is 'typical', non-reef Crown Point lithology. However, in the quarry wall and some of the cut blocks, small reeflets can be seen. These are assumed to be largely stromatoporoids and calcareous algae, although they have not been studied as intensively as the reefs at the same horizon to the east (Trip F). Evidently, these reef masses could grow at some depth in relatively silty waters. The mechanism of their establishment thus does not appear to be tectonic. Maclurites (large gastropod, rare) and a few trilobites and brachiopods may possibly be collected from the limestone, although they are not abundant.

STOP 4. Sheldon Lane
Upper Crown Point and Valcour Formations; dip north several degrees. Locality R3 of Shaw (1968) and "Road to Little Monty Bay" locality of Raymond and others.
South of the road, a very low-dipping section of Crown Point and Day Point extends for almost 2 miles across fields. The transition between the two units is similar to that on Isle La Motte. Bioherms appear not to be present in the Day Point in this area. The Crown Point, however, is only about 100-150 feet thick here, being composed largely of biohermal masses. These can be seen just south of the road. Just north of the road, in and around the abandoned quarry, are exposed bioherms usually classified as basal Valcour. They are characterized by somewhat more silt than the reefs south of the road. Similar reefs on Isle La Motte have been classed by Pitcher (1964) as having a higher percentage of bryozoan and algal components than the Crown Point reefs. Billingsaria (tabulate coral) may also be important here.
Impressive cephalopod and trilobite faunas have come from the Valcour reefs here, including Glaphurus (trilobite, Pl. 1, Fig. 4) and large asaphids, illaenids and ceraurids (trilobites). Shaw (1968) has discussed the restriction of some of these forms to the reef environment. Most of the fossils appear in fine lime mud which apparently was trapped in channels and pockets in the reef framework. Lime sands of pelmatozoan origin drape the reefs.

STOP 5. Abandoned quarry of International Lime and Stone Company
This is the uppermost part of the same section covered at stop 4 and shows well the contact of the Valcour with the overlying Black River Group (see also Fisher, 1968, Fig. 25). The upper Valcour, here, probably equals the Pamelia (lowest Black River), and is a shaly dolostone bearing Rostricellula (brachiopod, Pl. 1, Fig. 4). The contact with the overlying Lowville Limestone, a massive, gray limestone is gradational. The early horn coral Streptelasma is present in this unit, although possibly not here. The Isle La Motte appears correlative to the Chaumont west of the Adirondacks.

F. THE PALEOECOLOGY OF CHAZYAN (LOWER MIDDLE ORDOVICIAN) "REEFS" OR "MOUNDS"
Robert M. Finks
Queens College
Flushing, N. Y.
Donald F. Toomey
Pan American Petroleum Corporation
Tulsa, Oklahoma

STOP 1. Walking tour of LaBombard pasture
The walking-tour will start at the north end of the picnic ground and trailer camp on the north side of Wait Bay in southeastern Isle La Motte. It may be reached by following the main north-south road down the center of Isle La Motte to its southern end, turning left (east) to the trailer park entrance, and then turning left (north) up the hill to the picnic ground. Please note that the entire trip is on private property, and that permission must be secured from the landowners for visits.
Cross the fence and walk north to the bare exposures of the Lamottia biostrome in the Fleury Member of the Day Point Formation. CAUTION! DO NOT STEP INTO SOLUTION-ENLARGED JOINTS. SOME ARE PARTLY CONCEALED BY VEGETATION. WALK ONLY ON BARE ROCK SURFACES. THE JOINTS ARE OVER A FOOT DEEP.
The hemispherical to discoidal heads of Lamottia are closely packed in a calcarenite matrix. Joints offer an opportunity to observe their orientation in section. More than half are overturned over much of the area. Many are broken. The proportion of broken ones increases to the north and east, where the biostrome passes into calcarenite with ever fewer and smaller fragments of Lamottia. In the central area of the exposure there are belts some 10 feet wide in which fragmentation, proportion of over-turned specimens, and quantity of calcarenite matrix, are higher than elsewhere. These may represent surge channels. In the peripheral area to the northeast one may see much laminar Batostoma chazyensis surrounding the Lamottia fragments. This is the type locality for the genus Lamottia Raymond, 1924. Although Raymond's description of this bed as the "world's oldest 'coral reef" may be disputed, it still seems to be unchallenged as the world's oldest occurrence of corals of any kind.
Walk northwestward upsection, so far as fence lines, cultivated fields, and vegetation permit. DO NOT DISTURB FENCES OR LEAVE GATES OPEN! NO SMOKING WHILE WALKING THROUGH THE FIELDS; THERE IS A DANGER OF FIRE. ALSO, PLEASE KEEP OFF CULTIVATED GROUND.
At about 2000 feet N 45 W of the Lamottia outcrop, we will find small mounds of Batostoma chazyensis at the top of the Day Point Formation. They tend to show a N·S alignment, the zoaria are mostly branching rather than laminar. Possibly this is a deeper water environment than that of the Lamottia biostrome.
Continue to walk northward to a small dirt road, then walk west along it to a T-junction with a larger dirt road. Turn left and follow it southwest to a house and barn on the right. We will enter a gate into the large pasture behind the house and barn. Mr. Ira LaBombard, the present owner of the property, has kindly given us permission to enter his pasture to study the reefs in the Crown Point and lower Valcour Formations. He has requested, as a condition of permission, that NO SPECIMENS WHATEVER be collected. PLEASE RESPECT THIS ORDER. We will have an opportunity later in the day to collect from these same beds at another locality. The fossils are so beautifully displayed here that relationships may be seen without disturbing the rock. They may be photographed very advantageously on the glacially polished surfaces.
The reefs exposed here are mainly in the Crown Point formation and are the ones intensively studied by Pitcher (1964). You may examine contemporaneous reefs by walking northeastward along strike. You may examine successively younger reefs by walking northwestward upsection (slip is about 100 NW).
The reefs are exposed as mounds of light rock. The calcarenite between the reefs, and filling the channels in the reefs, is nearly black. The reefs outcropping nearest the fence were mapped by Pitcher as his Assemblage A, consisting of the stromatoporoid Cystostroma and the alga Solenopora. Those beyond to the northwest, and covering most of the pasture up to a distinct linear rise in ground, belong to Pitcher's Assemblage B. These show interesting variations from reef to reef as well as changes in faunal distribution from flanks to tops of the mounds. The fauna consists of the stromatoporoid Pseudostylodictyon eatoni, the lithistid demosponges Zittelella varians and Anthaspidella sp., the tabulate coral Billingsaria parva, the bryozoan Batostoma chazyensis, and the calcareous algae Solenopora, Sphaerocodium and Girvanella.
The fossils may be identified readily on weathered surfaces as follows:
1. Pseudostylodictyon eatoni: Large whitish masses with fine, dark laminae forming concentric patterns about centers an inch or two apart. These concentric patterns represent the mamelons and their small size is characteristic of the species.
2. Zittelella varians: Circular, dark gray bodies two to three inches in diameter, with a central circular light area representing the matrix-filled cloaca, and radial light areas, or ovoid dots, a few millimeters wide, representing the canals. In longitudinal section, the sponge is conical, and oblique sections will show the expected intermediate shapes. Some specimens have an irregular outline in cross section.
3. Anthaspidella sp.: Similar to Zittelella in color and texture, but shaped like long sinuous bodies, an inch or so thick and several inches long, when seen in cross section. A surface view of the sheet-like sponge shows a somewhat irregular mass with out a cloaca. The complete sponge has a short stalk, the whole being shaped somewhat like a distorted cake-plate. The open, "spongy" texture may help when shape fails. Needless to say, the shape and geometric arrangement of the spicules in thin section is necessary for a secure identification. Not every shapeless mass is a sponge.
4. Billingsaria parva: Small, black, oval patches, a few inches across. The dark color is very distinctive. Close inspection with a hand lens will reveal the stellate outlines of the corallites with their characteristic septal ridges.
5. Bryozoa: These weather white, either as small, branching twiglets, or as laminated sheets. Identification requires thin sections, but the outlines of the zooecia are usually visible on the weathered surface and suffice to identify it as a bryozoan.
6. Solenopora: White concentric circles, often sparry. A few inches across. This is the most common form of Solenopora seen on the reef surfaces.
7. Girvanella: Small black ovoid bodies, less than an inch in length. These are oncolites, or algal-coated shell fragments.
8. Maclurites magnus: Large coiled shells a few to several inches across. No septa. The shell substance is white in cross section.
At the rise in ground is a one-foot stromatolitic layer with many orthocone cephalopods. Pitcher called this his Assemblage C and assumed it was laid down as a blanket during a relative drop in sea level. It forms a dip slope through which appear, apparently, the tops of Assemblage B mounds, as well as small mounds of Batostoma chazyensis alone which Pitcher called Assemblage D. At the west end of this cuesta-like feature, nearest the main road, a good cross section of an Assemblage B mound is exposed (see Plate 2).
Down the dip slope, above a ten-foot interval of grey calcarenites, are mounds in the lower part of the Valcour Formation. They are composed of Batostoma campensis, together with the alga Solenopora. Some Zittelella may be found. The bryozoa are clearly dominant.
Walk northeastward along strike for about a half-mile, observing Crown Point mounds as you go. You will eventually reach the Goodsell Quarry, operated by the Vermont Marble Company. The quarry is opened in the lower beds of the Crown Point which are relatively lacking in reefs except for small stromatoporoid-algae mounds. The quarry has been intermittently active, and the stone, which makes a beautiful black marble when polished, has been widely used as an interior trim. The rock weathers light gray, and has also been used locally as a dimension stone. It was used to build the old border fort, Fort Montgomery, visible from the Rouses Point bridge.
CAREFULLY avoiding falling into the water-filled quarry, one may observe vertical sections through stromatoporoid-algal mounds and their relationships with the surrounding calcarenite (see Plate 5). By tracing laminae from the mounds into the surrounding sediment, one can see that the mounds never stood more than a foot or two above the sea floor at anyone time, though the total thickness is much greater because of the persistence of the mound population on the same spot. On the quarry benches, especially the glacially polished upper surface, one may see plan views of mounds and note their tendency to a N-S lineation. On these surfaces also, especially when wet down, one may see orthocone and other nautiloid shells, and Maclurites shells, overgrown by algal coatings.
This ends our examination of the Isle La Motte exposures. On our way back we will stop at the Sheldon Lane section, south of Chazy, where we may collect from the Crown Point and lower Valcour, in essentially the same facies.
The Sheldon Lane beds dip north. We will begin with cross-bedded upper Day Point (Fleury) calcarenite at the south end and walk through the entire Crown Point section including reef mounds with the same fauna as in LaBombard's pasture. North of the road is an old quarry in which the lower Valcour is well exposed.

STOP 2. Sheldon Lane
On our way back we will stop at the Sheldon Lane section, south of Chazy, where we may collect from the Crown Point and lower Valcour, in essentially the same facies.
The Sheldon Lane beds dip north. We will begin with cross-bedded upper Day Point (Fleury) calcarenite at the south end and walk through the entire Crown Point section including reef mounds with the same fauna as in LaBombard's pasture. North of the road is an old quarry in which the lower Valcour is well exposed.

G. SURFICIAL GEOLOGY AND GEOMORPHOLOGY OF WHITEFACE MOUNTAIN AND KEENE VALLEY
Jesse L. Craft
Carleton University
Ottawa, Ontario

STOP 1. Whiteface Mtn "Coon Pit" stop
Proceed from the bus to the chair lift and ride to the end of first lift. "Coon Pit" stop. After getting off the chair lift walk up stream to the waterfall. There is a deep glacial grove enlarging a joint. Which direction was the ice flowing to cut this grove?

STOP 2 - Top of Whiteface Mountain
After leaving the chair lift walk to the top of the mountain. Gather at the elevation marker.
From this point you can observe the only indication I have observed of continental glaciation over riding the mountain tops in the high peaks region. This is the "roches moutonnees" form of the crest on the south side of the peak.
Observe the "horn" configuration of the peak area. The "cirque form" of the valleys leading away from the peak and the very narrow "arete" ridge to the west of the peak. Could these features develop from Continental Glaciation?

STOP 3 - Atmospheric Sciences Research Centre, Whiteface Mountain Field Station
Leave the bus and walk up the jeep road to the Whitebrook valley trail (unmarked). We will be going about ~ mile up the valley. Anyone that wishes to, may stay at the centre and look around the lodge.
Whitebrook Valley Moraine. This ridge was described by Alling (1919) as a lateral moraine of a local glacier occupying this "cirque". Notice the high percentage of Potsdam sandstone pebbles lying on the surface.

STOP 4. - County Gravel Pit on 9 N
10' till, grey oxidize moderately stoney, very sandy at base, large folds of underlying sand, silt and clay carried upward into till.
50 to 100' fine sand, silt and clay upper 5' strongly contorted by load folding.

H: META-ANORTHOSITE OF THE JAY-WHITEFACE NAPPE, AUSABLE FORKS-LAKE PLACID QUADRANGLES, NORTHEASTERN ADIRONDACKS, NEW YORK
Bradford. B. VanDiver
State University of New York
Potsdam, New York

STOP 1. Locality A, Jay, Ausable Forks Quadrangle
Take woods road beginning opposite Tirolerland restaurant, 0.8 miles N. of Jay on Route 9N. Follow woods road to point where it begins to veer sharply south, 0.25 miles from Route 9N. Climb 100 yards south to exposed slabs on hilltop which has been stripped and cleared by Rock of Ages Corp. Professor Brewster Baldwin of Middlebury College prepared base map by plane-tabling on which geology and sample localities have been plotted (Fig. 2).
The exposure is representative of massive, generally porphyroelastic, core meta-anorthosite of the "Marcy-type," but shows the considerable local compositional and textural variation encountered in this map-unit. Three local facies have been distinguished here, viz:
Facies I: A fine-to-medium grained granoblastic equigranular gabbroic meta-anorthosite, locally passing into an anorthositic metagabbro, largely confined to the northwestern portion of the outcrop. It shows many analogies with the border facies anorthosite. (Whiteface- type") and perhaps should be so mapped. Clinoopyroxene (Wo40En35Fs25) takes place of hypersthene in this facies, and garnet is absent.
Facies II: This is the predominant lithic type in the exposure and consists of inequigranular meta-anorthosite with plagioclase megacrysts forming from about 25 to 70 per cent of the total rock volume, the proportion of megacrysts decreasing toward the southeast. Hypersthene is the major ferromagnesian constituent, but locally incipient rims of garnet and clinopyroxene are visible. Before concluding that the finer-grained plagioclase matrix between the megacrysts is of proto clastic origin or produced by post-crystallization deformation, examine the hypersthene grains intergrown with the matrix. Many will be seen to be optically continuous as shown by reflections from parallel cleavage surfaces and may indicate an ophitic intergrawth suggestive of a final, possibly eutectk, assemblage.
Facies III: Appearing as irregular patches up to 50 feet across in facies II meta-anorthosite is a pegmatitic phase, varying from meta-anorthosite to anorthositic metanorite. A coarse ophitic intergrowth of little-granulated plagioclase crystals and hypersthene, both attaining lengths up to one foot, is characteristic of facies. Garnet rims may be seen around some of the hypersthene.
In Table 2 are given modes measured on the outcrop (numbers painted on outcrop and located on Fig. 2) covering 6.5 feet2 apiece (619 cm2 ) with reticular spacing of one inch (2.54 cm.) Means for each of the facies and a mean for all modes, which have been apportioned among the various facies proportional to their aerial extent, have been calculated. The anorthite content of a limited number of plagioclase samples, both megacrysts and the finer grained matrix, has been determined by refractive indices. The compositional range is from calcic andesine (An44) to sodic bytownite (An72) with the average of all determinations An53. Where both matrix and megacrysts were measured in a single sample, the composition was identical in each. It is likely, however, that many of the megacrysts show chatoyant core and a non-chatoyant rim.

STOP 2. -- Omitted --

STOP 3. Roadcut South of the Flume, Route 86
In this extensive exposure (for cross-section 835 feet long prepared from a photomosaic refer to Plate 3), the relationships between three distinctive anorthositic varieties are well displayed. Coarse-grained porphyroclastic meta-anorthosite to noritic meta-anorthosite (Facies 1) with blue-black plagioclase megacrysts composing from iO- 40% of the total rock flanked by a medium-grained, generally equigranular noritic meta-anorthosite to anorthositic meta-norite gneiss (Facies II) and a medium-grained, granoblastic anorthosite with mottled pale green and pink to lavender plagioclase (Facies III). For petrographic details, see Table 3. Despite the considerable compositional and textural variation, the anorthosite content of plagioclase remains remarkably constant {ca. An55) with the principle difference being the Fe-Ti oxide inclusions of the dark plagioclase megacrysts and the absence of impurities and characteristic coloration of the (recrystallized?) plagioclase of Facies III.
Facies I meta-anorthosite closely resembles massive core meta-anorthosite of the Marcy-type although here it appears to be isolated from any extensive exposed body of such meta-anorthosite. Facies II is most closely related to border facies (Whiteface-type) meta-anorthosite and Facies III which forms most of the gorge (Flume) along the Ausable River just to the north is found interlayered with noritic meta-anorthosite at numerous localities in the Whiteface sheet to the west.
The meta-anorthosite facies are numbered in the order of their presumed relative ages as shown at this exposure. Block structure with inclusions of Facies II noritic meta-anorthosite gneiss in the much more leucocratic Facies III is especially well developed 600 feet south of the northern end of the cut. The position of Facies I meta-anorthosite in the sequence is much less certain, and it is placed first largely because of the inclusion within Facies II near the 400 feet marker. Large masses of Facies II, however, are surrounded by Facies I between the 200 and 300 feet markers. There is thus some evidence of reciprocal intrusion if geometric factors are ignored. Another example is patches of Facies III meta-anorthosite surrounded by Facies II at 400 feet. Some discussion of field criteria for age relationships will undoubtedly be warranted. In general elsewhere in the eastern Adirondacks as described in the literature, it is more common to find gabbroic meta anorthosite intruding and enveloping blocks of a more leucocratic meta-anorthosite. At the next stop we shall examine further evidence bearing upon the anorthosite sequence.
There are small inclusions of diopsidic or garnet-biotite rich fieldspathic gneisses or granofelses in Facies III meta-anorthosite at 690 feet (specimen 66-56). More extensive layers of diopsidic metasediments in Facies II gabbroic meta-anorthosite are to be found 100 yards west of the bridge over the Flume just to the north.
The outcrop shows a number of fine-grained diabase dikes from 10 inches to 6 feet thick nearly parallel to the general trend of the cut (estimated mode, samples 62-70, Table 3).
Many shear surfaces of indeterminate displacement are present, the most prominent set perhaps being about N30E, parallel to the cut face and on strike with the pronounced linear through Wilmington Notch visible to the south, a locus of probably major faulting. Augen gneiss zones in the meta-anorthosite with considerable microclinization may be seen at 100 feet and at 320 feet (estimated mode, sample 62-72, Table 3). Garnet in the meta-anorthosite appears to be localized in these gneiss zones, a phenomenon observed at many other exposures. Many secondary minerals occur along the late shear surfaces, including calcite, quartz, epidote, and chlorite. Natrolite has also been identified.

STOP 4. Stream-worn slabs under lower ski lift, elev. 1800 - 2000 feet
Between powerhouse and mid-lift station.
Drive into Whiteface Ski Center from Route 86 between Wilmington and Lake Placid. The lift will probably not be operating, so climb ski trail 600 feet vertically right (north) of stream along lift line to bare stream slabs above powerhouse.
Three distinct facies of the meta-anorthosite series are represented at this exposure, two of them related to those seen at the Flume. The earliest member of the series (Facies 1) is not, and is preserved as several rounded inclusions mostly under running water in the stream bed as it veers north of the lift line towards the upper end of the exposure. It is a fine-to-medium-grained equigranular mafic anorthositic meta-gabbro enclosed by both Facies II and Facies III rocks. For thin-section mode see specimen 65-175 in Table 5. Notable is the calcic content of the plagioclase (An70) compared to that of Facies II (An52-55)'
Facies II comprises most of the outcrop. For thin-section modes, see Table 5,: for larger-area point counts with the screen employed at Stop 1, see Table 4 -- the numbers are painted on the outcrop. The average rock is a noritic-meta-anorthosite (color index 17.85) with mean per cent plagioclase megacrysts 24.25 and plagioclase matrix 57.80. The proportion of megacrysts varies from a minimum of 7.6% to a maximum of 42%. There is also considerable textural variation with a medium-grained rock showing subtle compositional banding and a suggestion of sub-ophitic texture in the matrix the preponderant type (modes, no. 1-10). Mineralogically similar, but coarser-grained and showing better developed ophitic texture is mode no. 11, whereas modes no. 13 and 14 are somewhat more leucocratic than the average but otherwise related texturally.
Facies III is an inequigranular mediumn-to-coarse-grained leuocratic meta-anorthosite apparently cutting Facies II noritic meta-anorthosite in irregular dikes with apophyses. It is interpreted as definitely younger than Facies II, and bears out the sequence deduced at the Flume. Similar dike-like bodies of Facies III in Facies II meta-anorthosite are present in slabs along the Boreen ski trail 100 feet higher to the northwest, and may be visited if time permits.
It is worthwhile inspecting some of the coarser-grained ophitic Facies II noritic meta-anorthosites in the lower narrow portion of the stream slabs for textural evidence of protoclasis or several stages of granulation followed by crystallization. Representative of the textures seen are large, partially granulated, plagioclase megacrysts with inserted ungranulated hypersthene crystals and shattered plagioclase augen veined ty noritic meta-anorthosite. Relationships may be explained by varying paths of crystallization in Di-Ab-An ternary coupled with one or more stages of cataclasis. Locally there appear to be eutectic intergrowths of plagioclase and hypersthene between plagioclase megacrysts.
Observations bearing upon the metamorphic history of the metaanorthosite at this locality are the following:
1. Garnet is generally absent except along shears. At the slabs in the Boreen ski trail a little higher, leucocratic meta-anorthosite "dikes" in gabbroic meta-anorthosite have garnet and clinopyroxene + hornblende rims to hypersthene grains whereas hypersthene does not have such reaction rims in the gabbroic meta-anorthosite.
2. Hypersthene generally is rimmed by clinopyroxene or horrnblende or an intergrowth of the two in the noritic meta-anorthosite under the lift. Locally, a hypersthene core is rimmed by clinopyroxene and this in turn by hornblende. It is possible that the clinopyroxene rim represents exsolution from a primary orthopyroxene or inverted pigeonite host. No exsolution lamellae have, however, yet been detected in the hypersthene. If the clinopyroxene is a result of unmixing, then the only metamorphic mineral here is hornblende.

STOP 5 (6, 7 ...) Whiteface Memorial Highway and summit
If time permits, we will ride up the Whiteface Memorial Highway, making one or more stops, and take one of the trails to the summit, preferably the northeast ridge trail from the "Wilmington turn" at the large cut below the main parking lot.
The meta-anorthosite rocks exposed in the Whiteface sheet extending from the upper slopes of Whiteface Mt. on the south to Catamount Mt. on the north and the Franklin Falls area on the west show many mineralogical, textural, and structural contrasts with the border facies of the meta-anorthosite we have thus far examined.
In general, they are much more recrystallized and relict igneous textures as observed under the ski lift at Stop 4 are rare. Foliation, and often lineation as well, is strongly developed and plagioclase megacrysts, mostly small and augen-shaped, seldom constitute more than a few per cent of the total rock. Banding is also common; and gabbroic meta-anorthosite alternates with leucocratic meta-anorthosite layers over short intervals. Garnet becomes a major phase and hypersthene a correspondingly less important constituent. There are layers of varying thickness from less than an inch to many tens of feet of mangeritic rocks, of Keene gneiss and of metasediments including coarse-grained gray quartzite and garnet-diopside granofels. Graphite is present locally near marble or calc-silicate contacts. I believe many of the physical and mineralogical characteristics of the Whiteface meta-anorthosite sheet can be explained by its tectonic position at the leading edge and base of the nappe described in the introduction to these notes.
Table 6 presents 20 modes of anorthosite rocks on Whiteface Mt. along the Memorial Highway and summit ridges in order of increasing elevation to emphasize any depth-controlled trends that may be present in the sheet. As we climb the northern slope of the Whiteface massif we are slowly passing upward through a nearly dipslope compositional layering parallel to a regional foliation.
At the Lake Placid turn (First switchback) there is a spectacular view of Lake Placid to the south. The contact between gabbroic meta-anorthosite, here somewhat more mafic than average, and mangeritic rocks is exposed just to the east of the turn. At the contact the mangerites are greenish but further away they become progressively pinker and quartz content increases. Boudins of anorthosite are enclosed in the mangerite-charnockite sequence -- is this an intrusive or tectonic relationship?
At the Wilmington turn, gabbroic meta-anorthosite structurally overlies green mangerite at the eastern end of the large cut. Meta-anorthosite blocks in the retaining wall excavated from the cut provide a good sample of the average rock in the cut. Garnet coronas are fairly common. On the upper, slightly weathered surfaces of the cut strong gently northeast-plunging lineation shown by aligned mafic minerals is shown to advantage. There are also thin quartzitic beds parallel to the foliation in the meta-anorthosite. One meta-anorthosite block not quite in place shows sharp folding of a quartzite layer.
Continuing up the trail along the northeast ridge of Whiteface Mt. to the summit, the open slabs will show the strongly gneissic, lineated, and banded character of the gabbroic meta-anorthosite. Thin plate-like quartzite layers parallel to foliation are common. From the summit, if you descend the south face 100 vertical feet you will cross the meta-anorthosite-mangerite contact once more. There is no intermediate andesine augen mesoperthite gneiss (Keene gneiss) at the boundary. Quartz content varies widely from 30-40 per cent to less than 5% in adjacent layers.
If the day is fine, it will be possible to point out regional relationships between anorthosite and related rocks in the High Peaks to the south and in the Jay-Whiteface sheet to the southeast and northwest.

J: SURFICIAL GEOLOGY OF THE INTERNATIONAL LEAD COMPANY MCINTYRE DEVELOPMENT AT TAHAWAS, N.Y.
Jesse L. Craft
Carleton University
Ottawa, Ontario

J: SURFICIAL GEOLOGY OF THE INTERNATIONAL LEAD COMPANY MCINTYRE DEVELOPMENT AT TAHAWAS, N.Y.

STOP 1. Deltaic sands, forset beds dipping west into valley wall
Deltaic sands, forset beds dipping west into valley wall. Delta built into Glacial Lake Warrensburg (Miller 1925).
Water seems to have carried material into the Valley from the Blue Ridge moraine which lies about 3 miles due west.

STOP 2 - Blue Ridge Moraine
This is a narrow moraine complex blocking off the east west valley. Outwash from this moraine can be traced into the deltaic deposits of the last stop. The north side has been modified by water flow from the north indicating ice occupying the valley to the W of this spot with the main N-S valleys free of ice.

STOP 3 - Outwash gravel and Kame deposits
Water was flowing out of Niagara Brook along the north side of the Blue Ridge Moraine into Glacial Lake Warrensburg.

STOP 4. Striated bed rock face
Striated bed rock face on Highway 128, 2 miles west of Newcomb. Just west of BM 1595 and Lodo Pond.
Which way was the ice flowing past this point?

STOP 5 - Tahawus, McIntyre Development, International Lead Co.
Excavation of the present pit area was started in 1961. In clearing the overburden from the area formerly under Sanford Lake, a multiple till section was exposed with interglacial lake sediments between two tills. Disseminated wood fragments including material identified as Pinus strobus (David Bierhorst, Dept. of Botany, Cornell Univ.) were collected by E. Muller and the section was described (Muller 1966). The wood fragments were dated at an age greater the 40,000 years (W-1520). Muller describes two tills separated by the interglacial lake deposits.
This author observed what appeared to be a third till when visiting the pit in 1966. Detailed measurement in the pit verified the existence of three till units separated by stratified sediments.
Section at Sanford Pit (as exposed in 1966)
Top
| Feet
Coarse sand and gravel, oxidized in zones - upper part mixed with excavation fill from Tahawas village | 2 - 5
Laminated sand, silt some gravel lenses, upper parts oxidized, well developed ripple marks cut and fill structures throughout, bedding dips 8°N. | 1 - 20
Till,yellow brown oxidized moderately stoney, non-calcareous very few ore pebbles. | 1 - 25
Sandy gravel, laminated sand and silt. Numerous small folds overturned to the north. In some places this layer has been so disturbed it becomes till like in texture. | 4
Till, gray, moderately stoney, non-calcareous few Potsdam pebbles observed, no ore pebbles. Contact with overlying sediments marked by thin silt bands. | 8 - 15
Sand, yellow brown oxidized medium to coarse changes to sandy gravel a short distance to the west. | 5 - 15
Contact with underlying laminated clay not observed. |
Clay, brown with few pebbles and disseminated wood fragments including material identified as Pinus strobus (David Bierhorst, Dept of Botany, Cornell Univ.) Age greater than 40,000 years (W-1520). | 3 - 12
Gravel stratified | 1
Till yellow grey moderately stoney, noncalcareous, oxidized | 5
Till, stoney, numerous ore pebbles folded silt, sand inclusion, shear planes dipping south | 1 - 30

Field Studies of
New Jersey Geology
And Guide to Field Trips:
52nd Annual Meeting of the New York State Geological Association
Warren Manspeiser, Editor
Field trips are numbered as follows:
GEOLOGIC TRAVERSE:
GEORGE WASHINGTON BRIDGE TO THE DELAWARE WATER GAP
1.Triassic and Jurassic Formations of the Newark Basin
Paul E. Olsen
2. PreCambrian Rocks of the New Jersey Highlands
John H. Puffer
3. Lower Paleozoic Carbonates: Great Valley
Frank J. Markewicz and Richard Dalton
4. Geology of the Ridge and Valley Province, Northwestern New Jersey and Eastern Pennsylvania
Jack B. Epstein
FOLD BELT
5. Alleghanian Thrust Faults in the Kittatinny Valley, New Jersey
Avery A. Drake Jr. and Peter T. Lyttle
COASTAL PLAIN
6. The New Jersey Coastal Plain and its Relationship with the Baltimore Canyon Trough
Richard K. Olsson
7. Coastal Dynamics and Environments on Sandy Hook, New Jersey
Norbert P. Psuty, Lindsay Nakashima, and George Theokritoff
8. Landscape Features and Bog Iron Ore Deposits of the New Jersey Pine Barrens
Emily W.B. Russel and Edward Krug
GLACIATION
9. Late Wisconsin-Holocene History of the Lower Hudson Region: New Evidence from the Hackensack and Hudson River Valleys
Stephen. P. Averill, Richard R. Pardi, WaIter S. Newman, and Robert J. Dineeli
ECONOMIC GEOLOGY
10. Economic Geology: New Jersey Highlands General Introduction and Road Log
Andreas H. Vassiliou
Uranium and Rare Earth Mineralization at the Bemco Mine Near Cranberry Lake, New Jersey
Iron Ore Deposits of the New Jersey Highlands
The Geologic Setting of the Sterling Hill Zinc-Iron-Manganese Deposit
Bob Metsger
ENVIRONMENTAL GEOLOGY
11. Environmental Geology: Hackensack Meadowlands
Sam L. Agron
12. Environmental Geologic Traverse.
Joseph A. Fischer
13. The Passaic River Flood Plain and Basin in New Jersey: Problems of Encroachment
Joseph S. Weisberg and John Marchisin
RIFT BASIN
14. Late Triassic Part of Newark Supergroup, Delaware River Section, West Central New Jersey
F.B. Van Houten
15. Brittle Faults (Ramapo Fault) and Phyllonitic Ductile Shear Zone in the Basement Rocks of the Ramapo Seismic Zone, New York
and New Jersey, and Their Relationship to Current Seismicity
Nicholas M. Ratcliffe
16. Rift Tectonics Inferred from Volcanic and Clastic Structures
Warren Manspeizer
17. Fossil Great Lakes of the Newark Supergroup in New Jersey

1: TRIASSIC AND JURASSIC FORMATIONS OF THE NEWARK BASIN
PAUL E. OLSEN
Bingham Laboratories, Department of Biology
Yale University, New Haven, Connecticut
Abstract
Newark Supergroup deposits of the Newark Basin (New York, New Jersey and Pennsylvania) are divided into nine formations called (from bottom up): Stockton Formation (maximum 1800 m); Lockatong Formation (maximum 1150 m); Passaic Formation (maximum 6000 m); Orange Mountain Basalt (maximum 200 m); Feltville Formation (maximum 600 m); Preakness Basalt (maximum + 300 m); Towaco Formation (maximum 340 m); Hook Mountain Basalt (maximum 110 m); and Boonton Formation (maximum + 500 m). Each formation is characterized by its own suite of rock types, the differences being especially obvious in the number, thickness, and nature of their gray and black sedimentary cycles (or lack thereof).
Fossils are abundant in the sedimentary formations of the Newark Basin and provide a means of correlating the sequence with other early Mesozoic areas. The Stockton, Lockatong, and most of the Passaic Formation are Late Triassic (?Middle and Late Carnian-Rhaetic) while the uppermost Passaic Formation (at least locally) and younger beds appear to be Early Jurassic (Hettangian and Sinemurian) in age. The distribution of kinds of fossils is intimately related to sequences of rock types in sedimentary cycles.
Far from being the consequence of the last gasps of the Appalachian Orogeny, Late Triassic and Early Jurassic Newark Supergroup basins formed in dynamic association with the opening of the Atlantic Ocean (Sanders, 1974; Van Houten 1977; Manspeizer, Puffer, and Cousminer, 1978; Olsen, 1978). In addition, Newark Supergroup rocks, once thought to be nearly barren of fossils, are now known to be exceptionally rich in organic remains (Thomson, 1979), replete with plants, invertebrates, and vertebrates spanning some 35 million years of the Early Mesozoic (Cornet, 1977). Finally, long episodes of unusually continuous deposition coupled with an abundance of laterally extensive stratigraphic "marker" beds (McLaughin, 1946), makes this deposit ideal for studying time-facies relationships and evolutionary phenomena. These recent discoveries have focused new interest on Newark strata.
The Newark Basin (Fig. 1 and 2) is the largest of the exposed divisions of the Newark Supergroup, covering about 7770 km2 and stretching 220 km along its long axis. The basin contains the thickest sedimentary sequence of any exposed Newark Supergroup basin and correspondingly covers the greatest continuous amount of time. Thus, the Newark Basin occupies a central position in the study of the Newark Supergroup as a whole.
In well over a century of study the strata of Newark Basin have received a relatively large amount of attention. By 1840, the basic map relations were worked out (Rogers, 1839, 1840, Cook, 1868) and by 1898, the major rock-stratigraphic subdivisions of the basin section were delimited and named (Darton, 1890; Kummel, 1897, 1898). Despite this long tradition, fundamental aspects of its historical and structural geology have remained essentially unexplored. The lithostratigraphy of the younger sediments, in particular, has received short shrift. Recently I have revised certain aspects of Newark Basin stratigraphy with an emphasis on the younger rocks (Olsen, in press). In the process I have proposed a number of new formational names (Table 2). Here I will review the formations of the Newark Basin and attempt to place their broader lithostratigraphic features into biostratigraphic context.

1: TRIASSIC AND JURASSIC FORMATIONS OF THE NEWARK BASIN

Begin Trip
To the east about one mile is the west portal of the George Washington Bridge, Fort Lee, New Jersey. The west abutments of the bridge rest on Stockton and Lockatong formations and Palisade Diabase. Roads along the east face of the Palisade Escarpment in the Fort Lee portion of Palisades Interstate Park have excellent exposures of nine individual detrital cycles of the lower Lockatong, each of which has been traced 15 km to the south (Olsen, this 1.7 Fieldbook). Three of these cycles are especially fossiliferous; the lowest of these (called cycle 6) has produced articulated remains of Semionotus brauni and disarticulated remains of the little reptile Tanytrochelos. The middle fossiliferous cycle (cycle 5) contains abundant disarticulated remains of Diplurus newarki and articulated remains of Turseodus. The upper cycle (cycle 2) has produced abundant articulated Turseodus and disarticulated large Diplurus. Clam shrimp (conchastracans) and ostracods are also common in cycles 5 and 2. These and other Lockatong cycles exposed here were deposited in shallower water than their more southern extensions.
In this area the trigonometrically computed thickness of both the Stockton Formation and the Lockatong Formation is less than 200 m. This is almost an order of magnitude thinner than the same formations along the Delaware River (Van Houten, this Fieldbook). While part of this thinning is due to the lateral replacement of Lockatong facies by Passaic Formation, most of the thinning is due to the thinning of individual cycles of the Lockatong Formation and thinning of the whole of the Stockton.
Numerous small, predominantly normal, faults striking north and northeast and down-dropping to the east characterize this portion of the Newark Basin. The reentrant in the Palisade Escarpment just south of here is an erosional result of some of the larger of these faults.

Cross large normal fault.
Crossing large normal fault cutting the Palisade Diabase and overlying the Lockatong Formation. This fault nearly doubles the outcrop width of the Palisade Diabase in this area. Just north of here the upper contact of the sill and the Lockatong is duplicated by this fault.
In marked contrast to faults is the northwestern portion of the Newark Basin, many of which have slickensides showing lateral (both synestral and dextral) movement, those examined to date in the area along the Palisades show only vertical slickensides (both those dropping down to the east and to the west) (personal observation and Manspeizer, pers. comm.).

Lockatong-Palisade Sill contact
Excellent outcrops of the Lockatong-Palisade Sill contact and overlying detrital cycles of the Lockatong. Here the upper surface of the Palisade Sill is smoothly concordant with the Lockatong. I believe the cycles exposed here tie in with those exposed in Granton Quarry to the south, although it is far from certain. Articulated Turseodus and conchostracans, at least, are common at this outcrop.
According to Van Houten (1969), these Lockatong hornfels include grossularite-andradite, prehnite. and diopside varieties.

Stockton Formation
Hill at this point is underlain by a tongue of Stockton Formation (Van Houten, 1969). Presumably this is the same unit exposed about 1 km. north of Granton Quarry. There good exposures reveal Stockton Formation with a thin bed of Synorichthys -bearing green and gray siltstone with overlying beds of gray-buff arkose containing what I interpret as very well-developed limestone caliche paleosols. Tongues of Stockton such as this may correspond to clusters of chemical cycles prevalent in similar positions in the central Newark Basin.

Approximate contact with Passaic Formation.
Lowermost Passaic is very poorly exposed in the vicinity of Ridgefield and consists of mottled red-buff feldspathic sandstone and red siltstone.

Hackensack Meadows.
Broad belt of relatively soft red siltstone and minor gray siltstone and arkose correlating with upper Lockatong and lower Passaic Formation of Delaware River area (Van Houten, this Fieldbook).

Section A of Passaic type section begins here
Beginning of the type section of the Passaic Formation (see Table 2, fig. 4. this paper) (Olsen, In Press). The type section of the Passaic consists of intermittent exposures along Route 80. These exposures show interbedded red feldspathic sandstone and siltstone with small-to-large-scale cross-bedding, abundant bioturbation structures (including roots and Scoyenia) and some beds of caliche. Section A (fig. 4) of the type section begins here.
2011: Much of the outcrop has been obscured by sound barriers, probably constructed after 1980.

Section B of the type section of the Passaic Formation.
2011: Much of the outcrop has been obscured by sound barriers, probably constructed after 1980.

Section C of the type section of the Passaic Formation.

Section D of the type section of the Passaic Formation.

Garrett Mountain on Left, Passaic Falls on Right
Garrett Mountain is visible on left (south), Passaic Falls is on the right (north). The upper Passaic Formation of Rhaetic age (latest Triassic) has produced near here a series of well preserved skeletons of the highly specialized procolophonid reptile Hypsognathus (Colbert, 1946). About one skeleton or skull is found per decade.
Just south of this point, along Route 20 are exposures of Passaic Formation red conglomerates. The frequency of beds such as these increase to the northeast and decrease to the southwest. These conglomerate beds are crucial to tests of the "Broad Terrain Hypothesis" (Sanders, 1963, 1974). Cross beds consistently yield paleocurrent directions indicating transport from northeast to southwest (personal observation and Manspeizer, pers. comm.) in line with the mean paleocurrent vector for this portion of the Passaic Formation. Clasts consist primarily of Paleozoic sedimentary rocks, including quartzite, quartzite conglomerate, limestone, and minor phyllite. Such rocks are not known to be present to the east of the Newark Basin. Clast composition is very similar to beds found in the northernmost part of the Newark Basin, beds thought to have a northwestern provenance. The clasts are very different from those of the contemporary New Haven Arkose of the Hartford Basin. The "Broad Terrain
Hypothesis" predicts that these beds of the Passaic should be western equivalents of the New Haven Arkose. Two alternative explanations come to mind.
1. The provenance of these Passaic conglomerates was to the east of the Newark Basin; presumably these source rocks are completely eroded. Either the Newark and Hartford Basins were with the Paleozoic sedimentary rocks intervening or the Paleozoic rocks were exposed to the east of a southern continuation of the Hartford Basin and contributed to New Haven Arkose bed no longer exposed.
2. The provenance of these Passaic conglomerates was to the west or north but the sediments were redeposited by southwest moving streams.
Detailed studies of these conglomerates are clearly needed.

Contact of Passaic Formation with overlying Orange Mountain Basalt
Contact of Passaic Formation with overlying Orange Mountain Basalt on left (south). This is section E of the type section of the Passaic Formation (fig. 7). A series of faults cut the ridge made up of Orange Mountain Basalt here; some of these faults are visible in the cut on the left, just west of the Passaic-Orange Mountain contact.
Uppermost few meters of Passaic Formation, exposed to the south of here (Montclair State College) has produced a reptile footprint assemblage consisting of a mixture of taxa common to older beds of the Passaic and younger beds of the Feltville, Towaco, and Boonton Formations. The oldest North American occurences of Batrachopus, and grullatorid footprints of the Anchisauripus minuscolus- type have been discovered at this locality (Olsen and Galton, 1977).
This assemblage is nearly identical to a suite of footprints found in the Rhaeto-Liassic of France. It is unclear whether these uppermost Passaic beds are latest Triassic or earliest Jurassic (the French workers are unsure of their footprint bearing beds, as well); The Triassic-Jurassic boundary probably lies within a few meters of the Orange Mountain in the Route 80 area.

Exposures of Orange Mountain Basalt.
Upper flow units of Orange Mountain Basalt are exposed in quarries near here. A diverse suite of zeolite minerals has made some of these quarries famous (Manspeizer, this Fieldbook; Van Houten, 1969).

Crossing the Passaic River
Crossing the Passaic River, which here follows the Feltville-Orange Mountain Basalt contact.
The Feltville Formation is very poorly exposed in this area; the lower Feltville is not exposed at all. Exposures in bluffs just north and south of here consist of gray and buff arkose and sandstone, often cross-bedded and containing coalified plant remains, and red feidspathic siltstone and sandstone with roots and reptile footprints.

Position of Preakness Basalt: not exposed.
A confluence of a series of faults, densely spaced joint systems, and the low dip of the bedding are probably responsible for the low profile of the Preakness Basalt in this area. The outcrops of the main lower flow in this area (such as along Route 46 to the south) show the flow's characteristic splintery joint pattern.

Approximate position of Preakness Basalt - Towaco Formation contact.
The large outcrop width of Towaco Formation here is due to the Hook Mountain Anticline. Toward the west, along the axis of the anticline, the dip of the Towaco Formation steadily decreases.

Reptile footprints to North
About 4.4 miles north is the abandoned Vreeland Quarry which produced the superb reptile footprints on display at the Rutgers University Geological Museum. Just to the northeast is Tom's Point, an area which produced hundreds of reptile footprints in the 1960's. Exposures still extant include much of the non-red portion of the second-from-the-top Towaco Formation cycle. Exposures of the upper two Towaco Formation cycles occur sporadically in surrounding areas.

Type section of Hook Mountain Basalt.
Two flows and the contact between them are exposed along the highway (fig. 11). The entablature and lower colonnade of the lower flow are exposed on Hook Mountain Road just north of the Route 80 overpass.

Approximate position of Boonton-Hook Mountain Basalt contact.

The Boonton Formation is not exposed along Route 80.
The Boonton Formation is not exposed along Route 80 but 2 miles to the north are the excellent exposures along the Rockaway River (fig. 12). These exposures begin at the dam at the north end of Boonton (Jersey City) Reservoir and extend for over 1 mile along the river bluffs. The dam footing rests on the Boonton Fish Bed which during the 1800's and early 1900's produced thousands of fish of the "Semionotus elegans group," Redfieldius spp., several specimens of the large coelacanth Diplurus longicaudadus, and a single specimen of Ptycholepis.
Only the underlying beds are exposed now, by these beds produce abundant plant remains and reptile footprints.

Approximate position of the Ramapo Fault: end of the Newark Basin.
A prominent bluff of metamorphics marks the west wall of the fault (see Ratcliffe, this Fieldbook).

2: PRECAMBRIAN ROCKS OF THE
NEW JERSEY HIGHLANDS
JOHN H. PUFFER
Department of Geological Sciences
Rutgers University Newark, New Jersey
Rocks exposed along Route 15 offer an excellent opportunity to observe most of the major metamorphic and igneous units that make up the New Jersey Highlands (Fig. 1). Rock is exposed along almost the entire twenty kilometers of Route 15 that traverse the strike of the rock units. The purpose of this field guide is to describe the rock units exposed along Route 15 and to report on the current status of recent efforts aimed at understanding the metamorphic and igneous environments that formed the rocks,
Most early descriptions of the New Jersey Highlands subdivide the Precambrian into four major units: These four units appear on the legend of Lewis and Kummel's (1910-1912) Geologic Map of New Jersey as:
1. Byram Gneiss "Gray granitoid gneiss composed of microcline, micro-perthite, quartz, hornblende or pyroxene, and sometimes mica".
2. Losee Gneiss "White granitoid gneiss composed of oligoclase, quartz, and occasionally orthoclase, pyroxene, hornblende, and biotite".
3. Pochuck Gneiss "Dark granular gneiss composed of pyroxene, hornblende, oligoclase, and magnetite".
4. Franklin Limestone "Coarse white marble..."
More recent works by Hotz (1952), Sims (1958), Drake (1969), Smith. (1969), and Baker and Buddington (1970) have subdivided the Byram Gneiss into a "Hornblende Granite" and a "Pyroxene Granite" and a few minor units; have substituted rock names such as "Quartz-Oligoclase Gneiss" and. "Hypersthene-Quartz-Oligoclase Gneiss" for portions of the Losee Gneiss; have subdivided the Pochuck Gneiss into "Amphibolite" and "Pyroxene Gneiss"; and have recognized several additional rock units such as "Quartz-Potassium Feldspar Gneiss and "Syenite Gneiss". Widmer (1964) has recognized twenty-four mappable Precambrian rock units in the New Jersey Highlands including marble, quartzite, skarn, pegmatite, quartz diorite, four kinds of granite, and fifteen kinds of gneiss. Because of the general reconnaissance nature of this field trip only the major units among the complex assortment of Highlands rock types will be described in this report.

2: PRECAMBRIAN ROCKS OF THE
NEW JERSEY HIGHLANDS

STOP 1. Hornblende Granite (sample 0.9, Table 3).
Exit at the Picatinny Arsenal. The rock exposed along the hill to the right is Hornblende Granite. Exercise extreme caution when crossing the road to examine the granite. The granite here is quite homogeneous but on the other side of the hill contains less hornblende and becomes an alaskite. Note the well developed foliation.

Green Pond Fault.

Green Pond Conglomerate
Green Pond Conglomerate; silurian correlative of Shawangunk Conglomerate. Most of the pebbles are rounded milky quartz.

Very complex mixture of Pyroxene Granite
Very complex mixture of Pyroxene Granite near the south
end of the roadcut (sample 3.6, Table 3). Quartz-Oligoclase Gneiss near the center, and Hornblende Granite near the north end (4.0 mile on log). Several disconnected xenoliths of amphibolite may be observed in the granite as well as numerous granite pegmatites emplaced parallel to the foliation of the granite.

Amphibolite (sample 4.3, Table 3).

Fine grained quartz monzonite alaskite and Amphibolite
Fine grained quartz monzonite alaskite along end of roadcut; Amphibolite along the north end.

Pyroxene Granite (sample 5.9, Table 3).

STOP 2. Pyroxene Granite.
Note the wide ranging quartz content, dark color, and well developed foliation. The pyroxene component of the rock here is deeply altered; the feldspar component ranges from a plagioclase rich perthite (as in sample 5.9, Table 3) to a K-spar rich antiperthite (as in sample 6.6, Table 3). Busses will park on breakdown lane. Watch out for loose rock on vertical face of road cut.

Pyroxene Gneiss
Pyroxene Gneiss composed of approximately 50 percent antiperthite, 10 percent plagioclase, 15 percent quartz, 20 percent pyroxene-amphibole intergrowths, and 5 percent opaque oxides.

Pyroxene Granite

Pyroxene Syenite (sample 8.2, Table 3).

Pyroxene Granite
Pyroxene Granite including bands of syenite and various gneisses that have a similar general appearance but dissimilar mineralogies making up a virtually unmappable complex for 0.3 mile. Amphibolite bands are also found here.

STOP 3. Syenite Gneiss (sample 8.7, Table 3).

STOP 4. Quartz-Oligoclase Gneiss, (samples 9.1a and b, Table 3).
STOP 4. Quartz-Oligoclase Gneiss, (samples 9.1a and b, Table 3). Both white and pink varieties of Quartz-Oligoclase Gneiss occur here. Most of the rock here contains less biotite and is less foliated and banded than more typical Quartz-Oligoclase Gneiss. Amphibolite schliern are common. Busses park on abandoned entrance road to Route 15.

Amphibolite.

Quartz-Oligoclase Gneiss

Amphibolite

Hornblende Granite.
Hornblende Granite. Alternating plagioclase rich and
K-spar rich bands make this rock less homogeneous than
the granite at STOP 1.

Kittatinny Limestone. Cambro-Ordovician dolomitic limestone.

Hornblende Granite

Granodiorite Gneiss.
Highly foliated rock composed of 40 percent plagioclase, 30 percent quartz, 20 percent K-Spar, and 10 percent biotite.

STOP S. Franklin Marble.
The marble is intruded by granite pegmatites. If traffic is heavy it may be necessary to skip this stop. The road shoulder is quite narrow.

3: LOWER PALEOZOIC CARBONATES:
GREAT VALLEY
Frank J. Markewicz and Richard Dalton
New Jersey Department of Environmental Protection
Division of Water Resources, Trenton, New Jersey
The purpose of this field trip is to demonstrate the subdivision of the Cambro-Ordovician carbonate sequence as proposed by the field trip leaders. In addition, there will be discussions on environmental, hydrogeologic, and engineering problems in these carbonates and how this subdivision has "opened the doors" in understanding how everyday problems from man's activities can affect or be affected by certain lithic units within the carbonate sequence. This understanding of the interaction between man's activities and how it might affect or be affected by critical aquifers, thin or thick soil horizons, and specific lithologies by septic waste loads, ground water pollution, building foundation loading, landfills, etc., has become extremely important in the land development process.
We anticipate this field trip will not only relate the carbonate subdivision but will point out how important this breakdown is to applied geology.

3: LOWER PALEOZOIC CARBONATES:
GREAT VALLEY

STOP 1. Limeport member of the Allentown Formation.
Geologic Setting
Although less than 20 feet is exposed here it contains many of the sedimentary features found in the member.
In the Pequest Valley the highest stratigraphic rocks found by Markewicz and Dalton include units from Leithsville through the middle part of the Upper Allentown. Stop 1 is considered to be in the lower half of the Limeport Member.
The southeastern edge of the valley is underlain by a normal section of "Kittatinny" sediments lying above the Precambrian.
Along the southwestern border of the valley there are complex structural relationships just before the point where Route 80 enters the Jenny Jump Mountain Precambrian units. There have been various interpretations for this contact between the Precambrian and Paleozoic. These include nappe theories, normal contacts, and various fault interpretations such as an unrooted thrust block.
The Leithsville and Lower Allentown (Limeport) typically form a topographic lowland on the eastern border of the valleys in northern New Jersey. Leithsville rocks generally underlie the lowlands or river valleys and have a greater thickness of unconsolidated sediments -sand, gravel, clay, etc. overlying bedrock than any of the other formations of the "Kittatinny group." The Limeport, typically more resistant than the Leithsville forms a slighty higher pronounced bench. It is generally overlain by overburden that is thinner than the underlying Leithsville overburden, but thicker than overburden Upper Allentown.
Geologic Features
(a) algal units
(b) oolitic and local pisolitic units
(c) churned, lumpy, patchy bioturbidite facies
(d) intraformational conglomerate facies
(e) sandy facies
(f) ruditic, patchy textured clast conglomerate
(g) various dolomite facies, from dolomitic mudstones to medium coarse crystalline dolomite grainstone.
Many varied shallow water carbonate environments can be found at this stop. This is the type of outcrop that a geology professor likes to take his students to so that they can observe the many features that they hear about in the classroom.

Diabase dike within metasedimentary calc-silicates and various gneisses.

STOP 2. Harmonyvale Member of the Ontelaunee Formation
Geologic Setting
This is the first exposure of dolomite on the west side of Jenny Jump Mountain.
During the construction of Rt. 80 the Jacksonburg Limestone was exposed at the east end of the exposute. On the west side of Jenny Jump, the first rock exposed is always the Jacksonburg along with the uppermost part of the Kittatinny sequence.
At Stop 2 exposures of the uppermost-lower Ordovician dolomite present in New Jersey can be observed; this is the Harmonyvale member of the Ontelaunee Formation.
Geologic, Features
(a) dark to black wispy lines or streaks
(b) medium crystalline fetid beds
(c) massive paleo-solution breccia with silt (paleokast feature)
(d) possible fossils
(e) recent karst features
Black wispy lines are an important feature to be noted here. These seem to have been formed through some deformation process shortly after deposition of the dolomite since the Jacksonburg conglomerates in this region contain dolomite cobbles which have the wispy lines.

Exposures of the upper part of the Allentown Formation

STOP 3. The Rickenbach and Epler Formations
This series of exposures which starts in the upper Allentown Formation and extends up to the Lafayette Member of the Epler forms one of the most complete sections in this area. Off the road, the section continues up into the Jacksonburg Limestone. We will be limiting discussion to the Rickenbach and Epler Formations at this stop.
A. The Rickenbach Formation at this locality measures approximately 290 feet and both the lower and the Hope Members are present. This stop is also the type section for the Hope Member. The features to note are:
a) compare lithologies of the lower member with the Hope Member. .
b) clots of black botryoidal hydrocarbon? material -anthrazalite?
c) sand in the dark aphanitic beds
d) the "7 cherts" horizon
e) the upper chert horizon
f) algal structures
g) Trace amounts of sphalerite occur over a stratigraphic thickness of 225 feet.
B. The Epler at this stop has complete sections of the Branchville and Big Springs Members and a partial section of Lafayette Member. The features to note in the Epler are:
a) compare the alternating medium to massive bedded sequence of the Hope Member of the Rickenbach with very massive bedded laminated dolomites of the Branchville Member of the Epler.
b) the similarity Member of the Branchville with the Lafayette
c) note the siliceous ribbing (interbeds) as well as distinctive reddish weathering characteristic of dolomite.
d) the paleo-solution breccia in the Lafayette Member
e) fossils found in the Big Springs Member.

STOP 4. Rickenbach Formation
From Stop 3 the highway cuts across the Jacksonburg and the Martinsburg Formations west of Route 521. As the highway ascends the large hill known as Mt. Herman a west dipping thrust fault is crossed. The first dolomite exposure is the Limeport Member of the Allentown Formation.
The west side of Mt. Herman is also bounded by a fault. This fault, based upon preliminary mapping is high angle.
Geologic Features
a) the changes in dip
b) the large amount of sulphides present in the rock

4: GEOLOGY OF THE RIDGE AND VALLEY PROVINCE, NORTHWESTERN NEW JERSEY AND EASTERN PENNSYLVANIA
JACK B. EPSTEIN
U. S. Geological Survey
Reston, Va. 22092
The rocks seen in this segment of the field trip range in age from Middle Ordovician to Middle Devonian and constitute a deep basin-continental-shallow shelf succession. Within this succession, three lithotectonic units, or sequences of rock that were deformed semi-independently of each other, have somewhat different structural characteristics. Both the Alleghenian and Taconic orogenies have left their imprint on the rocks. Wind and water gaps are structurally controlled, thus placing doubt upon the hypothesis of regional super-position. Wisconsinan deposits and erosion effects are common. We will examine these geologic features as well as some of the economic deposits in the area.
Figure 1 is an index map of the field-trip area, showing the trip route and quadrangle coverage. Figure 2 is a generalized geologic map,

4: GEOLOGY OF THE RIDGE AND VALLEY PROVINCE, NORTHWESTERN NEW JERSEY AND EASTERN PENNSYLVANIA

Allentown Dolomite in the Hope klippe
Gently dipping Allentown Dolomite in the Hope klippe (see Drake and Lyttle, this volume).

Dolomite and cherty dolomite in the Allentown (?) Dolomite.

Small anticline in the Allentown (?) Dolomite.

Graywacke and slate in the Ramseyburg Member, Martinsburg Fm
Graywacke and slate in the Ramseyburg Member of the Martinsburg Formation. We have just crossed a major fault separating the Middle and Upper Ordovician Martinsburg from Cambrian carbonate rocks in the Hope klippe. <br

Kittatinny Mountain to the right
Kittatinny Mountain to the right (north) held up by quartzites in the Silurian Shawangunk Formation. The mountain is offset to the northeast by a syncline-anticline couplet near the site of the Yards Creek Pumped Storage Project north of Blairstown, N.J.

STOP 1. Discussion Of Trip And Lunch.
See Fig. 4 for stop description. After leaving Stop 1, we will travel down the Paulins Kill Valley, across the Delaware River, travel to the southwest to Pen Argyl, Pa., and stop at a slate quarry in the upper (Pen Argyl) member of the Martinsburg Formation. After crossing Blue Mountain at Wind Gap, we will visit a quarry at Bossardsville. Pa., in Silurian rocks. We will than attempt to drive to the top of Kittatinny Mountain to a vantage point overlooking Delaware Water Gap and examine the Shawangunk Formation and Bloomsburg Red Beds. After passing through the gap we will return to Newark, N.J.

Laminated slates of the Bushkill Member, Martinsburg Fm
Laminated slates of the Bushkill Member of the Martinsburg Formation. Note the typical fine bedding in this member. You will not see similar laminations in slate of its Pen Argyl Member. This is one of the characteristics distinguishing the two predominantly slate-bearing members of the tripartite Martinsburg Formation.

Paulins Kill to right.

Southeast-dipping dolomite of the Epler Formation.
We have crossed the Portland fault which separates the Epler from the Bushkill Member of the Martinsburg Formation.

Crossing Delaware River.
View of Delaware Water Gap to right (north). Tuscarora Power Plant smokestacks to left.

Toll Booth.
Continue straight ahead on U.S. 611S. We will be driving on the Richenbach Dolomite of the Beekmantown Group for about O.5 mile (0.8 km) and then on Wisconsinan kame deposits and till.

View of Kittatinny Mountain to right.

Wisconsinan sand and gravel and some till
The lowlands to the right are mostly underlain by Wisconsinan sand and gravel and some till.

Five Points. Thick glacial deposits
Glacial deposits are as much as 178 feet (54 m) thick in this area.

Graywacke and slates of the Ramseyburg Member, Martinsburg Fm
Crest of hill underlain by graywacke and slates of the Ramseyburg Member of the Martinsburg Formation. Note slate dumps ahead.

Slate dumps of the abandoned Capitol Slate quarry on right.
Slate dumps of the abandoned Capitol Slate quarry on right. Note the much thicker beds than in the Bushkill Member of the Martinsburg seen at mileage 7.4. We are in a slate "run" in the upper part of its Ramseyburg Member. Graywackes are found higher in the sequence and the contact with its overlying Pen Argyl Member is placed where graywacke beds become less dominant.

Flooded New Bangor and Columbia Bangor quarries on left
Flooded New Bangor and Columbia Bangor quarries on left, with nearly recumbent folds.

The Bangor Excelsior quarry on the left has been filled in
The Bangor Excelsior quarry on the left has been filled in, partly with fly ash. It was at least 140 (43 m) feet deep.

Pennsylvania Historical and Museum Commission sign
Pennsylvania Historical and Museum Commission sign on right: "Slate Industry - Robert M. Jones of Wales, who U.S. came here in 1848 as an immigrant, began the slate quarrying industry. The region became a major world center for slate. From here came slate roofs and old-time school slates and pencils."
To the right of the sign are the remains of an old kiln that used to fire the slate for lightweight aggregate (see Epstein, 1974a, for a discussion of the slate industry and potential uses for waste slate).

The Old Bangor slate quarry is over the dumps to the left.
The nearly flat Old Bangor syncline is exposed in the quarry and can be traced for several miles in the area. The quarry also lends its name to the "Old Bangor run", a series of beds that include important commercial slate beds.

Crest of Wisconsinan terminal moraine.
Poor exposures of till may be seen in cuts to the right.

Wisconsinan till to east and Illinoian(?) till to west.
Contact between the Wisconsinan till to east and Illinoian(?) till to west. Note slate dumps from quarry in the Pen Argyl Member of the Martinsburg Formation straight ahead.

STOP 2. Stephans Jackson Slate Quarry
Stephans Jackson Slate Quarry; Structure And Stratigraphy Of The Martinsburg Formation; Slaty Cleavage; Quarrying Operation.
DANGER-STEEP QUARRY WALLS, DO NOT BE TOO BOLD!
The Stephans Jackson Slate Quarry is one of only a few that remain active in the slate belt of Pennsylvania which extends for about 45 miles (72 km) west of the Delaware River. The belt is dotted with more than 400 abandoned slate quarries and prospects. The quarry is currently about 350 feet (110 m) deep. Quarrying and milling methods have changed little for the last 50 years, and are still much the same as described by Behre (1933). The slate is used for roofing, blackboards, flagging, aquaria bottoms, sills and treads, and billiard table tops. Immediately southwest over the dumps is the abandoned Parsons quarry. which reportedly was more than 900 feet (274 m) deep, the deepest slate quarry in the United States.
The Stephans Jackson Slate Quarry is in an overturned syncline whose axial plane dips gently to the southeast (fig. 5). A bedding-slip fault forms much of the northwest wall of the quarry. Slaty cleavage and bedding in the overiding block are dragged into the fault and a slip cleavage that shows antithetic movement to the fault, has developed in the drag fold (see inset, fig. 5). In general, slaty cleavage forms a gentle arch and fans the fold by about 14°. The fault is marked by a gouge or "spar zone" that is as much as 2 feet thick and filled with quartz and calcite.
The fault zone is a marked zone of weakness in the rock. In 1948, the northeast section of the quarry was being worked when a large mass of rock slipped down into the quarry along the zone, killing two workers below. That part of the quarry was abandoned, and the presently active section was started. Note the pins that were bent by the sliding mass in the northern corner.
The sequence of deformation was complex. Bedding-plane slickensides that are offset by cleavage indicate that initial flexural-slip folding was followed by passive folding (fig. 46, Epstein and Epstein, 1969). As the folds continued to tighten, failure was again along bedding, producing the bedding-slip fault, warping of slaty cleavage, and formation of crenulation cleavage parallel to the axial plane of the cleavage fold. Movement along the bedding-slip fault was up to the northwest, as indicated by the drag, but steps on one of two slickensided surfaces in the fault zone indicate an opposite sense of movement, perhaps due to earlier flexural slip.
The origin of slaty cleavage in the Martinsburg Formation, as well as in rocks above and below, has been a focus of considerable attention during the last two decades. Did it form by tectonic dewatering or did it form under conditions of low-grade metamorphism? Mapped relationships and petrologic considerations led me to conclude that it formed as a product of metamorphism (Epstein, 1974b) by a combination of the following processes: mechanical rotation of detrital grains parallel to the cleavage, corrosion of quartz by pressure solution and migration of silica. intrusion and flow of pelitic material, grain diminution by granulation, and by recrystallization and neocrystallization.
The Stephans Jackson Slate Quarry is in the Pen Argyl Member (upper) of the Martinsburg Formation and is about 1500 feet (457 m) above the contact with its Ramseyburg Member (middle) (fig. 6). The Pen Argyl is typically thick bedded, containing some beds of gray slate more than 10 feet (3 m) thick. The member is cyclically bedded, each cycle consisting of medium-gray slate grading up into grayish-black carbonaceous slate. Graywacke may form the base of some of the cycles.
For more than 70 years there has been controversy regarding the number of members in the Martinsburg (see Drake and Epstein, 1967). On the basis of the very characteristic difference in bedding thickness between the lower (Bushkill) and upper (Pen Argyl) members, and as proved by detailed mapping (fig. 6), I have mapped three members in this area, nearly in the same manner as Behre (1933). The Pen Argyl cannot be the Bushkill repeated by folding as earlier suggested by Stose (1930), for example. Recently, Stephens and others (1979) argued for a two-fold division based on fossil collections in the Schoharie "Ridge' area, about 35 miles (56 km) to the southwest. This bipartite interpretation, however, is presently clouded by structural complications that may be present in that area (Epstein and others, 1972; Lyttle, 1979).

Gentle slopes underlain by colluvium and Illinoian(?) till
We will be riding on gentle slopes underlain by colluvium and Illinoian(?) till which cover the Pen Argyl Member of the Martinsburg. Quartzites in the Shawangunk Formation are seen in cliffs in Blue Mountain to the right.

The low col straight ahead is Wind Gap
Exposures of the lower (Minsi) member of the Shawangunk Formation in woods on left. The low col straight ahead is Wind Gap, underlain by nearly vertical quartzites and veneered with weathered colluvium.

Red shale, siltstone, and sandstone of the Bloomsburg Red Beds.
For about 1.5 miles (2.4 km) along Pa. 33, the Bloomsburg is thrown into many small folds that are superimposed on the Ross Common Creek syncline and Wind Gap anticline. Note the well-developed cleavage in the Bloomsburg.

Chestnut Ridge to the left
Chestnut Ridge to the left, underlain by complexly folded rocks of Late Silurian and Early Devonian age.

Bloomsburg Red Beds to right.
Cherry Ridge straight ahead held up by sandstones in the Ridgeley and Palmerton Sandstones.

Wisconsinan till in road cut to right.

Cut through Cherry Ridge
Cut through Cherry Ridge in South-dipping overturned Esopus and Schoharie Formations and Palmerton Sandstones.

Many abandoned clay pits
Many abandoned clay pits in deeply weathered Buttermilk Falls Limestone are in woods to right. These are in saprolites as much as 250 feet (76 m) deep. The clay is used as whitener in cement.

Panoramic view to left (see fig. 7).

Hill to right underlain by Decker Formation and Bossardville Limestone.

STOP 3. Hamilton Stone Company Quarry.
Stratigraphy And Structure Of Upper Silurian Rocks In Cherry Ridge.
Three Upper Silurian units are well exposed in the quarry in a series of upright to tight and slightly overturned folds (fig. 8). The units are, from top to bottom:
Wallpack Center Member of the Decker Formation:
Medium-bedded and lenticular medium.gray to medium-light-gray, fine-to coarse-grained, quartzose limestone, medium-gray, fine-to coarse-grained calcareous sandstone, siltstone, and conglomeratic sandstone, containing brachiopods, rugose and colonial corals, bryozoans, and crinoid columnals. Leperditiid ostracodes are abundant near basal mud-cracked dolomite. Upper contact concealed. About 70 feet (21 m) exposed. Forms cap rock. Useful for crushed stone.
Bossardville Limestone:
Graded laminated to very thin-bedded, dark-gray, fine-to very fine grained pyritic argillaceous mud-cracked limestone with scour-and-fill at base of graded units and leperditiid ostracodes. Uppermost beds very finely laminated limestone and smaller amounts of dolomite. About 95 feet (29 m) thick. Quarry rock useful for crushed stone.
Poxono Island Formation:
Interbedded and interlaminated medium-gray, calcareous dolomite, medium-gray and mottled pinkish-gray-green to medium-greenish-gray to gray, very fine grained dolomite, grayish-red limestone, and light-grayish-yellow-green shale and calcareous shale; contains several mud-crack intervals. Uppermost dolomite contains color contortions. About 40 feet (12 m) exposed.
These rocks are interpreted to have been deposited in a complex and generally transgressive tidal-flat barrier-bar shallow subtidal environment on the basis of lithology, sedimentary structures, texture, bedding characteristics, fossils, and lateral facies (see Epstein and others, 1967, and Epstein and Epstein, 1969, p. 192-196).
The structure in the quarry area is dominated by about 25 folds whose axial planes strike N. 50° - 60° E. and whose axes plunge about 5°SW. These folds are disharmonic on the Kemmererville anticline in the Bloomsburg Red Beds in the underlying lithotectonic unit. The Poxono Island Formation is believed to be separated from the Bloomsburg by a decollement (see cross section, fig. 8). The anticlinal ridge underlain by the Bloomsburg rises as we travel to the northeast after leaving the quarry.
Folding was initiated by flexural slip followed by passive folding and development of cleavage. This is indicated by cleavage that wrinkles bedding-plane slickensides. In a few places, such as in the 10 foot-(3 m) wide fault zone in the east corner of the quarry, a slip cleavage cuts the earlier cleavage.
The stratigraphic units behaved differently during deformation. The more pelitic rocks failed passively, with development of prominent cleavage, whereas the more competent carbonate rocks and sandstones in the Decker and the Bossardville were concentrically folded and in places formed fold mullions. This small-scale folding is somewhat disharmonic and folds in the Poxono Island are generally tighter than in overlying rocks. This disharmonic folding is similar to the structure on a regional scale.
Places that we may visit in the quarry depend on the whims of the shovel, but we will probably go to three localities shown in figure 8: (A) A very tight anticline in the Poxono Island Formation and a fault that cuts out about 50 feet (15 m) of the Bossardville Limestone are conspicuous in outcrop here (fig. 9). As we look to the west from a high point we can see the Trimmers Rock and Catskill Formations in the southwest-plunging Weir Mountain syncline. To the north, the Pocono Plateau, Godfrey Ridge, and glacial lake deposits are seen. A well-developed ice-contact delta and esker marks a recessional position of the Wisconsinan glacier and the northeastern ice-defended boundary of glacial Lake Sciota. (B) Fold mullions and many sedimentary features are present in the Decker Formation in this overturned syncline. (C) Well-developed mudcracks, edgewise conglomerate, and other structures suggestive of supratidal deposition are of interest in the Poxono Island Formation. Cleavage that warps bedding slickensides is common in the Bossardville.

Abandoned quarries in the Bossardville Limestone to right and left.

View to right of Cherry Valley; Godfrey Ridge on left;
View to right of Cherry Valley; Godfrey Ridge on left; rounded ridge in the middleground is underlain by the Bloomsburg Red Beds in the southwest-plunging Kemmererville anticline; northwest-dipping quartzites in the Shawangunk Formation hold up Kittatinny Mountain on the skyline.

Poxono Island Formation exposed in creek to right.

Near-vertical Bossardville Limestone on left.

Flat floor underlain by glacial lake clays, etc.
Flat floor of Cherry Valley on right partly underlain by glacial lake clays, silts, and sands. Kittatinny Mountain forms skyline to right.

Stormville Member of the Coeymans Fm
Village of Stormville, type locality of the Stormville Member of the Coeymans Formation.

Whiteport Dolomite Member of the Rondout Fm
Very well developed columnar mud cracks in the Whiteport Dolomite Member of the Rondout Formation on left.

Kame ahead.
Low hill ahead is a kame containing Wisconsinan sand and gravel.

Coeymans Formation on left in slump block.

Ridgeley Sandstone in float on left.
Ridgeley Sandstone, which caps Godfrey Ridge, in float on left.

The Bloomsburg Red Beds in Kemmererville anticline to right rises up-plunge.

Stormville Member of the Coeymans Fm
Good exposures of the Stormville Member of the Coeymans Formation in steep slope beyond farm house on right.

Cross Cherry Creek.

Entering Wildcat Hollow.
Exposures of northwest-dipping red and green clastic rocks of the Bloomsburg Red Beds in the northwest limb of the Kemmererville anticline.

Crest of Kemmererville anticline.
South of here the rocks dip gently southeast.

Crest of Kemmererville anticline.

Southeast limb of Kemmererville anticline.
Turn right and descend southeast limb of Kemmererville anticline.

Trough of Poplar Valley Syncline.
Note ten foot long (3 m) long glacial erratics of Buttermilk Falls Limestone in creek to right.

Contact Shawangunk Fm / Bloomsburg Red Beds
Contact between the Shawangunk Formation and Bloomsburg Red Beds. Ascend (we hope) steep dirt road to crest of Kittatinny Mountain.

Crest of Kittatinny Mountain.
Proceed east (to left) along dirt road to Stop 4. The quartzites of the Shawangunk Formation here are overturned to the southeast, dipping about 50°. As we proceed eastward, the rocks become vertical and then dip moderately northwest at Delaware Water Gap.

Microwave Tower of AT&T on right.

Good view to left.
Good view of Kemmererville anticline, Godfrey Ridge, and the Pocono Mountains to the north (left).

STOP 4. Delaware Water Gap Overlook.
Stratigraphy And Structure Of The Shawangunk Formation: Origin Of Wind And Water Gaps; Nature Of The Ordovician-Silurian Contact; Summary Of Trip.
Park at end of road. Disembark and follow Appalachian Trail to edge of Delaware Water Gap.
The three members of the Shawangunk Formation, basically two conglomeratic quartzite units separated by a sequence of argillites and quartzites, and the lower part of the Bloomsburg Red Beds, are well exposed in the gap. The Minsi and Tammany Members of the Shawangunk are interpreted to have been deposited by braided streams flowing off highlands uplifted during the Taconic orogeny, whereas the Lizard Creek Member of the Shawangunk represents a complex transitional continental-marine environment (Epstein and Epstein, 1967. 1969, 1972).
Fining-upward sequences in the Bloomsburg are indicative of meandering streams. The contact between the Shawangunk and the Bloomsburg, based on an upward change from gray to red rocks, is extremely irregular, particularly near the village of Delaware Water Gap, 1.5 miles (2.4 km) to the northwest (see fig. 10 and Epstein 1973).
The Shawangunk in the gap dips moderately to the northwest (figs. 10 and 11) and contains many small satellitic folds. The beds reverse their dip in the Dunnfield Creek syncline, and do so again in the Cherry Valley anticline. We will see the northwest limb of the Cherry Valley anticline at the toll booth on Interstate 80 in the village of Delaware Water Gap. Many small undulations, wedges, and bedding slips in the Bloomsburg are superimposed on the larger Dunnfield Creek syncline. Movement of these structures suggests sliding to the northwest.
The regional strike between the Martinsburg and the Shawangunk in this area differs by about 15°, and the Ramseyburg-Pen Argyl contact in the Martinsburg is buried beneath the Shawangunk 1.2 miles (2 km) southwest of the gap. The difference in structural trends is very apparent in the field, on aerial photographs, and high-altitude imagery. This regional Taconic unconformity is well documented. On the basis of several lines of reasoning, however, I believe the cleavage in the Martinsburg at the gap to be Alleghenian in age. Note that the cleavage in the Martinsburg arches, whereas bedding maintains its general northwest dip (fig. 10). indicating that the arching was not caused by external rotation during post-Taconic deformation. Rather, I believe that the arching is due to a pressure-shallow mechanism whereby cleavage in pelitic rocks adjacent to more competent rocks fans away from the axis of a syncline (see Epstein and Epstein, 1969, p. 166-167). The upper limb of the syncline in the Shawangunk is eroded away, of course, but it can be seen down-plunge to the southwest where the beds are overturned, such as at Totts Gap.
Glacial striae and roches moutonnees are common on top of Kittatinny Mountain. They trend about due south, but the Wisconsinan glacier was deflected more to the southwest on the slopes and in the valleys, following the trend of the topography.
For many years there have been numerous discussions on the origin of wind and water gaps and how that origin relates to Appalachian geomorphic development. Basically, two contrasting viewpoints have been presented. One favors coincidental location of the gaps due to superposition from a coastal-plain cover (e.g., Johnson, 1931). The other argues for northwestward headward erosion from the original drainage divide to the southeast along lines or points of structural weakness. The test of superposition, according to Strahler (1945), was to show lack of structural control for the location of the gaps.
For 40 miles (64 km) along Kittatinny and Blue Mountains and the ridges to the north, I have mapped the geology at 12 major gaps in Pennsylvania and New Jersey. The gaps are located where one or more of the following geologic conditions exist: (1) folds die out within short distances, (2) beds dip steeply and resistant units have narrow outcrop widths, and (3) there is more intense local folding or shearing than nearby (see Epstein, 1966).
At Delaware Water Gap the crest of Kittatinny Mountain in Pennsylvania is offset 800 feet (245 m) to the southeast from the trend of the crest in New Jersey. However, a transverse fault is not present through the gap (as has been suggested by several workers), because the contacts of the three members within the Shawangunk are not displaced at river level (fig. 10). The offset of the ridge crest is due to downward flexing of the rocks on the Pennsylvania side whereas the rocks maintain a constant dip on the New Jersey side (fig. 12). The flexure can be seen by looking west from the New Jersey bank. The abrupt change in strike at the gap site must have resulted in extensive fracturing in the brittle Shawangunk. Structural control is therefore thought to have determined the location of the gap. Also, the Bloomsburg Red Beds just north of the gap are involved in about 15 folds that die out rapidly to the southwest, including the large Dunnfield Creek syncline and Cherry Valley anticline. This structural situation is present at other large gaps, such as Wind Gap and Lehigh Gap. The rocks were probably more highly sheared here, and resistance to erosion was less than in the areas between gaps where similar folds were not observed.
Thus, data supporting structural control for location of the gaps does not favor the concept of regional superposition. Rather, it favors those hypotheses that maintain that gaps are located in zones of structural weakness where erosion was most effective during the course of stream competition, along the ancestral drainage divide.
Time permitting, we will sumarize the themes of this trip: structural comparisons of the several lithotectonic units, ages of deformation, regional stratigraphic framework, history of sedimentation, and Quaternary history.

Crest of Kemmererville anticline.
Crest of Kemmererville anticline. Descend northwest limb of anticline. A thin layer of till caps bedrock in most of this area.

Stratified Wisconsinan sand and gravel in kames
Stratified Wisconsinan sand and gravel in kames underlying golf course on left right. Godfrey Ridge, underlain by complexly folded Upper Silurian and Lower Devonian rocks, forms the ridge beyond Cherry Valley.

NW dipping rocks in the Shawangunk Formation
Exposures are northwest-dipping rocks in the Shawangunk Formation on the northwest limb of the Cherry Valley anticline.

Shawangunk Formation on right dips to south
Exposures of Shawangunk Formation on right dip to south on the southeast limb of the Cherry Valley anticline.

Undulations in the Bloomsburg Red Beds
Undulations in the Bloomsburg Red Beds on left are superimposed on the northwest limb of the Dunnfield Creek syncline. Many wedges and bedding-plane slips are exposed in these rocks. Note the well-developed cleavage.

Water-worn and glacially striated Bloomsburg on left.

Kame terrace on left.

Shawangunk Fm / Bloomsburg Red Beds contact
Contact between Shawangunk Formation and Bloomsburg Red Beds covered on left.

Massive conglomeratic quartzites on left.
Massive conglomeratic quartzites of the upper (Tammany) member of the Shawangunk Formation on left.

(Lizard Creek) member of the Shawangunk Fm
Interbedded quartzite. siltstone, and shale in the middle (Lizard Creek) member of the Shawangunk Formation on left.

(Mimi) member of the Shawangunk Fm
Quartzites of the lower (Mimi) member of the Shawangunk Formation on left. Note to the right that the Shawangunk dips about 45° at river level and is warped to lesser dips halfway up the mountain (fig. 12). Note gabions retaining the colluvium on left. The contact of the Martinsburg and Shawangunk is buried here but was discussed by Beerbower (1956).

4A: ALTERNATE STOP 4
In case we do not go to Stop 4, follow this road log to alternate Stop 4, picking up at mileage 36.9.

Alternate STOP 4

Steeply dipping beds, and well developed cleavage.
Steeply dipping Port Ewen Shale of the Helderburg Group, Shriver Chert and Ridgeley Sandstone of the Oriskany Group, and Esopus Formation on left. Note well-developed cleavage in the Esopus.

Crest of Godfrey Ridge
Crest of Godfrey Ridge supported by siliceous siltstones in the Esopus Formation. The road descends through several folds in the Esopus and Schoharie Formations and Buttermilk Falls Limestone.

Slightly overturned Buttermilk Falls Limestone on right.

Overturned Schoharie Formation on right.
The road ascends through several folds.

Crest of Godfrey Ridge seen on left
Crest of Godfrey Ridge, underlain by the Esopus Formation seen on left with well-developed cleavage. View to right of Cherry Valley, the Kemmererville anticline underlain by the Bloomsburg Red Beds in the middleground, and Kittatinny Mountain, underlain by Shawangunk quartzites, in the skyline.

Esopus Formation on left.

Ridgeley Sandstone on left underlain by Shriver Chert.

Port Ewen Shale on left.
The road descends through various Wisconsinan deposits.

Northwest·dipping gray sandstone Shawangunk Formation on right.

Crest of Cherry Valley anticline.
Note the lateral gradation of red, green, and gray beds at this contact between the Shawangunk Formation and Bloomsburg Red Beds.

Resort Point Overlook on left.
Note the undulations in the Bloomsburg across the river which are superimposed on the northwest limb of the Dunnfield Creek syncline. Cleavage is well developed and wedges and bedding slips are common.

Note "Indian Head" in cliffs
Note "Indian Head" in cliffs of the Shawangunk on the left side of the gap.

Shawangunk-Bloomsburg contact on right.

ALTERNATE STOP 4.
Stratigraphy And Structure Of The Shawangunk Formation: Origin Of Wind And Water Gaps; Nature Of The Ordovician-Silurian Contact; Summary Of Trip.
Copied from description for STOP4:
The three members of the Shawangunk Formation, basically two conglomeratic quartzite units separated by a sequence of argillites and quartzites, and the lower part of the Bloomsburg Red Beds, are well exposed in the gap. The Minsi and Tammany Members of the Shawangunk are interpreted to have been deposited by braided streams flowing off highlands uplifted during the Taconic orogeny, whereas the Lizard Creek Member of the Shawangunk represents a complex transitional continental-marine environment (Epstein and Epstein, 1967. 1969, 1972).
Fining-upward sequences in the Bloomsburg are indicative of meandering streams. The contact between the Shawangunk and the Bloomsburg, based on an upward change from gray to red rocks, is extremely irregular, particularly near the village of Delaware Water Gap, 1.5 miles (2.4 km) to the northwest (see fig. 10 and Epstein 1973).
The Shawangunk in the gap dips moderately to the northwest (figs. 10 and 11) and contains many small satellitic folds. The beds reverse their dip in the Dunnfield Creek syncline, and do so again in the Cherry Valley anticline. We will see the northwest limb of the Cherry Valley anticline at the toll booth on Interstate 80 in the village of Delaware Water Gap. Many small undulations, wedges, and bedding slips in the Bloomsburg are superimposed on the larger Dunnfield Creek syncline. Movement of these structures suggests sliding to the northwest.
The regional strike between the Martinsburg and the Shawangunk in this area differs by about 15°, and the Ramseyburg-Pen Argyl contact in the Martinsburg is buried beneath the Shawangunk 1.2 miles (2 km) southwest of the gap. The difference in structural trends is very apparent in the field, on aerial photographs, and high-altitude imagery. This regional Taconic unconformity is well documented. On the basis of several lines of reasoning, however, I believe the cleavage in the Martinsburg at the gap to be Alleghenian in age. Note that the cleavage in the Martinsburg arches, whereas bedding maintains its general northwest dip (fig. 10). indicating that the arching was not caused by external rotation during post-Taconic deformation. Rather, I believe that the arching is due to a pressure-shallow mechanism whereby cleavage in pelitic rocks adjacent to more competent rocks fans away from the axis of a syncline (see Epstein and Epstein, 1969, p. 166-167). The upper limb of the syncline in the Shawangunk is eroded away, of course, but it can be seen down-plunge to the southwest where the beds are overturned, such as at Totts Gap.
Glacial striae and roches moutonnees are common on top of Kittatinny Mountain. They trend about due south, but the Wisconsinan glacier was deflected more to the southwest on the slopes and in the valleys, following the trend of the topography.
For many years there have been numerous discussions on the origin of wind and water gaps and how that origin relates to Appalachian geomorphic development. Basically, two contrasting viewpoints have been presented. One favors coincidental location of the gaps due to superposition from a coastal-plain cover (e.g., Johnson, 1931). The other argues for northwestward headward erosion from the original drainage divide to the southeast along lines or points of structural weakness. The test of superposition, according to Strahler (1945), was to show lack of structural control for the location of the gaps.
For 40 miles (64 km) along Kittatinny and Blue Mountains and the ridges to the north, I have mapped the geology at 12 major gaps in Pennsylvania and New Jersey. The gaps are located where one or more of the following geologic conditions exist: (1) folds die out within short distances, (2) beds dip steeply and resistant units have narrow outcrop widths, and (3) there is more intense local folding or shearing than nearby (see Epstein, 1966).
At Delaware Water Gap the crest of Kittatinny Mountain in Pennsylvania is offset 800 feet (245 m) to the southeast from the trend of the crest in New Jersey. However, a transverse fault is not present through the gap (as has been suggested by several workers), because the contacts of the three members within the Shawangunk are not displaced at river level (fig. 10). The offset of the ridge crest is due to downward flexing of the rocks on the Pennsylvania side whereas the rocks maintain a constant dip on the New Jersey side (fig. 12). The flexure can be seen by looking west from the New Jersey bank. The abrupt change in strike at the gap site must have resulted in extensive fracturing in the brittle Shawangunk. Structural control is therefore thought to have determined the location of the gap. Also, the Bloomsburg Red Beds just north of the gap are involved in about 15 folds that die out rapidly to the southwest, including the large Dunnfield Creek syncline and Cherry Valley anticline. This structural situation is present at other large gaps, such as Wind Gap and Lehigh Gap. The rocks were probably more highly sheared here, and resistance to erosion was less than in the areas between gaps where similar folds were not observed.
Thus, data supporting structural control for location of the gaps does not favor the concept of regional superposition. Rather, it favors those hypotheses that maintain that gaps are located in zones of structural weakness where erosion was most effective during the course of stream competition, along the ancestral drainage divide.
Time permitting, we will sumarize the themes of this trip: structural comparisons of the several lithotectonic units, ages of deformation, regional stratigraphic framework, history of sedimentation, and Quaternary history.

Cold Air Cave on right.
Cave is formed by a large slab of quartzite float resting on smaller stones. Cold air stored in the colluvium flows down through the rocks and into the cave. It was used for storage of soft drinks more than 50 years ago (Stone, 1932).

Ramseyburg member of the Martinsburg Fm
Outcrop of the middle (Ramseyburg) member of the Martinsburg Formation on right. Beds dip 32° NW and cleavage dips 7° NW.

Very coarse kame-terrace deposits on right.
These deposits flank both sides of Delaware Valley for more than 1 mile downstream.

Quarries in Bushkill member of the Martinsburg Fm
Two quarries hidden in narrow valleys on right are in the lower (Bushkill) member of the Martinsburg Formation.

5: ALLEGHANIAN THRUST FAULTS IN THE KITTATINNY VALLEY, NEW JERSEY
Avery Ala Drake, Jr., and Peter T. Lyttle
U. S. Geological Survey
Reston, Virginia
Introduction
Major thrust faults involving both Proterozoic basement and Cambrian and Ordovician sedimentary rocks have been known in the Kittatinny Valley at least since the geologic mapping that resulted in the New Jersey State Geologic Map (Lewis and Kummel, 1910-12) and the Raritan Folio (Bayley and others, 1914). Three important thrust faults, the Jenny Jump, Portland, and Federal Springs, display quite different tectonic styles at the present level of erosion and, thereby, serve as showpieces of thrust fault tectonics for this part of the central Appalachian orogen. The purpose of this field trip is to demonstrate these three thrust faults and to present evidence for their late, probably Alleghanian age. In addition, attendant structural features such as autoclastic melange and chert mylonite will be shown.
Road log
The field trip begins in the parking lot at Rutgers-Newark and reaches the Kittatinny valley by the garden state parkway and interstate 280 and 80. Subsequent to stop 9, the trip returns to Rutgers-Newark by route 206, interstates 80 and 280, and the Garden State Parkway. Geologic notes are provided for the route 206 segment of the return. Field trip stops 1-8 are in the Blairstown 7.5-minute quardrangle and stop 9 is in the Newton East quadrangle. (A copy of these two quadrangles will be provided to each participant.) The trip route also traverses the Tranquility, Newton East, and Stanhope quadrangles.

5: ALLEGHANIAN THRUST FAULTS IN THE KITTATINNY VALLEY, NEW JERSEY

Exposures of sandstone and mudstone
Alternating beds of red sandstone and mudstone with a few thin interbeds of gray siltstone and dark gray to black micaceous shale, occurring below the first overpass. These siltstones yield a probable late Norian palynoflora and occur about 1100 m below the First Watchung Mountain Basalt (Cornet and Traverse, 1975, p. 27). Sporadic exposures of sandstones and mudstones with fining-upward sequences, characteristic of meandering streams, occur along Interstate 280 for the next 4.4 miles.

Basalt of the First Watchung Mountain
Contact with the underlying red beds is concealed. Note: characteristic radial columnar joint pattern.

Basalt of the Second Watchung Mountain
Contact with the underlying beds is concealed.

Basalt of the Third Watchung Mountain
Basalt of the Third Watchung Mountain is exposed to the south of the highway.

Passaic River Valley
The valley is underlain with glacial clays and silt that were deposited in Glacial Lake Passaic. The lake formed as glacial meltwaters were impounded between the New Jersey Highlands to the west and the Watchung Mountains to the south and east (see Kummel, 1940).

First preCambrian rocks
Water tower on right (left?) is on Proterozoic (Precambrian Y) rocks of the N.J. Highlands.

Begin climb from Jurassic-Triassic Basin into the Highlands.

Steeply dipping amphibolites.
First roadcuts of Highlands rocks, here steeply dipping amphibolites.

Biotite-quartz-plagioclase gneiss.
Outcrops of very rusty metasedimentary biotite-quartz-plagioclase gneiss.

Field area of Paul Sims
This was field area of famous Precambrian geologist Paul Sims. The ridge to right front is held up by the Silurian Green Pond Conglomerate.

Cruddy outcrops of Proterozoic gneiss.

Lots of glacial till on left.

Biotite-quartz-plagioclase gneiss
Large outcrop of strongly layered biotite-quartz-plagioclase gneiss of Proterozoic age on right.

Outcrops of hornblende granite of Proterozoic age.

Outcrops of Proterozoic rocks.

Musconetcong River
Formerly a great trout stream, now a temporary habitat for fish between hatchery and skillet.

Continuous outcrops of Proterozoic rocks
Continuous outcrops of Proterozoic rocks on Allamuchy Mountain. These rocks are in the core of the Allamuchy nappe of the Musconetcong nappe system of the Reading Prong nappe megasystem. The rocks cropping out at the rest stop to the left and above the highway are severely deformed and contain several flat thrust faults.

Scenic overlook.
If weather is fine, bus will pull off here and we will give a short briefing on the regional geology and this field trip. Looking north from this place, one has an excellent view of the Kittatinny Valley and Jenny Jump Mountain.

Bold outcrops of Proterozoic rocks.

Granite gneiss containing mafic segregations
This outcrop of granite gneiss contains mafic segregations of plagioclase, epidote, garnet and magnetite surrounded by a rind of almandine garnet in a more felsic matrix of potassium feldspar, quartz, plagioclase, epidote, and accessories. Foliation appears to parallel gneissic layering and is oriented N. 45° E., 39° SE. Pegmatites are roughly parallel to foliation, but upon close inspection are seen to cut it.

Entering Bear Swamp.
Rocks in this area are Allentown Dolomite of Late Cambrian age.

Nice outcrop of Allentown Dolomite.
Beds strike N. 82° W., and dip 15° NE, cleavage strikes N. S5° W. and dips 22° NE, their intersection, roughly parallel to axes of small folds, plunges 14° N. 18° W. The beds face up and are probably in the upper limb of the Allamuchy nappe.

Begin the ascent of Jenny Jump Mountain
Here we are crossing the trace of the Shades of Death thrust which brings rocks of the Allamuchy nappe onto rocks of the Jenny Jump klippe of the Jenny Jump thrust sheet. The Proterozoic rocks here are dominated by a sequence of marble, amphibolite, and lesser calcsilicate rock.

Lower Paleozoic rocks beneath the thrust fault
We have passed through the Proterozoic rocks of the Jenny Jump klippe and here enter a sequence of lower Paleozoic rocks beneath the thrust fault. Here the outcrops are Epler Formation of the Beekmantown Group of Early Ordovician age. These outcrops contain fairly abundant solution collapse breccia. Many bedding surfaces in these rocks are also thrust faults and a fair amount of carbonate mylonite has been formed. Axes of small folds plunge 5° S 25° E; beneath the Proterozoic rocks of the Jenny Jump klippe.

Nice outcrops of Allentown Dolomite.
Here we are about on the crest of an anticline which plunges 5° N 45° E. Beds face up as shown by good algal stromatolites.

Long continuous outcrop
Long continuous outcrop beginning in Allentown Dolomite, Rickenbach Dolomite, Epler Formation, and Ontelaunee Formation. (See Markewicz and Dalton, this Guidebook.)

Epler / Rickenbach contact
Large outcrop of sandy, mottled, laminated dolomite of the Epler Formation. The contact with the Rickenbach Dolomite is about in middle of this cut. It is placed at the contact of laminated, burrowed, mottled, finely crystalline dolomite (Epler) with thick-bedded, dark-medium-gray, medium crystalline dolomite (Rickenbach). Rock contains abundant cascade-type folds which plunge 5°-10° N 25° E.

Outcrops of Jacksonburg Limestone.
Most of rock here is crystalline limestone but some beds are dark-gray, more argillaceous cement rock. Axes of small folds here plunge 20° N 5° W. Slickensides on bedding surfaces plunge down the dip.

More outcrops of Jacksonburg Limestone.

More outcrops of Jacksonburg Limestone.
More outcrops of Jacksonburg Limestone. A lot of conglomerate here. Outcrops to south of Interstate are Bushkill Member of the Martinsburg Formation. Slaty cleavage, which strikes N 60° E and dips 20° NW., is principal planar element in these rocks. The cleavage surfaces are marked by a strong extension lineation which plunges 5° N 35° W. and crenulations which are nearly horizontal N. 70° E. Strong crenulation cleavage strikes N. 70° E. and dips 75° SE.

Bushkill Member of Martinsburg Fm
We are driving on Bushkill Member of Martinsburg Formation. Outcrops to right are Allentown Dolomite in the large Hope klippe of the Jenny Jump thrust sheet. The dolomite beds face up, dip gently northwest, and contain abundant algal stromatolites and oolite.

Here we are at the base of the Hope klippe.
The outcrop to the right is oolitic, shaley, Allentown Dolomite, probably the lowest beds of that unit. The beds dip gently to the northwest and face up.

Hope, a pre-revolutionary Moravian settlement
Entering the town of Hope which is a pre-revolutionary Moravian settlement.

Outcrop on right is Leithsville Formation
Outcrop on right is Leithsville Formation of Early and Middle Cambrian age. The gently northwest dipping rocks are right at the sole of the Hope klippe. They dip gently northwest, have a vague mylonitic foliation which strikes N. 45° E. and dips 18° NW., and a general mangled appearance.

Outcrops on right are Jacksonburg Limestone.
The rock here is well-bedded, calcarenite grainstone that contains abundant fossil hash and small scattered pebbles of dolomite. The beds strike N. 75° W. and dip 25° NE. They have a cleavage which strikes N. 55°E. and dips 15° SE.; this cleavage is marked by an extension lineation which plunges approximately down the dip. The intersection of the cleavage with the bedding plunges 7° N 88° E. These rocks are autochthonous to the Jenny Jump thrust sheet and belong to an as yet unnamed tectonic element of the Musconetcong nappe system of the Reading Prong nappe megasystem.

Ontelaunee Fm of Beekmantown Group
Outcrop on right is Ontelaunee Formation of Beekmantown Group. This is Field Trip Stop 2 to which we will return.

Poor outcrop of Allentown Dolomite
Poor outcrop of Allentown Dolomite on lawn on the right. Abundant, excellent outcrops of Allentown on wooded knoll to to the east.

STOP 1. Jenny Jump klippe of Jenny Jump thrust sheet
Speaker, Peter Lyttle.
(Field trippers will disembark, bus driver will take bus to top of hill to Hissim Road to turn around. He should wait there for 30 minutes, and return down the hill to pick up the field trip in front of the house at the base of hill.)
We are on the northwest edge of the main mass of the Jenny Jump thrust sheet on the northwest side of Jenny Jump Mountain. The Proterozoic rocks we will be looking at here are primarily hornblende granite gneisses with minor fine-grained mafic dikes. These rocks structurally overlie the lower Paleozoic rocks of the valley that we have just driven through. Although the Jenny Jump thrust is nowhere exposed, there are several locations along the north side of Jenny Jump Mountain where outcrops of Paleozoic carbonate with structures dipping to the southeast occur within a few tens of meters of the Proterozoid gneisses. It is clear in map pattern (see Figure 4) that the Jenny Jump thrust truncates both contacts and structures in Paleozoic rocks.
In order to see all of the structures mentioned below, it is necessary to hike a hundred meters or so along the side of Jenny Jump Mountain in this area of semi-continuous outcrop. Almost all of the structures can be seen in several places and the diligent tripper should be able to find them all on his/her own. The most important structure to note at this outcrop is well-developed foliation that is, in most places, parallel to compositional layering and is axial planar to the rarely observed earliest isoclinal folds that are presumably Grenville in age. This foliation is seen in both the gneiss and mafic dikes. The orientation of the dikes appears to roughly parallel the foliation, but can by at an angle to compositional layering, indicating that the dikes intruded either during or before this early folding episode. This foliation is folded by a later event interpreted to be the emplacement of the Jenny Jump thrust sheet. Over most of Jenny Jump Mountain the foliation strikes roughly N. 60°E. and dips 30-40° to the southeast. However, at several places along the northwest edge of Jenny Jump Mountain. it is common to find the foliation folded by large, open, upright to slightly overturned folds .
There has been considerable slip on many foliation planes (evidenced by slickensides) and if the rocks at this outcrop are not wet or in the shade, the field tripper will note many narrow zones of mylonite that are roughly parallel to the foliation. Locally, these zones of mylonite are brecciated. These outcrops are very near the sole of the Jenny Jump thrust sheet and it is likely that the mylonitization and brecciation are related to the emplacement of the thrust sheet.
In one area of these outcrops, a thin mafic dike is cut by numerous small-scale thrusts spaced 3-10 cm apart. The sense of movement is always toward the NNW.
The gneisses here are quite magnetic, the magnetite probably being produced with chlorite at the expense of hornblende. Very little fresh hornblende is seen in thin section. Quartz, microcline oligoclase, minor hornblende and magnetite, and accessory zircon and apatite make up the bulk of the gneisses. The oligoclase and hornblende are commonly altered, and the quartz is highly strained and occurs in long sheared out stringers.

STOP 2. Bedding-parallel faults in the Ontalaunee Fm
Speaker. Peter Lyttle. (Driver pull bus onto turnout on left side of road.)
This will be a very quick stop to illustrate bedding-parallel shear and mylonitization in the Lower Ordovician Ontalaunee Formation. Other outcrops show this more extensively, but this outcrop is logistically more feasible for this field trip. Although pressure solution is the dominate deformation mechanism producing tectonic shortening in the carbonate rocks of the Great Valley, both the rocks within and tectonically beneath the Jenny Jump thrust sheet exhibit extensive faulting parallel to bedding. This shearing is commonly, though not exclusively, concentrated in chert rich zones within dolomites. The chert need not be in continuous beds. Zones of nodular chert and very thin stringers appear sufficient to provide a contrast or inhomogeneity in rock strength sufficient to concentrate shearing within these areas.
Although this stop has well developed zones of mylonite concentrated along chert zones that have behaved ductilely and show small drag folds (see fig. 7), other outcrops show a transition from brittle to ductile structures in these zones. This transition is achieved through a continual change in the mechanical properties of the rock probably because of the reduced grain size, water weakening or localized frictional heating rather than changes in external parameters such as external temperature and confining pressure. Initially, the dolomite and chert together form a breccia with pieces of dolomite ranging in size from 1·15 cm and pieces of chert ranging in size from 1 mm to 5 cm. Continued shearing pulverizes the chert which then acts as a fine-grained matrix surrounding pieces of dolomite which are still angular and recognizable, yet smaller, pieces of dolomite. At this stage the rock has a "frothy" appearance and the chert has lost its black translucence. More shearing produces a mylonite, such as the example at this stop (see fig. 6), and there are no longer any recognizable pieces of dolomite. Everything has been finely comminuted and the rock has a fluxion structure. At this outcrop the fluxion structure is folded into small drag folds.
It is important to realize that the fluxion structure or "cleavage" developed in these zones does not represent regional cleavage. The orientation of the "cleavage" or mylonitic foliation in these shear zones is related to the original attitude of the chert zones and is parallel to the shear zones. Regionally. this "cleavage" is best developed in narrow shear zones in and immediately beneath the large scale thrusts and is essentially parallel to these thrusts. The Jenny Jump thrust was slightly above the present erosional surface at this stop and may have caused the subsidiary thrusting and mylonization at this locality.
The Ontelaunee Formation at this stop is very finely to finely crystalline, light to medium gray, medium- to thick-bedded dolomite with thin beds of chert. Fabric information: bedding N. 67° W. 15° NE; extension lineation 13° S 38° E; fold axis in mylonite 14° N 48° E.; joints N 85° E. 67° SE. and N. 15° E. 15° SE.

Outcrop at Jacksonburg Limestone on left.

Sole of Hope Klippe.
Outcrops of Allentown Dolomite on the left. Beds strike. N. 75°, and dip 25° NW. Rocks face up as shown by abundant algal stromatolites.

Outcrops of Allentown Dolomite on left.
Here there are dolorudite beds and orthoquartzite lenses. Big, rounded bedding surfaces suggest algal stromatolites but internal ornamentation is not obvious.

Outcrops of Allentown Dolomite on right.
Rock here is mostly oolite with some oolite matrix conglomerate.

Outcrops of oolitic Allentown Dolomite on right.
Rock has strongly developed extension fractures which strike N.48° E. and dip 65° NW.

Cross small stream
Cross small stream which follows a steep normal fault which fragments the Hope klippe in this area.

STOP 3. Hope klippe of Jenny Jump thrust sheet
Speaker. Avery Drake.
(Park in Methodist Church parking lot on right, unless church services are being held; if services are being held, park on left side of street near Honeywell Hall.)
Here we are on the Bushkill member of the Martinsburg Formation at the northwest border of the Hope klippe. The bounding thrust fault lies in the stream a short distance to the southeast, and carbonate rocks of the klippe crop out on the ridge to the southeast of the streams. The klippe here has been fragmented by a later normal fault which has brought rocks of the Epler Formation into contact with the Bushkill. We will first observe rocks of the Bushkill on the slope to the southeast of Green Chapel Cemetery. The Bushkill here is very disturbed. In the fall of 1978 the following fabric elements could be measured: bedding, N. 30° E., 65° SE. (inverted); slaty-cleavage, N. 20° E., 40° SE.; and pseudo·slaty cleavage, N.38°E. 52°SE.; strainslip cleavage, N. 50°. 45° NW.; intersection of bedding and slaty cleavage and pseudo-slaty cleavage, 20°S.55° W., crenulations, 16° N. 36° E.; extension lineation on slaty cleavage, 38 °S. 50°E.; and a joint, N. 60° W. 60° SW. There are many folds in bedding, but the details have not been worked out. The pseudo-slaty cleavage is thought to result from the emplacement of the Jenny Jump thrust sheet. At this place the planar elements, save the strain-slip cleavage which results from post-klippe emplacement folding, dip beneath the carbonate rocks and the extension lineation plunges beneath them. Bushkill is also exposed in pavement outcrops in the secondary road to the southwest of the Mt. Hermon Road.
After observing the Bushkill, we will examine the outcrops of Epler on the ridge to the southeast. The rock there is finely crystalline to medium crystalline, light gray to medium-gray dolomite which contains thin partings, lenses, and very thin beds of orthoquartzite. The outcrop contains abundant solution collapse breccia. Many of the blocks in the breccia are quite large. Bedding in the outcrop is N. 45° E. 38° NW. A poor fracture cleavage has the altitude N. 10° E. 55° SE. Return to bus and continue northwest on Mt. Hermon road.

Northwest border of Hope klippe.
Cross small stream which marks the northwest border of Hope klippe.

Ramseyburg Member of Martinsburg Fm
Outcrop of Ramseyburg Member of Martinsburg Formation on the left.

Poor outcrops of Ramseyburg on the right.

More poor outcrops of Ramseyburg on the right.

Small pond on right.
Geology along here is obscured by ground moraine.

Outcrops of Ramseyburg on left.

Mangled outcrops of Allentown dolomite
Mangled outcrops of Allentown dolomite of Hope klippe on the left. Continue north .15 mile distance and pull into turn-off on right.

STOP 4: Northwest boundary of Hope klippe
Speaker, Avery Drake.
Here rocks of the Bushkill Member crop out in a cut at road level and carbonate rocks of the klippe crop out on the hill above. This is not a good exposure of the Bushkill, but it is extremely important as the rock here is an auto clastic tectonic melange. Careful observation will reveal phacoids, "tectonic fish" of graywacke and slate, some of which are fold hinges, within the mangled slate matrix (see fig. 8). PLEASE NO HAMMERING OR PLUCKING OF "TECTONIC FISH." There are at least two flat cleavages interlacing within this outcrop, presumably the slaty and pseudo-slaty cleavages viewed elsewhere. The prominent foliation in this outcrop is due E. 10° S.
Here the carbonate rock of the klippe is Allentown Dolomite. The outcrop has a jumbled appearance and bedding is difficult to determine but seems to be about N 10° W., 10° NE. Most of the rock is rather nondescript crystalline dolomite, but there is a fair amount of dolarenite and some oolite, desiccation dolorudite, and dark-gray chert lenses and skims. In addition, some curved forms without internal ornamentation are suggestive of algal stromatolites. It is quite clear at this stop that the carbonate rocks of the klippe lie above the Bushkill. Reboard the bus and continue northeast on Hope Road.

Turn right on Mud Pond Road
Turn right on Mud Pond Road (10,000 pound limit). This road essentially follows a normal fault which has fragmented the Hope klippe in this area, carbonate rocks of the klippe on the right, Martinsburg on the left. Carbonate rock for first .2 mile along road is Rickenbach Dolomite.

Mangled outcrops of Allentown Dolomite on right.

Outcrops of severely mangled Martinsburg.
Rock here is an autoclastic melange consisting of phacoids and lenses of graywacke and slate "swimming" in slate. Extension lineation plunges essentially down the dip of the principal foliation. The klippe sole here lies a few feet up the hill to the right.

Small pond on left.

Good pavement outcrop of Bushkill on the left.

Ramseyburg outcrop on the left.

Slate with graywacke
Outcrops of slate containing a few thin graywacke beds at intersection.

Bridge over small stream.
Bus will go a short distance farther and disembark the field trippers. It will then continue south on Ridgeway Road and turn around wherever possible, and return for the field trip in about 1/2 hour.

This carbonate rock constitutes the small Cooks Pond klippe.
Cooks Pond on the left. Outcrop of cherty, laminated, finely crystalline medium-dark-gray dolomite of the Epler Formation on the right. This carbonate rock constitutes the small Cooks Pond klippe.

Outcrops of Bushkill slate at intersection.

STOP 5: Silver Lake I klippe
Speaker, Peter Lyttle.
The Silver Lake I klippe is a tiny erosional remnant of the Jenny Jump thrust sheet that contains a strongly deformed and perhaps highly telescoped section of Proterozoic granite and Lower paleozoic dolomite (probably Cambrian Leithsville Formation). Although the two or three outcrops that we will examine at this stop may at first glance be a little disappointing, this single locality records much of the tectonic history that we are trying to present on this field trip. We will look at a small ledge of Proterozoic granite that records an early tectonic event of high strain, local mylonitization, and retrograde metamorphism. This first event is interpreted to have occurred during the Taconic orogeny. Later, these same rocks were severely brecciated and comminuted, but not recrystallized (see fig. 9) photomicrograph. Although most of the rock consists of quartz, perthite, and plagioclase, there are minor amounts of magnetite and chlorite that appear to be alteration products of a mafic mineral, probably hornblende. All the minerals, particularly the perthite and quartz are highly strained, brecciated and rotated and severely reduced in grain size. These later structures are interpreted to have been produced during emplacement of the Silver Lake I klippe as part of the much larger Jenny Jump thrust sheet in Alleghanian times.
This small klippe structurally overlies the Middle Ordovician Bushkill Member of the Martinsburg Formation. After the bus picks us up we will head back north along this road passing an outcrop of the Bushkill at the first intersection. At this locality the slaty cleavage dips southeast under the Silver Lake I klippe. South of Stop 5 near Camp Hope (approximately 1/2 mile) the slaty cleavage in the Bushkill dips consistently to the northwest. Therefore, the klippe is sitting in a broad synformal trough of the slaty cleavage. Although it is impossible to prove at this stop, the emplacement of the klippe postdates the formation of the slaty cleavage. We will establish this to the satisfaction of the sceptical field tripper at the last stop of the day, the Grand Union klippe.
The only structures recorded at this stop are a fairly flat mylonitic foliation, N. 16°E. 18° NW. and a steeper and later cleavage N. 78°E. 50° SE. These were both measured (with difficulty) in the highly weathered Proterozoic granite. The pervasive rusty weathering was probably facilitated by the extensive brecciation along the later fracture cleavage. The tiny outcrop of dolomite fractures in a rectilinear fashion no matter how small the pieces become. This may be related to the late fracture sets.

STOP 6: Ebenezer klippe
Speaker. Avery Drake
(At about the Ebenezer sign, the bus will pull off to the right and allow field trippers to disembark. The bus will continue up hill to intersection with Lake Wasigan Road and park. Field trippers will walk up hill examining the outcrops. This will be the lunch stop.).
The first outcrop to examine is just to the north of the small stream, The rock here is Ramseyburg Member of the Martinsburg Formation. Fabric elements measured here in the fall of 1978 include: bedding, N.52° E. 25° NW.; slaty cleavage, N. 48° W. 5°NE.; strain-slip cleavage, N. 25° E. 20° SE,: a joint, N. 44° W. 70° SW.; intersection of bedding and slaty cleavage, 7° N. 48° E.; and extension lineation, 3° N. 35° W. The reader will note that here the bedding, slaty cleavage, and extension lineation have been rotated from their normal southeast dips and plunge so as to dip and plunge beneath the carbonate rocks to the north.
The last outcrop of Ramseyburg is about 400 feet to the north and the first outcrop of the carbonate rock of the klippe is about 375 feet north of there. The rock of the klippe is Allentown Dolomite. There is a particularly good outcrop of Allentown about 225 feet farther north which contains all the characteristic rock types of that unit: algal stromatolites, oolites, dessication dolorudites, etc. The sedimentary structures show that the carbonate rocks face up. The subtle field trippers will have noted that Ramseyburg crops out about 30 feet to the south of this Allentown outcrop for a length of about 20 feet showing that the klippe here, like the Hope klippe, is fragmented by later normal faults. The beds in the Ramseyburg dearly dip beneath the carbonate rocks of the klippe. There are additional good outcrops of Allentown along the road to the east of Lake Wasigan.
We plan to have lunch around Lake Wasigan. This is far from a perfect place, but our choices are limited. Following lunch, board the bus.

Inverted Bushkill slate crops out on the left.

Excellent outcrop of Ramseyburg on the left.
Some beds here are more than 1 m thick.

Rocks here are Martinsburg Fm in the Musconetcong nappe system.

Crossing small stream.
We will cross the trace of the Portland thrust fault within a few feet. Here the slaty cleavage in the Martinsburg is marked by a strong extension lineation which plunges down the dip. The Portland thrust fault frames the very large Paulins Kill window.

Large outcrops of Allentown Dolomite.
These rocks are in the Lyon Station-Paulins Kill nappe which is exposed in the Paulins Kill window.

Allentown Dolomite crops out up Hope Road to the Left.

Outcrops of Allentown Dolomite
Outcrops of Allentown Dolomite in Lyon Station-Paulins Kill nappe on right. Rock is severely deformed, most bedding surfaces have served as fault surfaces. Outcrop is characterized by very abundant filled, northeast-trending extension fractures.

Small outcrop of Allentown Dolomite on knoll to right.

Small outcrop of Allentown Dolomite on right.

Very sandy Allentown Dolomite on right.
Outcrop of very sandy Allentown Dolomite on right. There are abundant orthoquartzite beds here.

Large outcrops of Epler Formation
Large outcrops of Epler Formation on the left. Rocks here include laminated sandy dolomite, laminated dark-gray dololutlte, chert-ribbed finely crystalline dolomite, sandy medium to medium-coarse crystalline limestone, and excellent examples of solution collapse breccia. Axes of small folds here plunge 70° S 15° W., down the dip of the beds.

STOP 7 Portland thrust fault
Speaker Avery Drake
(Field trippers will disembark and examine outcrops along road to left. Bus will have to find some means of turning around. There is a small parking area along road to left. This stop is just above the abandoned grade of the New York Susquehanna and Western Railroad. This is a very narrow road and field trippers must use extreme caution.)
The first outcrop to observe is 500 feet along the road to the east. Here are slate outcrops of the uppermost Bushkill Member of the Martinsburg Formation. The slate contains abundant thin beds of graywacke. Fabric elements include: bedding, N. 85° E. 48°SE.; slaty cleavage, N. 72 ° E. 68° SE.; and intersection of bedding and slaty cleavage, 35° S 55° W.
The Portland thrust fault crops out about 375 feet farther to the east.The observations recorded here were made in October 1978 shortly after the road was widened. Winters are particularly hard on exposures in this area and no guarantee can be made as to what the quality of the exposure will be at the time of the field trip. In any case, the Portland fault was found to have the attitude of N.78° E. 48°SE. and the slate above the fault to the east an attitude of N. 80°E. 55° SE. The carbonate rock beneath the fault is thoroughly tectonized. It is mostly medium crystalline, medium-gray dolomite that contains some solution collapse breccia, flat-pebble conglomerate, and dark gray sparr calcite. Judging from stratigraphically lower outcrops of extremely cherty dolomite up the hill to the north, this rock probably belongs to the Ontelaunee Formation. The dolomite contains several movement zones beneath the major thrust which are marked by carbonate mylonite. Extension lineations on the thrust surface plunge 45°S 38° E. Post-thrust strain-slip cleavage has the attitudes of N. 80° E. 40° NW., and post-thrust crenulations plunge 10° S 70° E. There are outcrops of both Ontelaunee and Epler along the road to the east and excellent outcrops of Epler up the hill to the north. We may examine some of these rocks depending on available time. (Board buses and follow unnamed road back up the hill to the north.)

Trace of the Portland thrust fault
Crossing the trace at the Portland thrust fault, the frame of Paulins Kill window.

Inverted Bushkill slate
Outcrop of inverted Bushkill slate at road intersection on the right

Nice outcrops of Ramseyburg on the right.

More nice outcrops of Ramseyburg.
Sedimentation sequences in these rocks begin with a cross-laminated interval which pass up into a planar laminated interval which is overlain by pelite. They are, then Tcde turbidites and belong to turbidite Facies D of Walker and Mutti (1973). The cleavage in these rocks is marked by an extension lineation which plunges 35° S. 15° E.

Outcrops of Bushkill slate on left
Cleavage here is marked by an extension lineation which plunges 20° S. 48° E.

Outcrops of Bushkill slate on the right.
Extension lineation on cleavage here plunges 34° S. 25° E.

Rickenbach Dolomite in the small Alpha Klippe
Rickenbach Dolomite in the small Alpha Klippe crops out to the left. Allentown Dolomite in the even smaller Beta Klippe crops out in the woods about .25 miles to the east-northeast. Both these klippen rest on Ramseyburg and are shown but not labeled on figure 1.

Rock is Bushkill.

STOP 8: Federal Springs thrust fault
Speaker, Avery Drake.
(Follow path to left of stop to reach the grade of the Erie-Lackawanna Railroad. Be extremely careful on the railroad grade, there are occasional trains. Follow railroad grade about 600 feet to west.)
Here are beautiful outcrops of interbedded slate and thin graywacke of the upper Bushkill member of the Martinsburg Formation (see fig. 2). The Ramseyburg Member crops out along the road about 700 feet north of these outcrops. The rock in this outcrop is inverted as shown by sedimentary structures. Fabric elements are: bedding, 50° W. 45° SW.; slaty cleavage, N 70° W, 35° SW.; intersection of bedding and slaty cleavage, 20° S. 35° E., and extension lineation. 28° S. 38° E. Here, the bedding-cleavage intersections which are roughly parallel to the local fold axes plunge southeast beneath the Federal Springs klippe about parallel to the direction of transport as shown by the extension lineations.
Next, the field trip will turn around and follow the railroad tracks to the east. About 400 feet east of the overpass there are horribly mangled outcrops of Bushkill not very far beneath the Federal Springs thrust fault. The field trippers can sort out structures here at their pleasure. The Federal Springs thrust fault crops out about 500 feet farther to the east. The geologic relations at this site are quite complex as it is essentially a quadruple point between Epler Formation, Ontelaunee Formation, Jacksonburg Limestone, and Bushkill Member of the Martinsburg Formation. The Federal Springs thrust fault brings rocks of the Beekmantown Group and Jacksonburg Limestone onto the Bushkill. Two units occur within the Beekmantown here. The lower unit, the Epler Formation consists of very earthy, silty, finely crystalline dolomite that has silty partings, limey dolomite, and some limestone. The Epler is overlain by a unit of medium-gray, medium- to coarsely-crystalline dolomite which based on our experience in Pennsylvania, we assign to the Ontelaunee Formation.
The Jacksonburg Limestone appears to uncomformably overlie both Beekmantown units in these exposures. The Jacksonburg here is a small tectonic sliver of dark gray, shaly cement rock. A sample of this rock contained a poor conodont fauna which, according to John Repetski (written commun., 1979) included the following:
2 drepanodonti form elements, indeterminate, deformed
1 paltodonti form element A
1 paltodonti form element B
Another tectonic sliver of Jacksonburg crops out along the Federal Springs fault about 1100 feet N. 63° E. from this site. The Jacksonburg here is a radically different rock type. being medium-grained calcarenite grainstone. A sample from this site contained as, identified by John Repetski (written commun., 1979) the following conodont fauna:
PANDERODUS
PHRAGMODUS UNDATUS Branson and Mehl
dichognathiform elements
oistodonitform elements
phragmodontiform elements
PLECTODINA
cyrtoniodontiform (N) element
This rather non diagnostic microfauna ranges from the Rocklandian to upper Richmondian. The conodont color alteration index (CAl) of the elements in this sample is 5, indicating host rock temperatures greater than about 290°C.
The structure above the Federal Springs thrust is quite complex. At the end of the railroad cut about 5S0 feet to the east of the fault, Epler crops out at track level. About 65 feet west of this point Ontelaunee is at track level, and about 250 feet farther west Epler comes back down to track level. This rock distribution defines a very tight fold which plunges about 35° N 70° E. Small early folds within this part of the outcrop plunge 35° S 47° E.; essentially parallel to the extension lineation within the Epler. These folds have an S rotation sense when viewed in profile showing that this is an inverted limb. Other fabric elements here include: steep fracture cleavage, due N., N. 80° E.; pressure solution veins which plunge 40° S 20° E., and opens buckle folds in bedding which plunge 10° N 75° E.
Just at the Federal Springs thrust which trends northeast and at these places dips rather steeply, the Jacksonburg Limestone is transposed and the transposition foliation is folded with the rocks of the Beekmantown Group. The fabric elements within the Jacksonburg include: the transposition foliation, N 25° E., 52°NW.; intersection of bedding and slaty cleavage 40° N; 20° W., extension lineation on the transposition foliation, 48° N 40° W.; and axes of small folds in the transportation foliation 10° S 45° W. The lineation formed by the intersection of bedding and cleavage streams around the fold hinge directly above the thrust.
Folds such as those above the thrust are not obvious in the slates of the Bushkill beneath the thrust. The fabric elements in the slate include: bedding, N 75° E 35° NW. (sedimentary structures show that the rock faces up); slaty cleavage. N. 5° W. 35° SW.; fracture cleavage, N. 75° W. 40° SW.; and axes of small folds in slaty cleavage 12° S. 60° W. A wide variety of structures can be observed in the Bushkill to the west of the thrust and the interested observer can observe these at his/her leisure.

More outcrops of Bushkill on right.

Small outcrop of Bushkill on left.

There is a good view of Hunts Pond
There is a good view of Hunts Pond to the right front. We have done no geologic mapping in this area.

Pavement outcrops of Bushkill on the left.

Excellent Bushkill outcrop on the left.

Bushkill outcrop to right, small pond to left.

Bushkill outcrops on the left.

Outcrops of Bushkill on the left.
Here, the slaty cleavage has been rotated past the horizontal and dips northwest. Route 94 is roughly paralleling the geologie strike in this area.

Scattered outcrops of Bushkill along here.
Slaty cleavage dips to the northwest.

Outcrops of Martinsburg Formation on the left

STOP 9: Grand Union klippe
Speaker Avery Drake.
This klippe is a relatively small slab of Allentown dolomite which lies on rocks of the Ramseyburg Member of the Martinsburg Formation. The thrust fault beneath it (fig. 10) was well exposed during excavation for this shopping center. The thrust fault, thought to be the Jenny Jump thrust fault, is roughly parallel to the bedding in the Allentown N. 50° E. 40° NW., and is marked by 1 to 3 inches of gouge as well as by a fair amount of crushed dolomite. The rocks of the klippe face up as is clearly shown by abundant algal stromatolites.
The rocks of the Ramseyburg beneath the thrust are isoclinally folded. The fold trains have a (zigzag) "M" pattern suggesting that the rocks occur in a fold hinge. Bedding immediately adjacent to the thrust is N. 35° E. 65° NW., and it approaches vertical several feet to the southeast (Fig. 10). Slaty cleavage is N. 20° E. 35° NW., has been rotated past the horizontal, and is truncated by the thrust. These data and their geometric relations suggest that the Ramseyburg here is in the brow and upper limb of a northwest-closing recumbent fold. The slaty cleavage is marked by an extension lineation which plunges 39° N 55° W. and extension fractures are N. 38 ° E. 85° SE.
Close examination of the Ramseyburg shows that it, like other Martinsburg we have seen in exposures beneath the Jenny Jump thrust, is an autoclastic melange. Here, most of the graywacke beds have been pulled apart and fragmented and swim as autoclasts in a more slaty matrix.
Two sets of small faults can be seen in the Ramseyburg. One set is
N. 52° E, 40° NW. and has pressure solution veins which show left-separation. The other set is N. 50° E. 80° NW. and shows normal-separations.
This exposure is extremely important as it clearly shows that a klippe of the Jenny Jump thrust sheet was emplaced subsequent to major deformation and slaty cleavage development in rocks of the Martinsburg Formation. This klippe, like the others we have seen, lies in a synform in the slaty cleavage of the Martinsburg.

Large outcrops of Allentown dolomite on right.
This rock is in the Allamuchy nappe.

Good outcrops of Allentown Dolomite on left.

Outcrops of Allentown Dolomite on the right.

Outcrops of Allentown Dolomite behind the Rustic Wine Cellar.

Outcrops of Allentown Dolomite on both sides of road.

Proterozoic rocks at the Allamuchy nappe
Proterozoic rocks at the Allamuchy nappe crop out to the right. The allochthonous nappe-nature of the tectonic unit was confirmed in this area by diamond drilling by the New Jersey Zinc Company (Baum, 1967).

More outcrops of Proterozoic rocks
More outcrops of Proterozoic rocks on the left. We will remain in these rocks until we rejoin Interstate 80.

Outcrops of hornblende granite.
This is Bryam Township, the type area of the so-called Bryam Gneiss.

6: THE NEW JERSEY COASTAL PLAIN
AND ITS RELATIONSHIP WITH THE BALTIMORE CANYON TROUGH
Richard K. Olsson
Department of Geological Sciences
Rutgers University
New Brunswick, New Jersey
Introduction
The coastal plain of New Jersey lies along the western edge of the Baltimore Canyon Trough, a large sedimentary basin which extends along the United States Middle Atlantic states (Fig. 1), Tne Baltimore Canyon Trough extends seaward beneath the continental shelf to the upper continental slope. A westward extension of the trough forms the Salisbury Embayment of New Jersey, Delaware, Maryland and eastern Virginia. The Raritan Embayment of northern New Jersey and Long Island is a shallow embayment. The South Jersey High separates these two embayments of the trough. The Baltimore Canyon Trough is composed of a seaward-thickening wedge of Mesozoic and Cenozoic sedimentary rocks which overlie a warped and faulted crystalline basement. The sediments that lie within the New Jersey Coastal Plain were deposited west of the main hinge line of deposition. Seaward of the hinge line the sedimentary rocks of the Baltimore Canyon Trough thicken to at least 14 km (Poag, 1979). In contrast the maximum thickness of sediments in the New Jersey Coastal Plain is less than 2 km in tHe Salisbury Embayment.
The sediments in the Baltimore Canyon Trough were initially deposited when North America and Africa separated during early Mesozoic time. The sediments (Figs. 2,3) that accumulated in the Baltimore Canyon Trough consist of limestones, sandstones, sands, shales, and clays (Poag, 1979). Diapir structures noted in geophysical profiles (Grow, 1980; Schlee and Grow, 1980) along the continental slope suggest evaporite deposition occurred in the early phases of continental separation. A deeply buried thick sequence of limestone of Jurassic and Early Cretaceous age is identified in multi-channel seismic reflection profiles of the trough and a carbonate bank or reef thought to represent the lower Cretaceous shelf edge is postulated to lie beneath the present day upper continental slope. Limestones of late Jurassic and early Cretaceous age were penetrated in the basal portion of the COST B-3 well which was drilled on the continental slope off New Jersey. The limestone sequence is confined to the deeper portions of the trough and does not extend beneath New Jersey.
Overlying the limestone sequence (Figs. 2,3) are upper Jurassic and lower Cretaceous nonmarine and shallow marine sandstones and shales (Poag, 1979). These sediments thin beneath New Jersey and lie upon crystalline basement rock. Where penetrated in wells they appear to be nonmarine in character although they have not been thoroughly studied. The upper Cretaceous and Tertiary marine sequence that forms the major part of the New Jersey coastal plain belongs to a marine cycle that began during Aptian time and transgressed over the Atlantic margin, bringing sea level over the New Jersey area for the first time since the Atlantic began to open.
The sediments that were deposited in the coastal plain of New Jersey consist of fluvial sands, gravels, and varigated clays; coastal deposits of beach, lagoon, marsh, and related deposits; inner shelf sediments consisting of shoreface sands with characteristic Ophiomorpha trace fossil assemblages and offshore micaceous clay and silty thinly bedded fine sands; mid and outer shelf clay glauconite sands and glauconitic clays, often extensively burrowed; and slope deposits composed of calcareous clays and silts. The formations of these various facies were deposited during major cycles of sea level change and are genetically related to sedimentary units that have been penetrated in the COST B-2 and B-3 wells in the Baltimore Canyon Trough. The relationship of the New Jersey formations to the units penetrated in these wells will be discussed in the section on lithologic units.

6: THE NEW JERSEY COASTAL PLAIN
AND ITS RELATIONSHIP WITH THE BALTIMORE CANYON TROUGH

STOP 1. Raritan Formation overlain by the Pensauken Formation (Pleistocene?).
The sands and clays of the Raritan represent continental and coastal marine sediments deposited adjacent to a transgressing sea. The marine facies of the transgression is encountered in coastal plain wells. The subsurface marine unit is called the Bass River Formation.
Pensauken Formation 5-10 feet
dark yellowish-brown sand and gravel. Large scale steeply dipping cross-beds represent slip faces of fluvial bars. Approximately 50 yds. to the west a fining upward sequence is present. Gravel and lithic fragments are present at contact with Raritan Formation.
Raritan Formation (Woodbridge Member) 65 feet
interbedded sand and clay with numerous siderite and iron oxide cemented sand layers. Two directions of planar cross-bedding can be observed. The cross-bedding probably represents sand waves of a meandering stream or of intertidal currents. Marine fossils are present in some of the sand layers. 30-40 feet.
sand and clay containing abundant carbonized wood. 5 feet.
dark-gray clay and silt, sharp contact with overlying unit. Fine bedding (0.5 mm) composed of clay·silt laminations. 20 feet.
Correlation: Plant fossils and palynological remains in the Raritan indicate a Cenomanian to Turonian (Washita to Eagle Ford) age. Marine fossils (planktonic foraminifera) of a similar age occur in the Bass River marine facies in N.J. coastal plain wells.

STOP 2. Magothy Formation overlain by Pleistocene? sediments.
The Magothy represents estuarine sediments deposited in front of the advancing Merchantville sea. This exposure represents an intertidal sequence of tidal delta sands and lagoonal clays.
Pleistocene? 1 1/2 feet
Sand and gravel
Magothy Formation 45 feet
dark gray sands and clays with carbonaceous rich layers, uniformly cross-bedded sands, intermixed flaser bedding and layers of rip-up clasts. 29 feet.
dark gray laminated clay which laterally on the east side of exposure grades into interbedded sands and clays, carbonaceous rich layers. 8 feet.
dark gray alternating sands and clays. 8 feet.
Correlation: Palynological studies indicated that the Magothy is Santonian in age. This suggests that the Coniacian is absent due to disconformity. This is confirmed in the subsurface on the absence of marine assemblages of Coniacian age.

STOP 3. Woodbury, Merchantville, and Magothy Formations.
The Merchantville Formation represents the second major transgression in the Upper Cretaceous sequence of New Jersey. Subsequent transgressions and regressions of the Cretaceous appear to have fluctuated about the Merchantville strandline.
Woodbury Formation 5-10 feet
dark gray micaceous clayey silt
Merchantville Formation 12 feet
dark gray to greenish black, uniformly bedded sandy silt and clay to sandy clay. Glauconite, mica, and siderite are abundant throughout. Many molds of molluscs are present.
Magothy Formation 8 feet
dark gray alternating fine sand, silt, and silty clay. Rare Ophiomorpha burrows.
Correlation: Ammonite species (Scaphites hippocrepis and others) found in the Merchantville in outcrop date this formation as early Campanian (Taylor) in age. In the sub-surface marine assemblages (planktonic foraminifera) of Santonian (Austin) to early Campanian age are present in the Merchantville thus demonstrating its partial equivalence with the Magothy.

STOP 4. Wenonah Formation overlain by Mt. Laurel, Navesink, and Redbank formations.
The base of the section is exposed in the lower excavation and the upper part is exposed in the higher excavation behind the gymnasium
The sedimentary units at this stop and the next were deposited during a regressive-transgressive-regressive cycle. Bedding characteristics and trace fossil morphology position these units in a marine profile of the transgressive-regressive cycle. See fig. for a composite section.
Redbank Formation (Sandy Hook Member) 15 feet
dark gray, very micaceous; argillaceous, feldspathic, fine quartz sand with disrupted sandy laminae and occasional small-scale cross-laminae. Thick-bedded with mottled texture. Contains sand-filled burrow tubes and the trace fossil Zoophycus.
The above features suggest that the Sandy Hook was deposited in an inner shelf environment not far from the shoreface.
Navesink Formation 20 feet
dark gray clayey, silty, glauconite sand. Burrowed mottled. Contact with the overlying Sandy Hook is gradational. The basal 2 feet of the Navesink contains abundant molds of megafossils and rounded pebbles. Megafossils include large bivalves, gastropods, and phragmacones of belemnites.
The Navesink represents the typical glauconitic shelf facies of the Cretaceous of New Jersey. Paleo-bathymetric indicators (various fossil groups and sediment characteristics) suggest deposition under mid-shelf conditions.
Mt. Laurel Formation 27-33 feet
Thin to medium bedded light gray to white fine to medium sand with thin chocolate brown silt and clay layers. The sand is well-sorted, angular, and slightly glauconitic with dark micaceous laminae. Tabular planar cross-bedding is common in the sand beds. The beds range in thickness from 2-3 inches at the base of the section to 4-6 inches at the top. Maximum thickness is 15 inches. Common broad shallow trough cross-bedding suggests shoreward migration of lunate megaripples. The paleocurrent direction is bimodal, being northwest and southeast. The predominate direction is to the northwest (onshore).
The upper 6 feet is bioturbated and consists of a poorly sorted clayey sand and containing rounded pebbles, abraded fossil molds, and glauconite. Glauconite infills burrows in the upper 3 feet.
Vertical cylindrical burrows of the trace fossil Ophiomorpha and cylindrical to rod-shaped burrows of the trace fossil Asterosoma are present in the lower 20 feet of the section. From about 15-20 feet above the base large robust vertical cylindrical and ellipsoidal horizontal burrows of Ophiomorpha predominate. Thalassinoides also occurs within this interval.
The sedimentary characterisitics and the trace fossil associations indicate that the lower 10 feet of the Mt. Laurel Sand was deposited in a transitional zone from offshore (innermost shelf) to shoreface (just below the surf zone). The interval from 10-20 feet above the base represents lower shoreface deposition. The uppermost 6 feet of the Mt. Laurel may be a lag deposit related to deposition of the overlying transgressive Navesink.
Wenonah Formation 8 feet
gray clayey, slightly glauconitic, micaceous, fine quartz sand. Burrowed mottled with indistinguishable bedding. Occasional large clay-filled subvertical burrows (Asterosoma) and Zoophycus
The Wenonah represents an inner shelf facies related to a minor regression prior to the Navesink transgression.

STOP 5. Redbank Formation (Sandy Hook and Shrewsbury Members).
The basal part of the section is exposed behind the Ern Construction Co. and the upper part is exposed above and just beyond in a long excavation.
Continuation of the section from Stop 4. It represents regression shoaling after the Navesink transgression.
Redbank Formation (Shrewsbury Member) 25 + feet
Light gray to white, micaceous, feldspathic, mostly well-sorted fine to medium quartz sand. The lower 10 feet is slightly silty. Occasional thin clay horizons define inclined bedding which represents forset beds of a prograding sand body. Planar cross-stratification occurs within the forset beds. Both dip south-westward.
The trace fossil assemblage includes vertical cylindrical and horizontal ellipsoidal Ophiomorpha, rod-shaped Asterosoma, and Chondrites.
Redbank Formation (Sandy Hook Member) 15 feet
Dark gray, very micaceous, argillaceous, feldspathic, fine quartz sand. Mottled texture with sand-filled burrow tubes and the trace fossil Zoophycus. The large light-dark mottled shapes are caused by weathering related permeability

STOP 6. Navesink Fm overlain by Redbank Fm (Sandy Hook Member).
Turn right into parking lot just beyond small bridge. Poricy Park fossil beds area. Walk along path to stream bank.
In contrast to the Navesink at Stop 4, at this locality the formation is richly fossiliferous with skeletal material.
Redbank Formation (Sandy Hook Member) 25 feet
Dark gray, micaceous, feldspathic, fine to medium quartz sand. Glauconitic in the basal part which contains microfossils and small megafossils.
Navesink Formation 15 feet
Greenish-black. clayey glauconite sand. Several shell layers are present. The oysters Exogyra, Pycnodonte, and Ostrea; the brachiopod Choristothyris; and the belemnite Belemnitella are well-preserved and common. Molds of various molluscs are common and an extensive well-preserved epibiont bryozoan fauna is present. Microfossils include foraminifera, ostracodes, coccoliths, and dinoflagellates.

Optional STOP. Type locality of the Tinton Formation
Tinton Falls. Turn left and immediately park by restaurant. Walk behind restaurant.
Type locality of the Tinton Formation, the only indurated unit within the Upper Cretaceous section. The formation is very limited in its geographic extent, disappearing within a short distance along strike to the southwest and in a downdip direction.
Tinton formation 22 feet
Brownish green, argillaceous, quartz and glauconite sandstone interbedded with layers and lenses of gray claystone. Molds of megafossils of gastropods and pelecypods are common. Rare specimens of the ammonite Sphenodiscus occur. A well developed dinoflagellate flora is also present.
The Tinton probably represents an inner shelf facies related to the Redbank regressive facies. It is latest Maestrichtian in age.

STOP 7. Manasquan and Shark River Formations
Stop by dirt road on left. Walk along road to riverbank on the right
Manasquan and Shark River Formations overlain by Piney Point (1) and Kirkwood Formations.
A major disconformity is present here wherein the middle and upper Eocene and the lower Oligocene is missing. More of the Eocene and the Oligocene is encountered in the subsurface, however. Marine deposition that began in the late Cretaceous continued in the early Tertiary. It ended during late Eocene time with a large scale regression. The overlying transgressive Piney Point was deposited under inner shelf conditions on an eroded Eocene surface. The basal Kirkwood is probably a shoreward facies of the Piney Point.
Kirkwood Formation 6-7 feet
Chocolate brown clay 5-6 feet
Piney Point Formation ?
Brown, medium to coarse quartz sand 1 foot
Shark River Formation (Squankum Member) 6 feet
Cream to gray brown, argillaceous, glauconite sand. Upper 1-3 feet indurated. Numerous molds of Molluscan megafossils, plus sharks teeth.

7: COASTAL DYNAMICS AND ENVIRONMENTS ON SANDY HOOK, NEW JERSEY
Norbert P. Psuty and Lindsay Nakashima
Center for Coastal and Environmental Studies
Rutgers University
New Brunswick, New Jersey
George Theokritoff
Newark, New Jersey
Sandy Hook is a complex and compound recurved barrier spit located at the northern end of the ocean shoreline of New Jersey (Figure 1). The spit is formed from the northerly transport of beach material derived from the erosion of beaches extending approximately 40 kilometers to the south. The shoreline of Sandy Hook consists of several distinct segments with different rates and forms of development. The spit system may be conveniently broken down for analysis into a set of subsystems, each with differing shoreline orientations to the approach of ocean swell and each experiencing different equilibrium conditions. These subsystems, or beach segments are identified on Figure 1 as numbers 1 through 7. Certain beach subsystems may be further divided into subunits, identified by lower case letters on Figure 1. Each of these experiences slightly different shoreline development. These smaller subunits are strongly affected by man-made beach protection structures. The effect of these structures in producing longshore movement of sediment through the spit system is considerable, as revealed in the conspicuous erosion downdrift of the beach protection structures in Segments 1 and 50
The majority of high energy deep water waves approach the region from the east-northeast and east (Saville, 1954). However, wave refraction on the in-shore portion of the continental shelf causes the shallow water waves to approach from the east-southeast (Fairchild, 1966). This region is also subject to the effects of mid-latitude and tropical cyclones, as well as to ocean swell generated by winds far out in the Atlantic Ocean. On the bayside of the spit, the limiting variables of wind speed, duration, and fetch distance favor wave generation from the northwest. Evidence of the importance of these northwest winds is seen in the orientation of bayside beaches perpendicular to this compass direction and also in micro-spit development to the south of these beaches.
The spit platform, delineated by the 6-foot, 12-foot, and 18-foot contours, is the subaqueous extension of the headland beach upon which the spit ridge (beach and dune system), has formed. The platform extends out a considerable distance on the bayside and has a filtering effect on the higher bayside waves during low tide. This condition is most pronounced when strong northwest winds occur. These winds generate high energy waves and blow water out of the bay. During such periods, spilling waves may occur across the width of the shelf and a considerable amount of material may be moved alongshore within this broad surf zone. However, the presence of deep coves downdrift of Segments 4 and 5 prevents significant transfers of sediment between segments by this mechanism. False Hook Shoal appears to be the seaward extension of the spit platform formed by ebb tidal currents passing the distal portion of the spit. This shoal affects wave refraction and thus controls shoreline orientation and beach development on Segments 2 and 3.
Table 1 reveals the magnitude of beach processes within each of the subsystems. Table 2 identifies the amount of shoreline change which occurred within each segment from 1943 to 1972. The two tables reveal that bayside beaches are retrograding at surprisingly high rates. This is due to a reduction in the quantity of sediment being passed to downdrift segments, and to higher wave steepnesses.
The differences in response to changing wave processes on oceanside and bayside beaches at Sandy Hook have been discussed in detail in Nordstrom (1975). It was concluded that bayside beaches (Segments 4 through 7) appeared to be more in equilibrium with storm conditions than oceanside beaches (Segments 1 through 3). Lower bayside wave energies occurring between storms have little effect on profile development, and foreshore slopes inherited from previous storms undergo minor change. There is little or no deposition between storms. The rate of return is too low to provide adequate protection against dune erosion during the next storm, and dune and foreshore erosion will continue. On the oceanside, in contrast, long, high energy, constructive waves occurring between storms rapidly restore the sediment. These deposits provide a buffer zone to protect the beach and dune against the direct attack of storm waves. The net displacement of the shoreline, therefore, is reduced because of the beach recovery between storm periods.

7: COASTAL DYNAMICS AND ENVIRONMENTS ON SANDY HOOK, NEW JERSEY

Entrance gate to Sandy Hook
Entrance gate to Sandy Hook Unit of Gateway National Recreation Area. Proceed straight (north) on Hartshorne Dr. Segment la. Seawall to the right (east) was constructed at the turn of the century and fronts the narrowest portion of the spit.

Northern terminus of a seawall and groin field
Enter parking lot on right (east) and walk out to seawall. Segment 1a. This represents the northern terminus of a seawall and groin field that extends 8.5 miles (14 km) southward. Beaches in this segment are either non-existent or very narrow. High wave energy, a low littoral drift rate, and excessive downdrift erosion combine to produce a negative sediment budget.

Segment 1b.
At this point the road parallels the most critical zone of erosion on Sandy Hook. The beach here is narrow and forms a log-spiral in plan. Recent beach nourishment and sand bag dike operations have been employed as shore protection measures. Note the absence of dunes and the presence of over-wash deposits on left (west) side of the road.

Segment 1b. Site of bath house
Segment 1b. Site of bath house destroyed by storm activity in February, 1978. Parking lot forms on extensive impervious surface which facilitates back-barrier flooding.

Visitors Center
Turn right (east) into National Park Service Visitors Center parking lot and walk out to beach. Segment lb. Regressive log-spiral shoreline of Segment 1b and offset terminus of seawall in Segment la are evident in a southward view. This Segment experiences cyclic beach response and very high erosion rates (Table 2). Ocean swell and wave-induced currents are dominant processes. Sands on the oceanside are well-sorted and medium size. Beach cusps area frequent occurrence. The site of a second bath house lies 100 yards (30 m) to the north.

South Fishing Beach
Bear right (east) on gravel road to South Fishing Beach. Segment 2a. This Segment primarily responds to waves and wave-driven currents, and experiences relatively high storm and swell energies. Backshore features a natural dune belt. Beach is wider than that found in Segment 1.

Battery Gunnison
Enter gravel parking lot on right (east) at Battery Gunnison and walk to beach. Segment 2b. The nearshore in this Segment is characterized by a longshore bar which shelters the beach under high wave conditions. Cyclic beach response is solely associated with major storms. Ocean waves and wave-driven currents are dominant processes. The entire Segment is backed by a natural dune system. The beach north of the timber groin is used as a beach fill borrow area for nourishment of Segment lb.

Lighthouse to the left
Lighthouse to the left (west) marked the terminus of the spit in the 18th century.

Segment 3.
Turn right (east) on gravel road to North Fishing Beach parking lot and walk to beach, Segment 3. This beach is sheltered by longshore bars and False Hook Shoal. Net deposition-occurs in this Segment which is effected by the complex interaction of waves (ocean and bay) and currents (tidal and wave-induced). The shoreline in this Segment is not straight but displays a concave seaward geometry as one walks northward. The tip of the spit exhibits the highest dunes and an ebb shoal which forms False Hook Shoal. Spit growth occurs to the northwest but is limited by annual dredging of Sandy Hook Ship Channel.

Segment 5a.
At this point a seawall fronting large houses (Officer's Row) is visible. Tidal currents and bayside waves are important processes. Bayside Segments possess shore protection structures and deep coves which inhibit sediment transfers to adjacent Segments. The highest bayside waves are experienced here and Segment 4 to the north. Segment 4 lies under jurisdiction of the U.S. Coast Guard and is a restricted area.

This is the terminus of the seawall in Segment 5.
The formation of a log-spiral beach is occurring immediately to the south of the seawall. This Segment is undergoing the greatest amount of erosion due to locally generated swell and storm waves. A peat bed is exposed on the low tide foreshore and a transgressive sequence is forming over the salt marsh deposit. Sediment eroded from this beach is important to development of a spit farther south.

Segment 6a.
The aforementioned accreting spit can be seen to the right (west) across Horseshoe Cove. Wave activity and tidal currents are less important here than other bayside sites. The beach is extremely thin and erosion is threatening the road adjacent to the seawall.

Segments 6a and 6b.
Limited access parking area. This Segment experiences net erosion. Sediments are continuously eroded from behind the timber bulkhead and a deep cove updrift limits input of sediment. The southern extent of this Segment exhibits a small flood tidal delta formed in a breach at Spermacetti Cove. Sediments in this Segment are primarily coarse sands and lag gravels.

Segment 7.
This permits a view of Plum Island and the Shrewsbury River. As would be expected, the lowest wave energies are encountered here. Plum Island is undergoing erosion with accretion occurring at both ends. Such accretion favors formation of a salt marsh habitat. Coarse sands and lag gravels are present. Much of the sediment composing this island is fill, including the land that connects it to Sandy Hook.

8: LANDSCAPE FEATURES AND BOG IRON ORE DEPOSITS OF THE PINE BARRENS
Emily W. B. Russell
Rutgers University
New Brunswick, NJ
Edward Krug
Department of Soils and Crops
Cook College, Rutgers University
Introduction
The New Jersey Pine Barrens, which include the designated Pinelands National Reserve, are a large, unique combination of ecosystems which in general are coextensive with a Tertiary (Miocene) surficial formation, the Cohansey sand (Fig. 1). They thus represent an area where surficial geology exerts a large effect on vegetation. In this general climatic region the natural vegetation is usually deciduous, primarily oak (Quercus spp.) forest (Braun 1950). However, in the Pine Barrens, the forests have a much larger percentage of pines (Pinus spp., esp. P. rigida), in places even to the exclusion of any tree-size oaks. Minor topographic variation plays an important role on the variability within this ecosystem. Lowland forests, mainly of cedar (Chamaecyparis thyoides), pitch pine (Pinus rigida) or hardwoods (Acer rubrum, Nyssa sylvatica, and Magnolia virginiana), grow where the water table is near the surface, and dwarf pines grow on topographical highs, usually on a slightly different geological substratum, the Beacon Hill formation.

8: LANDSCAPE FEATURES AND BOG IRON ORE DEPOSITS OF THE PINE BARRENS

STOP 1. Pedogenic Bog Iron Formations
Pedogenic Bog Iron Formations Of Pigeon Swamp, South Brunswick.
Unmined bog iron site that shows the relationships of podzol soils, surface water quality, and pedogenic bog iron formation. This is posted private land. Viewing of bog iron is best achieved by walking in the stream itself. The south bank of the stream is disturbed by dredgings (parts of this stream were straightened) and by bedding of long-abandoned dirt roads.

STOP 2. Bog Iron Dump, Mount Holly
The remnants of an iron ore dump still exist under two large trees growing at the edge of the North Branch Rancocas Creek, Iron Works Park, Mount Holly. Both lake and bog ores are in these piles. The ores were presumably used by the Mount Holly Iron Works which was destroyed in 1778 by the British Army and never rebuilt.

STOP 3. Water Quality, Soils, And Topography
Water Quality, Soils, And Topographic Relationships To Pedogenic Bog Iron Formation Of Rancocas State Park, Hainesport.
Soils are extremely acidic, pH approximately 4, but are not podzols, the vegetation is typical of that of the Pine Barrens. Water draining this land is clear, not organic stained or rusty, not participating in significant iron cycling. At low tide the relationship of pedogenic bog iron formation to topography is easily observable. River water is the source of iron, the brown river waters coming from the upstream podzols. Shallow groundwaters of the Pine Barrens (podzol zone) are also brown (and ferruginous). Therefore this site is unique in that pedogenic bog iron is visible on the surface because of tides and formed in an area where there is little doubt that the local groundwaters can not supply iron for deposition. This iron deposit is unusual in that ocherous earth forms both above and below the ironstone layer whereas it usually only forms below. This sandwiching effect is probably due to the tidal variation.

STOP 4. Typical pingo
In the middle of the field on the south side of the road is a typical pingo, a common local land feature. Similar structures with raised edges are formed in areas of permanently frozen soils in the Arctic, by a complex process of thawing, erosion and deposition (Tedrow, 1969). The permanently wet center here prevents cultivation and is thus seen by the brush growing there. Pingos appear to have attracted Indians and frequently have artifacts on their raised edges. They may also account for the existence of small bogs where the ground water table is well below the surface, since they are usually underlain by clay lenses.

STOP 5. Harrisville Pond.
This is the site of an old iron works. Evidence for mining of bog iron ore can be seen along the river. Much of the lowland forest here is pitch pine, with a canopy of almost pure pine. The understory is dense and includes many shrubs of the heath family (Ericaceae), for example sheep laurel (Kalmia angustijolia) and blueberry (Vacdnium spp.). These lowland areas occur often along streams with low levees, the same conditions conducive to the formation of bog iron ore.
The Oswego River here has a drainage area of 64 mi2 and discharge of 18.7 in/yr (Pinelands Commission, Draft· Comprehensive Management Plan, June, 1980).
Just up on the left is an exposed soil profile and upland forest. The canopy here is mainly pitch pine (Pinus rigida) but also includes the typical blackjack oak (Quercus marilandica). Tall shrubs are mainly scrub oak (Q. ilicifolia); other prominent shrubs are black huckleberry (Gaylussacia baccata) and lowbush blueberry (Voccinium vacillans). The litter is thin,and scattered where there have been frequent fires. Sandiness and leaching show in the podzo!. Without fire the upper humic horizon would be deeper. Below this is the bleached zone. A zone of accumulation of the leached iron and humic compounds may form below this, just above the parent material or Cohansey sand. In places this yellow sand is brought to the surface and deposited on the white sand by ants.

STOP 6 Oswego Lake (Penn State Forest).
There are two types of swamps in this vicinity, hardwood and cedar. Note the pointed tops of the cedar trees (Chamaecyparis thyoides) compared with the flat tops of the pines. The short gradation between these two indicates the small changes in elevation associated with the change from upland to lowland vegetation. The understory here includes highbush blueberry (Vaccinium corymbosum) and swamp azalea (Rhododendron viscosum). In openings the sphagnum moss mat also includes the tiny plants of cranberry (Vaccinium macrocarpon). Both of these species of Vaccinium are grown here commercially.
In places in the cedar swamp, red maple (Acer rubrum) and black gum (Nyssa sylvatica) form an understory which may eventually replace the cedars. Such an area of hardwood swamp can be seen shortly downstream from Oswego Lake. The red maple and black gum are here accompanied by sweet bay (Magnolia virginilma). Continue on past the lake.

STOP 7. Pine Plains
These dwarf forests are the most distinctive feature of the Pine Barrens. There are no other such forests approaching the areal extent of these elsewhere in the world. Stunted, many-trunked blackjack oak and pitch pine dominate the low canopy. Broom crowberry (Corema conradil), a species which reaches its southern geographical limit in the Pine Barrens, is found here. It is a species which probably migrated south along the exposed coastal area during the Pleistocene and has since been isolated from northern populations by the rise in sea level. Note also that the soil here is coarser than in the other upland site, a characteristic of the Pine Plains which may increase dryness and thus fire frequency.

STOP 8. Oyster Creek rest area.
Oyster Creek with 7.43 mi2 of drainage area has a flow of 51.4 in/yr. Compare this with the values for Oswego River. This difference is caused by interbasin transfer of ground water. Much of the water that falls in the Oswego River watershed soaks quickly down into the aquifer below the bed of the river and flows past it, to come to the surface eventually in such streams as Oyster Creek.

9: LATE WISCONSIN-HOLOCENE HISTORY OF
THE LOWER HUDSON REGION:
NEW EVIDENCE FROM THE HACKENSACK
AND HUDSON RIVER VALLEYS
Stephen P. Averill
Fairleigh-Dickinson University
Rutherford, N.J.
Pascack Valley Regional High School District
Montvale, New Jersey
Richard R. Pardi and Walter S. Newman,
Radiocarbon Laboratory
Department of Earth and Environmental Sciences
Queens College, City University of New York
Flushing, New York.
Robert J. Dineen
New York State Geological Survey, Museum
Science Service State Education Department
The study area (Fig. 1) is the central and upper Hackensack River valley of northeastern New Jersey and adjacent New York State with reconaissance study of the surrounding area in Bergen County, N.J. and Rockland County, N.Y. In the text, town names will be in New Jersey unless indicated otherwise. Geologically, the area is the northern portion of the Trias-Jurassic Newark basin where a gently dipping (14°W) homoclinal sequence of Brunswick Formation red sandstones and shales form the deeply scarred bedrock surface. The Palisade sill and basalt lava flows of the Watchungs, interbedded with the Newark series sediments, form prominent topographic ridges in the region. The western slope of the Palisade sill, whose well-studied eastern escarpment forms the Hudson Palisades, is at the eastern margin of the Hackensack Valley. Resistant sandstones of the Newark group form the ridges and cliffs along its western border as well as the divide between it and the parallel drainage system of the Saddle River. The Ramapo fault system slices northeast at the northern terminus of the basin separating it from the rugged Precambrian crystalline mass of the Ramapo Mountain portion of the Appalachian chain. The Hudson River and glaciation have carved an impressive gorge through the Hudson Highlands, The Ramapo River lies in a similar but less spectacular gorge ten miles to the west at Suffern, N.Y. Continental glaciations overdeepened both gorges before overwhelming the Ramapos to push south to their maxima. The deep preglacial Hackensack Valley has been partially overdeepened by glacial ice, then mostly filled by pro-glacial lake sediments (Lovegreen, 1974). The present terrain is gently rolling, with drumlinoidal hills generally aligned north to south paralleling the strike of the bedrock. Essentially glaciation has subdued the preexisting topography, even occasionally reversing it.

We are crossing the Secaucus drumlin.
It is aligned with its long axis N-S. A relatively thin red till overlies this red and gray rock-cored drumlin. Contact metamorphism of the sandstone was observed throughout most of a very large excavation. The Palisade Sill cannot be far below.

Old Lake Hackensack floor
We are crossing the old Lake Hackensack floor now covered by a 3 to 6 meter sheet of sand with the tidal marsh over the sand. The lake covered the "Meadowlands" as far as one can see. The ridges to the east and west formed the shores.

STOP 1. This is the Rutherford rock-cored drumlin.
The Upper Triassic Brunswick formation sandstones and shales are exposed here at the side of the drumlin. Note the copper mineralization. Red drift, sometimes till, sometimes sand and gravel, blanket the drumlin. Some yellow "loam'" may be exposed (if we're lucky). The "loam" here is about 15'cm thick and is loess. This drumlin was at the western edge of Lk. Hackensack.

Proceeding onto the old lake bed surface.
We are leaving the drumlin and proceeding onto the old lake bed surface. As you drive north on Rt. 17, note what was the steep western shoreline of the lake. A deep preglacial valley exists under Rt. 17. The varves are by far the thickest here along the western side of the Hackensack Valley (Lovegreen, 1974).

Reeds' clay pits for 2550 varves
At the center of the valley close to the Hackensack River are the former brick yard clay pits from which Reeds' extracted and counted 2550 varves.

Sandstone ridge
We are now crossing one of the sandstone ridges that form the low divide between the Hackensack and Passaic valleys.

Near distal end of outwash fan
We have just passed through the divide between the Hackensack and Saddle Rivers and are near the distal end of the outwash fan associated with the Ridgewood kame group. As we proceed north on Rt. 17, notice the slope of the outwash plain.

Northern-most of Lake Hackensack red varves
This is the northern-most known location of Lake Hackensack red varves in the Saddle River valley. (G.S. Pkwy boring records.)

STOP 2. Mastodon display and rest stop.

STOP 3. Crest of the Ridgewood kame group.
Walk back to kame. South side of kame shows stratified drift. This used to be a gravel pit. We are told that much coarser gravel was removed from here than is presently exposed. Return to north side of kame. Clean off the face and note the vertical sand layers with minor asymmetrical folds. At the top of the exposure is a layer of fine to medium sand capped with yellow loess under the top soil and vegetation. Return to bus. <br

STOP 4. Musquapsink Brook
Exposure of red till in the banks to the south. Bedrock in stream to the north.

STOP 5. Woodcliff Lake kame delta
We will have to walk along the causeway. Please watch the traffic. This is the Woodcliff Lake kame delta that built into the proglacial lake in the Musquapsink Valley. Note the very sharp drop in elevation below the dam.

Till capping outwash on the island
As we ride, note the till capping outwash on the island in the lake. It forms a small dark slightly overhanging layer at the top.

STOP 6. Woodcliff Lake reservoir
Enter the Woodcliff Lake reservoir of the Hackensack Water Co. NO TRASH DROPS PLEASE. We will examine the wave-cut cliff exposure of yellow-brown till over readvance outwash. There is less than 1 meter of till here. One-tenth of a mile west, immediately west of Pascack Rd., the tightly packed red cobble till of the Lake Hackensack glaciation lies below the readvance outwash.

STOP 7. Atkins Glen Park
This lovely glen is a preglacial valley (at least pre-Woodfordian) cut across the Brunswick fm. strata at right angles to the bedrock strike. This valley contains red till and near the top is overlain by the yellow-brown till. It is very close to the farthest north natural exposure of the red till. The valley was exhumed in post-glacial time when a large and deep lake left by the ice, in what is now the Bear Swamp section (Park Ridge 7 1/2 minute Quadrangle), was drained by downcutting.

We have crossed into the Saddle River basin.

STOP 8. Side of a Drumlin
Turn RIGHT into gravel surfaced area of pit. It is across the street from the Cemetery of the Ascension. The exposure is in the side of a drumlin. The yellow-brown till is well exposed here. A strong bimodal till fabric can be measured here and fissility of the till was noted in two steep-faced exposures.

STOP 9. The River Vale Road drumlin
The Yellow-Brown till is 2.7-4 meters thick here. Red till is below. View to the east (over golf course) is the line of River Vale kames that form a north-south ridge to the east of River Vale Rd. until they join the Old Tappan moraine at their southern end. The west slope of the Palisades is across the Hackensack Valley in the distance.

Kettle bog areas
We travel through some kettle bog areas before reaching the old (landscaped) kame crest line. The Old Tappan moraine is ahead of us (south). The present reservoir is the location of post-glacial Lake Tappan. Note the ice-pressed terrain on the back-side of the moraine dam. Many large kames were removed from here during construction of the reservoir. Ultimate drainage, resulting in that catastrophic flood, was through the present Hackensack River drainage exit at the dam.

Steep-sided kettle
As we drive up the back slope of the moraine ridge, we can see a steep-sided kettle to the left of the road and just north of the small cemetery.

STOP 10. Old Tappan Rd. and Ledson Parkway
Old Tappan Rd. and Ledson Parkway are on the sandy outwash plain. Erosion has cut a gully here and has revealed the yellow-brown till of the moraine at the base of the ravine.

STOP 11, Observe excavated end of moraine.
It is mostly stratified drift here.

STOP 12. Outwash capped by Tappan till
This is a great sequence of outwash capped by a thin layer of yellow-brown Tappan till. The owner has suddenly died and at this writing we are not sure whether we will be able to enter legally.

STOP 13. Tallman Mt. State Park. Lunch.
After lunch Dineen will discuss the geology of the adjacent Sparkill Gap. Averill will discuss the importance of the Gap to the Woodfordian history of the Hackensack Valley. Newman will discuss the origin of the Piermont salt marsh below and the rise of sea level. For the uninitiated, Dineen and Newman will demonstrate their seismic and coring procedures.

Norwood kame grouping
Road begins to increase in elevation at the Norwood kame grouping and generally runs along the crest.

Norwood kames history
The Norwood kames were constructed into glacial Lake Hackensack and were later buried by the readvance Tappan till glacier.

STOP 14. Kame
Enter new development on north side of road. Walk up hill to top.
Kame is constructed of red coarse cobble outwash and has patches of overlying yellow-brown till.

Outwash plain, then erosional slope
The first slope is the outwash plain. There is then a break in the slope and the slope increases. This is the erosional slope first cut during the drainage of glacial Lake Hackensack.

STOP 15. Mastodon site
This is the Norwood portion of the Oradell Reservoir. This is where the mastodon remains were found. The large (3 meter) diabase boulder can be seen. Discussion....

You are on the outwash plain of the Old Tappan moraine.

Ascending the River Vale collapsed moraine outwash plain.

Incised Pascack Brook to left
Note the flood plain of Pascack Brook to the left (West). It cut deeply into the outwash plain south of the Hillsdale heads-of-outwash.

Going down hill into the area of collapsed moraine.
We have crossed Cleveland Ave. head-of-outwash and are going down hill into the area of collapsed moraine. At the end of Cedar Lane at the "T". is a new Condominium complex. These five story pre-cast concrete structures were built directly on glacial Lake Hackensack red varves. No pre-construction preparation was necessary as they (the varves) were already in a pre-consolidated state.

Crevasse channel outwash feeder
The 1st street on the right (Ruckman Ave.) is the crevasse channel outwash feeder. It can be seen on the left (south) across from Ruckman Ave. It is composed of medium clean sand with occasional large boulders. Piermont Rd. cuts through the crevasse filling in a small stream valley (more on that later).

Everdell Ave. along the crevasse filling.

Kinderkamack Road drumlin
We proceed down the hill to the flat valley floor. Ahead of us is the Kinderkamack Rd. drumlin, one of the largest in the area.

STOP 16. Beechwood Park, Hillsdale, N.J.
Walk into park. Note the kame on the west and the large kettle bog. The bog is also found south of Hillsdale Ave. beyond the confines of the Park. B.P.1 boring was made on the southeast side of the bog and penetrated to the bedrock floor of a deep valley 55 ft. down. Surface elevation of the bog is 50 ft. ASL. B.P.2 was sited 10 m south of Hillsdale Ave. almost due south of B.P.1. B.P.3 was sited east of B.P.2 just east of the sewer cut in the deepest part of the kettle.
Note the stratigraphy as shown in Fig. 10. Discussion.
The Hillsdale head-of-outwash is immediately south of us. A small, apparently very short-lived, proglacial lake formed behind the dam and between the drumlin on the west and the crevasse filling on the east. As the ice retreated, the eastern ridge was breached at Piermont Rd.

Proceed south on the outwash plain of the Hillsdale heads-of-outwash.

The first valley we cross is the Pascack Brook.

Large valley drained by Musquapsink Brook
Farther south, after we pass through "5 Corners" in Westwood, we drop into a very large valley drained by the now tiny Musquapsink Brook. This is the valley cut by the draining of proglacial Lake Musquapsink. The Woodcliff Lake kame delta was constructed into this lake.

Proceeding south in Emerson we are still on the outwash plain.

Oradell drumlin
In Oradell, near the Xerox building, more of the same but on the west is the large Oradell drumlin; rock-cored and coated with red till. Lake Hackensack red varves were encountered at the Xerox site under the outwash sand. Yellow "loam" loess as much as 30 cm thick overlies the area to the south. Man's activity has removed much of the loess.

10: ECONOMIC GEOLOGY:
NEW JERSEY HIGHLANDS
General Introduction and Road Log
Andreas H. Vassiliou
Newark, New Jersey
The New Jersey Highlands province comprises the centermost portion of northern New Jersey, extending 96 Km northeasterly across the state and ranging in width from 16 to 40 Km. It is flanked on the northern side by the Valley and Ridge province and on the southern side by the Triassic Lowlands of the Piedmont province. The province, which is part of the Reading Prong of the New Jersey Highlands is essentially a belt of Precambrian crystalline rocks with certain narrow belts of folded and in-faulted Paleozoic sedimentary rocks. The three articles that follow this general introduction contain specific information on these rock types and their relationships.
The Precambrian rocks of the New Jersey Highlands have been hosts to several commercial mineral deposits. Historically, the magnetite iron ore deposits are of unique importance. These deposits have been mined since at least as early as 1710 (Buddington, 1957), perhaps the oldest iron mining in the United States. Geologic and other information concerning the major magnetite deposits of the Highlands was first outlined by Bayley (1910). For several years during the third quarter of the nineteenth century, New Jersey was the biggest producer of iron ore in the United States. Of the 136 mines active in 1880, none are operating today, However, some of the now abandoned mines are still accessible. During this field trip, John Puffer will lead us through two such mines: the Andover-Sulphur Hill Iron Mines (STOP 2) and the Edison Magnetite Deposits (STOP 3).
Interest in the mineralizatoin of the Franklin area has been worldwide and has continued, unabated, for more than a century. In certain rare cases, a significant accumulation of a wide variety of elements is possible in certain areas of the earth's crust, resulting in the formation of a large number of minerals, some of which are unique or exclusive to the area. Kostov (1968) lists only four such localities in the world, with the Franklin area being one of them. The Franklin deposits are enriched mainly in manganese, iron, and zinc, but the combination of the silicate-oxide ore minerals with numerous associated gangue minerals is unique and generally unknown elsewhere. Kushner (1970) compiled an abbreviated manual of Franklin minerals and listed about 200 species. Some of these minerals (e.g., franklinite, zincite, etc.) are either unique to Franklin or are rarely found elsewhere. Today, except for the mining operations at Sterling Hill and at the Farber White Limestone Quarry on Cork Hill Road, all of the mining activities at Franklin have ceased. Bob Metsger, who has been the chief geologist at the Sterling Hill Mine for several years, will lead us through the mine area and describe the occurrence and origin of this classic deposit (STOP 4). Mineral conecting will be available at the mine dump. However, those who are interested may also visit the Trotter and Buckwheat dumps for additional mineral collecting upon payment of a small fee.
The search for uranium in the 1950's is responsible for the greatest metal hunt in the history of the world. The New Jersey Highlands province was included in this hunt, and in 1955 a series of geiger counter hot spots were discovered along the perimeter of a large pegmatite near Cranberry Lake by Mr. Edward Koral and the New Jersey Geological Survey. In 1959 the Byram Exploration Minerals Company put down a vertical shaft on one of the hot spots and named the deposit the Bemco Mine. Throughout the summer of 1959 some uranium was recovered and shipped out (about 95 tons of ore), but the rare earth values of the ore were overlooked at the time. The Bemco Mine, also known as the Charlotte Mine, is located on land now designated as Green Acres and is, of course, inactive. The ore represents a highly unusual mineral assemblage of metamict minerals (e.g. fergusonite, uranothorite, zircon), and is of interest as a good example of hydrothermal mineralization relating to the intrusion of a pegmatite into the metamorphic host rocks. Diamond drill cores studied by Williams (1967) define the ore zone up to a depth of 30 meters. On STOP 1 of the trip, this writer will point out the relationships between the ore and the associated rock units and discuss the origin of the deposit.

10: ECONOMIC GEOLOGY:

STOP 1. Bemco Mine
Led by A. H. Vassiliou
(about one hour). At this point the dirt road has small parking area on the right whose path or trail (uphill) leads to the BEMCO MINE. Go 420 feet along the trail: "sulfide quarry" to the right, downhill. + 840 feet to "red flag" -turn right down the hill to lower trail (about 50 feet).
+ 350 feet, turn left for mine area.
+ 145 feet, to old shaft.
See attached article on the deposit by A.H. Vassiliou.

STOP 2: Andover-Sulphur Hill Iron Mines
Led by J.H. Puffer
(about one hour). Park off road and follow path or trail (right side of road) to ANDOVER-SULPHUR HILL IRON MINES. See attached article by J.H. Puffer.
You will be asked to sign a waiver before entering the mine property, and are requested to wear a hard hat and safety glasses. Follow the path from the mine gate to an open clearing. The Andover Mine workings including adit portals and an open pit are found along a cliff located south of the central clearing. Highly altered diabase dikes are intruded along the cliff. The diabase is black to dark green, highly chloritized, fine grained rock that has been sheared and mylonitized. The magnetite ore is disseminated in a light gray Quartz-Oligoclase Gneiss. Dark green pyroxene-feldspar gneiss is exposed above the cliff east of the mine. The pyroxene-feldspar gneiss is green (highly epidotized) fine grained, migmatitic, locally calcareous rock. The pyroxene component is diopside. A light buff microcline granite gneiss is exposed along the road just west of the mine.
The Sulphur Hill open pit is located about 400 feet north of the central clearing. The pits are dangerous and are closed to visitors. Most of the rocks found in dumps at the north and eastern edges of the clearing are from the Sulphur Hill Mine. The rock is a magnetite and sulphide rich garnet skarn. Amphibolite is exposed south of the Sulphur Hill Mine. It is recognized by its black hornblende content, and is coarser grained than the pyroxene-feldspar gneiss.

STOP 3: Edison Magnetite Deposit
Led by J.H. Puffer
(about 30 minutes). Park off road (clear area on right). Climb up bank, cross fence, to the EDISON MINE magnetite deposit. See attached article by J. H. Puffer.
Buses will turn around. At the southern end of the open pit (The Old Ogden Mine) there are good exposures of a biotite, sillimanite and magnetite rich phase of a metasedimentary Quartz-Potassium Feldspar Gneiss. Sulfides including pyrite, chalcopyrite, and molybdenite are disseminated throughout the rock but are found concentrated near the south-east corner of the pit. Acid solutions leached through the sulfides have accelerated the alteration of the rock to a sericite rich saprolite. Please exercise extreme caution when approaching the open pit, and be on the alert for poison ivy.

STOP 4. The Sterling Hill Mine, Ogdensburg
Led by R. Metsger.
Here we shall have lunch, go on a mine tour, and then do some mineral collecting at the dump. See attached article on the deposit by R. Metsger.

11: ENVIRONMENTAL GEOLOGY OF THE HACKENSACK MEADOWLANDS
Sam L. Agron
Newark, New Jersey
This trip to the Hackensack Meadowlands District has several purposes:
1. To observe the natural environment of the Meadowlands, the problems and challenges it poses, and to gain some understanding of how the geologic history gave rise to that environment.
2. To see how numerous, complex, diverse, and seemingly incompatible land uses can be carried out harrmoniously and profitably if a region's geology and ecology are adequately understood by planners; and if imaginative engineering, political and economic planning are applied.
3. To inspect several of the major projects that have been erected in the Meadowlands, consider their operational processes and how they impact on the environment and, above all, how geologic constraints were dealt with in designing foundations, etc.
The pioneering work done by the Hackensack Meadowlands Development Commission in planning and overseeing the harmonious growth of the District is unique in this country. A long-blighted area, where land was almost worthless some four decades ago, now contains some of the most valuable acreage in the country. What can be learned here may very well have application elsewhere.

11: ENVIRONMENTAL GEOLOGY OF THE HACKENSACK MEADOWLANDS

West margin of Hackensack Meadowlands.
Schuyler Avenue which follows bluff marking west margin of Hackensack Meadowlands.

STOP 1. (Kearny) Overlook, south end of the Meadowlands.
Panorama (left to right) shows sanitary landfills, more than 100 feet in elevation, over which the first section of the De Korte State Park will be erected; the New York City skyline including the World Trade Center towers (about 7 miles distant); Snake Hill; New Jersey Turnpike; Pulaski Skyway (Routes 1 and 9); and the Bayonne Bridge arch to Staten Island. The southern boundary of the Hackensack Meadowlands District, which is under the jurisdiction of the Hackensack Meadowlands Development Commission, lies about 1/2 mile north of the Pulaski Skyway. The meadowland environment continues south of the District boundary.

Belleville Turnpike descends into Meadow lands.

STOP 2. Tour of HMDC Solid Waste Baling Facility
See text above.

STOP 3. (North Arlington) Schuyler copper mine.
This is the approximate location of the Schuyler copper mine. The shaft was a couple of hundred feet to the NW. The mine was discovered about 1719 and was probably the first copper mine in the United States. It shipped 110 casks of ore from New York in 1721 (Lewis, 1907). Much detailed historical information can be found in Woodward (1944).
The mine was a source of considerable wealth before the Revolutionary War and continued to be worked intermittently until 1865. The primary ore mineral, chalcocite, occurs in unaltered gray arkosic sandstone overlain by red shale and intruded by small, irregular basalt dikes. The major secondary mineral is the bluish-green copper silicate chrysocolla which penetrates the rock along joints and bedding planes.

STOP 4. Panorama of the Meadowlands
Fig. 20 Looking E from Schuyler Ave. (near Carrie Rd.), North Arlington to wetlands in Lyndhurst, N.J. Kingsland Creek, in middle, flows towards the Hackensack River. To the right are landfills and the Sawmill Creek Wildlife Management area.
Overlook showing a panorama of the Meadowlands N of the one in Stop 1. Kingsland Creek, in the foreground (Fig. 20), lies towards the N end of the Sawmill Creek Wildlife Management Area (Fig. 13). The panorama from left to right shows the Meadowlands Racetrack, Giants Stadium, and the Arena; sanitary landfill; twin towers at S end of the Harmon Cove development; Empire State building and mid-town Manhattan skyline behind the Palisades ridge, sanitary landfill, World Trade Center towers are almost in line with Kingsland Creek. The W spur of the N. J . Turnpike is in the middle distance; the E spur passes behind Snake Hill, at the right. Note the wetland dikes.

Descend to Meadowlands.

Copper mine exploration shafts
Bricked-up entrance to copper mine exploration shafts in red beds behind Kuttner Prints plant on left. This is the Lyndhurst Office Industrial Park, one of 11 industrial parks in the Meadowlands. This park includes the Meadowlands Corporate Center and tenants such as Peugeot, Citroen, etc.

Polito Ave. has developed a "wash board" effect
Polito Ave. has developed a "wash board" effect because the road was built directly on the meadow mat, which doesn't support the heavy truck traffic very well.

Cross Berry's Creek.
The very serious mercury pollution problem in Berry's Creek and its environs originated in an industrial plant about 3 miles upstream (see text above). The Creek forms the W boundary of the Meadowlands Sports Complex. whose three major structure loom large on the left.

STOP 5. Meadowlands Sports Complex
(Note: Mileage and routing directions to parking site will be made available by the Sports Authority at time of the trip).

STOP 6. Sewage Treatment Plant
Tour of the plant and new construction in progress. See text above. Opposite this stop, across the Hackensack River in Ridgefield Park, is the Bergen generating station of Public Service Electric and Gas Company (Fig. 21). This plant is in the extreme northeast corner of the Hackensack Meadowlands District. It is a conventional oil-burning power plant, but is also equipped to use coal and natural gas. In 1983 it will also burn garbage from the resource recovery plant to be constructed adjacent to it by Bergen County (Boyd, 1980d). Procedures are employed to minimize thermal pollution of the Hackensack River, to condense spent steam from the turbines for reuse in the boiler.
Several ponds to the northwest of the Sewage treatment plant were clay pits. Little Falls was once the center of a major brick-manufacturing industry.

Two LNG storage tanks to the east

STOP 7. Stone pier S of Sky Harbor Marina
Walk to end of pier for view of Hackensack River (Fig, 22). Sand and gravel storage facility can be seen on opposite (E) shore of the river. in Secaucus. Route 3 bridges cross the river to south. Behind bridge is the Harmon Cove development, our next stop.
Two LNG storage tanks can be seen about 0.7 mile to the NE very close to a superhighway (Fig. 23). Most of the area between here and the tanks has been rezoned for residential use. See text above.

Bridge crossing Hackensack River.
Harmon Cove development on the right.

STOP 8. Harmon Cove Development
Harmon Cove Deve!opment, Hartz Mountain Industries. Secaucus. See text above.
We will leave the bus here and board it at the Twin Towers high-rise condominium at the south end of the development. Start walking along the bicycle and jogging path that winds southward through the area of town houses that stand between Meadowlands Parkway and the Hackensack River (Fig. 24). The top of the 25-story Twin Towers affords a spectacular view of the entire Hackensack Meadowlands District lying on the floor of post-glacial Lake Hackensack. The Manhatan skyline looms impressively beyond the back slope of the Palisades, which marks the eastern border of the District. The Hackensack River can be seen as the central artery sustaining the watery ebb and flow of estuarine life in the wetland habitat. The network of highways includes the Pulaski Skyway, East and West Spurs of the New Jersey Turnpike, Rte. 3, and others. Five highway bridges and six railroad bridges cross the Hackensack River in the District. Landfills towards the SW mark the site of the De Korte State Park. To the north can be seen the Sports Complex, the LNG storage tanks and the PSE & G electric generating plant. Another power plant is at the far south end of the area. Several industrial parks are distributed throughout the District.

Secaucus water tower on right.
The town of Secaucus forms two "islands" inside the Hackensack Meadowlands District (Fig. 6). Its location was determined by the presence of bedrock at the surface, which posed none of the foundation problems found elsewhere in the Meadowlands.

Little Snake Hill on left.

Snake Hill (Big Laurel Hill) on right.
These are diabase plugs which may have served as vents or feeders for the Watchung lava flows. Snake Hill has been largely quarried out for trap rock crushed for use as road metal. It supplied crushed stone for Hartz Mountain Industries. Snake Hill is zoned for residential use (Fig. 4). Because the basalt provides an excellent foundation housing can be built more cheaply here than at Harmon Cove or elsewhere in the District where costly pilings must be used. Low-cost housing has been suggested for the site because the cost per unit would be lower. The site's isolation, however, mitigates against this type of housing.

Sawmill Creek Wildlife Management Area
Sawmill Creek Wildlife Management Area to the right (Fig. 2). This will be part of the De Korte State Park.

12: ENVIRONMENTAL GEOLOGIC TRAVERSE
JOSEPH A. FISCHER
Fees Geosciences Inc., Meyersville, New Jersey
GENERAL CONCEPT
Initially, this trip was going to include a number of stops in the Appalachian Fold Belt, the Highlands, the Newark Basin, the Coastal Plain and right down to New Jersey's barrier beaches. As the detailed plans began to take form, there appeared to be no way to sample in one day, all the varieties of geology that New Jersey has to offer unless one did it from a speeding helicopter. Thus, the route shown on Figure 1 attempts to sample as many different geological environments and concurrent geologic problems as can be "shoved" into a single field trip.
A total of 10 stops are planned (as shown on Figure 1). These are:
1. Route 280 West Orange, road cuts in the First and Second Watchungs;
2. Ridgedale Avenue, Morristown, terminal moraine -- semi-abandoned quarry;
3. Route 202 South of Morristown, Ramapo Fault, hospital across "active" fault;
4. Great Swamp, problems of managing 6,000 acres of wildlife preserve in a suburban environment and how the refuge affects its surroundings;
5. Millington Gorge -- faulted (or erosional) cut through Second Watchung, flooding concerns;
6. Millington Quarry -- blasting and transportation of trap rock in a middle class suburban environment;
7. Bridgewater Township-Route 78 road "cuts" in Second Watchung Mountain, compare with Stop 1;
8. Far Hills -- -Where does the Ramapo go?
9. Bernards Township/Bedminster, proposed 1,500 acre development, variable soil and rock, mostly impermeable soils, mostly shallow rock -- how do you build a new "town"?;
10 . Berkeley Heights -- Whither goest Route 78?

STOP 1. First Watchung
Rather than a stop, this will be a slow drive by (either by direction or limitations of the bus). As the elevation rises from the Northfield Road (State Route 508) intersection with Route 280, the first outcrops seen are of the Brunswick Formation (sandstones). Then Route 280 climbs into a major road cut within the Watchung basalts (First Watchung). The basalt cut is steep and the blocky, columnar structure of the lower basalt can be observed early. At higher elevations, the cut is in ropey and pillow lava. Along the cut in the Second Watchung, while it is still at a high angle, several failures can be observed along minor shear zones in columnar basalt. (see Manspeizer, and Olsen this fieldbook).

Second Watchung
Note Riker Hill to the west as 280W descends to the area of Glacial Lake Passaic . Along the cut in the Second Watchung, while it is still at a high angle, several failures can be observed along minor shear zones in columnar basalt. (see Manspeizer, and Olsen this fieldbook).

Glacial Lake Passaic

New Jersey Highlands to the west
Traversing glacial deposits overlying Brunswick Formation.

STOP 2. Abandoned Quarry
This is a semi-abandoned quarry. The main purpose is to observe the materials in the terminal moraine at this point. At this location, the embankment is primarily sand.

STOP 3. Morristown Memorial Hospital - On Ramapo Fault
Ramapo Fault - Highlands immediately west of road
Is it or isn't it an active fault? If it is active, how active?
Lamont-Doherty Geologic Observatory has indicated it is a capable* fault. The technical and judicial examiners on the recent (1977) Indian Point Nuclear Power Plant Appeal Board hearings declared it was not. The Nuclear Regulatory Commission and Consolidated Edison Co. consultants agree with the hearing board.
Controversy still rages with the planning of two water supply dams across the fault in southern Rockland County. Intervenor witnesses have quoted an April 1978 Science article (see References) concerning the Indian Point plants as their rationale for requesting a seismic factor even greater than that used in design of the nuclear plants across the Hudson River.
Yet here in New Jersey, there are hospitals and schools built across the fault in two towns we will pass through on this field trip -- Morristown and Bernardsville. No controversy seems to exist in this area of the state concerning the activity of the Ramapo, despite experiencing a Mag. 3.1 earthquake in Bernardsville as recently as March 10, 1979,
At this stop we'll quickly look at the "fault" as it passes below a hospital. Is it disaster waiting to happen or is it a tempest-in-a-teapot? Look at the trace here in Morristown. The trip will pass over the Ramapo and related structures several times. The seismicity of the Ramapo will be discussed at Stop 4 (in greater comfort).
* 10CFR 100 Appendix A, Seismic and Geologic Siting Criteria for Nuclear Power Plants.

Route 202 generally lies along Ramapo Fault.
Notice new construction, homes, apartments, office buildings. Some are on septic systems; some are on Morristown sewage treatment plant system.

Descend to Glacial Lake Passaic terrain
Outlier of Third Watchung basalt flow to the north and Long Hill (third flow) to south.

STOP 4. Great Swamp Refuge (lunch)
The Great Swamp Refuge was established in 1960. It is only 26 miles west of New YorK City in the Boston-Washington metropolitan corridor. It is approximately 6,000 acres of swamp woodland, hardwood ridges, grass lands, old croplands, and water impoundments. As previously noted, it is within a portion of the area covered by ancient Lake Passaic.
Approximately two thirds of the refuge is designated as Wilderness Area and the remainder as Management Area. Man-made structures and motorized vehicles and equipment are prohibited by law from this area. In the Management Area, the habitat is controlled by cutting brush and timber, mowing, farming, planting shrubs, regulating water levels, and by providing nesting structures.
The problems of maintaining a wildlife refuge in an area where population and commerce are steadily growing will be discussed by members of the Refuge staff.

Rise from Glacial Lake to Long Hill basalts

STOP 5. Millington Gorge (gorge in basalt)
This steep-sided cut through Long Hill (the Third Watchung) is aligned with Osborne Pond in Basking Ridge and Mt. Kemble Lake in Harding Township as well as a valley through a ring of basalt in the New Vernon area. Is this an en-echelon fault of the main branch of the Ramapo or just differential erosion and coincidence?
Whatever the reason, during heavy storms the Gorge acts as a constraint to flow in the Passaic ponding water as far upstream as the Great Swamp and contributing to many flooded basements to the north (see Figure 1) along Black Brook and the Passaic River.

STOP 6. Millington Quarry (quarry in basalt)
At the time of preparing this outline, it was not known whether we would be allowed within the Quarry or would have to walk from Millington Gorge to view the scope of the operation. The concern here is not the mere idea of quarrying the Watchung basalts, which are well exposed in the Gorge and many other locations for inspection, but in blasting rock and the resulting transportation in a middle-class, suburban environment. The quarry has continually been in litigation with the town because of the noise, dust and shaking caused by trucking and blasting operations.
Present New Jersey State law requires that a peak particle velocity of two inches per second should not be exceeded in critical areas away from any blasting. Whenever checked, the quarry has not exceeded these limits yet the complaints continue, not unexpected as the human body is an excellent vibration device, The present N.J. criteria were derived from work undertaken in the 1960's by the U.S. Bureau of Mines with subsequent confirmation (?) by others in Sweden, Canada and Great Britain. The presently proposed Bureau of Mines criterion is a particle velocity of one inch per second. What will these criteria do to quarries like this and others in similar environment? The proposed criteria also establish air blast limitations.
We'll discuss all of the above.

Shallow Brunswick

Shallow Brunswick to basalts, Second Watchung

STOP 7. Scenic View Parking Area on Second Watchung
Can view road cut best from east end of Parking Area. View to the west is across Newark Basin to New Jersey Highlands
Two possibilities exist for the problems as encountered at this highway cut. One is that a fault zone cut through the basalt in this area; the other is that merely the broken columnar nature of the rock here made steep rock cuts impossible. The embankments at this location were cut originally at the same slopes as the remainder of the highway. Repairs kept the highway closed for over a year while the pavement was otherwise completed. After a long period of cogitation, the slopes were cut back to what you see at present. Rock falls were minimized and the ten miles of highway opened. The additional costs of time and excavating are not known but must have been considerable. Could a good site investigation have prevented this problem? -- a discussion.

Descend from Second Watchung

Probably Brunswick mudstone
Probably Brunswick mudstone with perhaps some more conglomeratic facies toward Highlands to the west

STOP 8. N.J. Highlands to West, Ramapo Fault bends to west.
At Far Hills, we can compare the mapped location of the Ramapo (See Figure 1) with the local topography and discuss the effect of the fault upon local construction, both socially and from a general ground water viewpoint.

Leonard J. Buck Gardens
The proposed (Spring 1980) Somerset County Arboretum is at Moggy Hollow. A bit of New Jersey geologic history will be retained.

STOP 9. Johns Manville Properties site
Development of New Town-Bernards Township/Bedminster
A new development comprised of housing and office buildings is planned for a 1,500 acre site. The site was in litigation for several years and the decisions in the two townships were totally different (and will be discussed). Some 400 acres (higher density - Bedminster) will be sewered while 1,100 acres (low density - Bernards Township) will be on individual or small combined septic systems.
The site has shallow basalts and shales, residual soils, lacustrine deposits, glacial till, high water table, protected streams, steep slopes and is adjacent to the Ramapo Fault. How do you develop this property (the largest single site planned for development in New Jersey)? We'll have a local geology map, test this pit data, percolation test data and some development concepts for discussion -- a seminar.

STOP 10 Route 78 - Berkeley Heights
The highway has been completed to this location for some 5 to 10 years. The road has opened in 1978 from Millburn to Newark Airport (see Figure 1) but there has been extensive discussion concerning the most environmentally sound route (or non-route). We'll discuss it a little more, from primarily a geologic viewpoint.

13: THE PASSAIC RIVER FLOOD PLAIN AND BASIN IN NEW JERSEY
JOSEPH WEISBERG & JOHN MARCHISIN
Department of Geoscience/Geography
Jersey City State College
The field experience follows parts of the Passaic River and its tributaries beginning at the Newark Campus of Rutgers University. The trip parallels the course of the River. It then continues along U.S. Route 46 West to Wayne, Oakland, Lincoln Park and Fairfield in Passaic and Essex Counties near the confluence of the major tributaries; the Pequannock, Ramapo and Pompton Rivers and returns to Newark.
The Passaic River Basin
Created during the Wisconsin age, the present drainage basin of the Passaic River trends in a generally east-to-southeast direction in the Passaic-Essex County Region. The River, rising in Mendham Township, N.J. in Morris County, receives major tributaries as the Saddle River, Mahwah River, Third River, Rockaway River, Whippany River, Pequannock River, Pompton River, Ramapo River, and Wanaque River. All these tributaries drain a natural retention basin formed in the swamp made up of the Black Brook, Troy, Little Piece and Great Piece Meadows. These are part of the remnants of ancient Lake Passaic formed as an empoundment when the Wisconsin glacial advance closed a water gap at Short Hills and subsequently opened another in the Little Falls-Great Notch area.

13: THE PASSAIC RIVER FLOOD PLAIN AND BASIN IN NEW JERSEY

Note debris build-up and desnagging needed.

Dundee Dam
Dundee Dam is the area of demarcation between fresh water above and estuary below Garfield.

STOP 1. Great Notch
The roadway is located in an area that was formerly one of two spillways. The lithology is a basaltic flow of the First Watchung Mountain. This is the second water gap opened at the close of the Wisconsin glaciation.

Junction of Singac Brook and the Pompton River

STOP 2. Weir and flood marker
Weir and flood marker are located at the junction of the Pequannock and Pompton Rivers. Note the bar deposits due to the curtailment of the stream energy by the bridge and pipeline. In this area the watershed traverses a setting of homes and ball fields. Return to bridge, proceed right on Pompton Plains Cross Road.

STOP 3 Intersection of Cross Road and Framingdale Ave
Old Feeder Dam above junction of the Pequannock and Pompton Rivers. Note changeable sign that keeps drowning record. This is a region of severe flooding after heavy rainfall despite the canal that can be followed from this region to Stop Two.

First Watchung flow on right
The ridge on the right is part of the First Watchung flow. Drainage on this side runs toward Pompton Lake, opposite is Wayne Township.

Pompton Lake
Long term siltation and eutrophication has affected the retention ability of the lake. Dredging is to begin in mid-1980. Evidence of an abortive landfill can be seen in part of the lake shore along Rt. 202N.

STOP 4. Upper end of Terhune Park
This location is at the upper end of Terhune Park on Pompton Lake which receives the Ramapo River. It is named for Albert Payson Terhune, a dog breeder and author. It is also the site of boxer Joe Louis's training camp during the 1940's. Residential development lies on both sides of the river; note the undercutting of the retention wall. The area is connected by a small bridge to elevated Rt. 202N where residents park cars prior to flood events. Similar bridges can be found east of this location. A major problem is that the flood plain is swamp woodland resulting in debris jams at many sites.

STOP 5. Newark's Wanaque Reservoir pump station
Newark's Wanaque Reservoir pumping station has a persistant desnagging problem. The Ramapo Fault lies under the talus sloop (north) seen across the lake dam at the pumping station site.

Turn right over the Bridge at Dawes Highway.
The Pompton River forms a meander near its junction with the Pequannock River. Two to four feet of water inundate four blocks of homes during severe flooding.

STOP 6. Sewage Treatment Plant?
2011: There is no description for STOP 6 in the Guidebook. The directions, to go left on Riveredge Drive, take you near here. -- OHM

Sand and gravel pits
Note the sand and gravel pits associated with the Wisconsin glacial moraine. Rt. 23 dips in several locations leading to major flooding following heavy rain, especially near the sites of the Racquetball Spa and MacDonald's Beach and Lake adjacent to the road.

Drainage Ditch
Note the drainage ditch that now enhances flooding near the elevated cottages.

STOP 7. Bridge at Riverside Drive.
The bridge and pipeline are part of the water supply for the city of Newark. The siltation and build up of, debris occur in several locations in a limited area.

STOP 8 Dorsa Ave.
Dorsa Ave. is the designated flood parking area, for area residents. Pia Costa Co. property is a natural retention basin extending into Fairfield, now being developed near Rt. 46E at opposite side of the basin. The railroad trestle shows much evidence of heavy siltation.

STOP 9. Park at Soccer Field.
Note Pompton River undercutting banks and homes with retaining walls opposite the fields. This is Lincoln Park, the site of repeated flood problems during heavy rainfall. The soccer fields have been flooded to a depth of 3-4 feet during flood stage of the river. Make a U-turn in parking lot and return to the Newark-Pompton Turnpike. This road follows part of the flood evacuation route to emergency parking.

Pompton River
Fairfield Rd. follows the course of the Pompton River. Elevated homes are built on the island and opposite bank. Raised bridges create access to the sites of housing.

STOP 10. Two Bridges
This is the junction of the Passaic and Pompton Rivers, a site of frequent flooding after heavy rain. Color differences noting the river junction is often obvious at the bridge junction.

Riverside Drive.
Proceed to Riverside Drive. Homes built on the flood way of the Passaic River between it and a former retention site. Minor flooding occurred with frequency prior to the development of the retention site.

STOP 11. Willowbrook Mall.
A mall developed on the former retention area elevated the region. The homes near Riverside Drive now receive drainage from this parking lot and flood water from the river. Flooding is more frequent and severe. The roadway is township property and not mall property and is designated a flood parking area.

14: LATE TRIASSIC PART OF NEWARK
SUPERGROUP, DELAWARE RIVER SECTION
F.B. VAN HOUTEN
Department of Geological and Geophysical Sciences
Princeton University, Princeton, New Jersey
The Late Triassic part of the Newark Supergroup exposed along the Delaware Valley (Van Houten, 1969) consists of as much as 6 km of nonmarine sedimentary rocks and an associated sill. Its strike generally parallels the northeasterly trend of the basin with a dip of 10-20°NW. Along the northwestern margin the sequence is bounded by Precambrian and Paleozoic rocks of the Reading Prong of the New England Upland. Most of this boundary is a system of high-angle faults (see Ratcliffe, this guidebook), but intermittently Newark border conglomerate overlaps on rocks of the upland terrane. Within the basin and along its southeastern margin Newark strata lie on Paleozoic and Precambrian rocks of the Blue Ridge and Piedmont provinces.
In the northeast (Fig. 3) the Newark Supergroup consists of a lower, locally conglomeratic Stockton Arkose (1840 m, 6000 ft), grading upward into reddish-brown Brunswick Mudstone (more than 1900 m and perhaps as much as 4000 m thick). Along the northwestern faulted border these deposits interfinger with the Hammer Creek Conglomerate. In the central part of the basin the widely-occurring Stockton and Brunswick formations are separated by and interfinger with the dark gray to reddish-brown Lockatong Formation (as much as 1145 m, 3750 ft thick). These major sedimentary rock types comprise rather uniform, widespread units. In the Delaware Valley area a diabase (dolerite) sill is intruded into Lockatong and lower Brunswick strata.
Across the central part of the basin, as seen along the Delaware River, the Newark formations are repeated in three large northwest-tilted blocks. The Flemington and Hopewell faults that bound them may be part of a transcurrent system involving those along the northwestern border as well. Geophysical and subsurface evidence of intrabasin faults near the present margin of the basin (Summer, 1977; Cloos and Pettijohn, 1973) indicates that it was not a simple half-graben.
The Newark Supergroup ranges in age from Karnian (Late Triassic, 215 my) to late Liassic (about 180 my), with Liassic sedimentation beginning about 100 m below the 1st Watchung basaltic lava flow in the middle of the Brunswick Formation (Cornet and Traverse, 1975; Olsen and others, 1980; Olsen, this guidebook). Along the terrane of extension in eastern North America basin development and igneous activity apparently peaked about 190 my ago. In the Delaware River section the Triassic-Liassic boundary presumably is above the preserved Brunswick strata.
FIELD TRIP
Route and Objective
This one-day field trip (Fig. 3) crosses the Newark Basin and Watchung lava flows northwestward from Newark to the border fault, then turns southwestward to the Delaware River section of the Newark Supergroup in the northernmost of three major fault blocks in the central part of the basin. Stops along the 33 km (20 mi.) traverse southward down the section afford study of 1) the Hammer Creek Conglomerate near the northern border fault, composed of Paleozoic carbonate and quartzite clasts in fining-upward sequences marked by calcrete paleosols; 2) the lower part of the Brunswick Mudstone arranged in repeated alternations of reddish~ brown silty mudstone and claystone mudflat deposits; 3) the cyclic lacustrine facies of the analcime-dolomite-rich Lockatong Argillite and its hornfels; 4) the small Byram diabase sill; and 5) the Stockton Arkose with a predominance of Na-feldspar, confirming derivation of most of the Newark basin fill from an eastern or southeastern source. This thick (6 km) sequence is the record of interior basin sedimentation in a major rift valley developed during the early stage of post-Appalachian-Variscan opening of the central Atlantic Basin. The return trip to Newark crosses the Brunswick mudflat lowland in the middle fault block (Fig. 3, 4), then continues northeastward along the south flank of the Watchung lava flows.
The focus of the field trip is on the principal sedimentary facies and the successive changes in sedimentation displayed in the Newark Basin. In this review particular significance is attributed 1) to the eastern upland as the source of the distinctive soda-rich basin fill, 2) to relatively intense weathering in the upland terrane required to produce the large supply of clay in the Lockatong and Brunswick formations, in contrast to the evidence of aridity in the basin reflected in many of the sedimentary features, 3) to a long interval of stability during development of the graben documented by the Lockatong lacustrine deposits, and 4) to several patterns of allocyclic sedimentation recorded in the Lockatong and Brunswick deposits.

14: LATE TRIASSIC PART OF NEWARK
SUPERGROUP, DELAWARE RIVER SECTION

Many zones of reversed magnetic polarity
Interbedded Brunswick (Passaic) reddish-brown arkosic sandstone and mudstone with thin layers of dark gray micaceous mudstone. Local exposures of fining-upward fluvial sequences. See Olsen, this guidebook for revised stratigraphic nomenclature.
Samples across this traverse to the border fault reveal that the 1250m section of Late Triassic Brunswick beds below the 1st Watchung lava flow contains many zones of reversed magnetic polarity. All of the Liassic strata (1750m) above the 1st flow are normally magnetized (McIntosh and Hargraves, 1980, ms; Cornet and Traverse, 1975).

1st Watchung lava flow (Orange Mountain Basalt)
1st Watchung lava flow (Orange Mountain Basalt) 50-65m thick. Basal contact covered. Very thin hornfels facies with small patches of copper minerals. Lower part displays well-developed colonnade with vertical columnar joints. Main body of flow is curvi-columnar zone with closely-spaced radiating joints. (See Manspeizer, this guidebook). Roadcut is 38m deep, said to be the deepest east of the Mississippi River.

Brunswick (Feltville) Fm
Crossing Pleasant Valley Way in mudflat and lacustrine facies of Brunswick (Feltville) Formation between 1st and 2nd Watchung Mts.

2nd Watchung flow (Preakness Mountain Basalt).

Towaco Formation
Crossing lowland in reddish-brown fluvial and dark gray lacustrine Towaco Formation (37m). Rikers Hill (Roseland) National Monument (dinosaur tracks) to SW. Locally some of these lacustrine deposits contain traces of hydrocarbons.

3rd Watchung lava flow (Hook Mountain Basalt)
Crossing 3rd Watchung lava flow (Hook Mountain Basalt). Each Watchung flow was extruded somewhat later than renewed faulting and differential uplift of the flanking highlands that produced fanglomerates (Faust, 1978).

Passaic River
Passaic River, drains Hatfield Swamp on broad expanse of uppermost Brunswick (Boonton) Formation to W.

3rd Watchung flow
North horn of New Vernon anticline in 3rd Watchung flow to S.

Patch of Hammer Creek Conglomerate in low hill to SE.

Ramapo border fault
Narrow gap between Ramapo border fault and west end of New Vernon anticline in 3rd Watchung flow. The fault continues for about 50 miles to the NE end of the basin (see Ratcliffe, this guidebook).

Crossing Passaic River.
In its last stage Glacial Lake Passaic drained northeastward through gaps in the Watchung flows at Little Falls and Paterson. Great Swamp National Wildlife Refuge to S is a swampy remnant in broad syncline above the 3rd Watchung flow.

Narrow gap between 2nd and 3rd Watchung ridges.

Moggy Hollow
Moggy Hollow (Mine Brook Road) between recurved 2nd Watchung Mt. to NW and 3rd Watchung (Long Hill) Mt. to ESE. Early drainage of Glacial Lake Passaic flowed westward through this notch to the North Branch of the Raritan River. West scarp of 2nd Watchung faulted against Brunswick Formation (Adams, 1980).

Watchung Mts. on skyline to E.

Syncline in New Germantown flow in low hills a mile N.

NE end of Flemington Fault
Crossing NE end of Flemington Fault at junction with the border fault (near Lebanon). To S Cushetunk Mt. (diabase) encloses Round Valley Reservoir.

Cambro-Ordovician strata and Precambrian gneiss
Complexly faulted Cambro-Ordovician strata and Precambrian gneiss that project S into the Newark Basin are limited on E by the Flemington Fault.

Remnant of a Taconic klippe
Reddish-brown and gray Early and Middle Ordovician shale with thin beds of chert and limestone. Apparently a remnant of a Taconic klippe (Perrisoratis, 1974).

Ordovician shale overlapped by Hammer Creek Conglomerate.

On northern edge of Hammer Creek Conglomerate
On northern edge of Hammer Creek Conglomerate covering Cambro-Ordovician strata faulted against Precambrian gneiss.

Cross Rt. 579 on border fault.
Large fan of quartzite-rich conglomerate interfingers with Brunswick, Lockatong, and Stockton formations to E and SE. Evidence that movement on border fault occurred throughout episode of basin-filling.

Brunswick Formation
Brunswick Formation S of narrow belt of limestone-pebble conglomerate.

Brunswick Mudstone between fanglomerates.

Continue W on Church Road along border fault.

Quarry in Hammer Creek Conglomerate
Quarry in Hammer Creek (Silurian quartzite clasts) Conglomerate to S. Clasts shattered by crushing in fault zone. Detailed map of Musconetcong Mt. to N and Newark Supergroup S to Frenchtown by Drake and others, 1961, 1967.
2011: Workings apparent in GE photos before 1997. --OHM

Cambrian limestone and border conglomerate
Traverse crosses narrow belt of Cambrian limestone and border conglomerate, and the Brunswick Mudstone between lobes of Hammer Creek Conglomerate. Good exposures of border fault relations across the Delaware River at Monroe (0.5 mi S of Durham Furnace on PA 611).

Cliff on far side of river
Cliff on far side of river above power station shows patterned sequence of middle Brunswick deposits seen at Stop 2. Plateau capped by Coffman Hill diabase sheet (165 m) above gray Brunswick hornfels. The sill is estimated to be about 1400m below the 1st Watchung lava flow.

STOP 1. Hammer Creek Conglomerate
STOP 1 Hammer Creek Conglomerate, Pebble Bluffs at culvert.

Stop 1B. Conglomerate in steep roadcut
Southward projecting lobe of quartzite-rich fanglomerate dipping 10-15 NW. Most clasts are less than 8 cm in diameter, a few are 13 cm long, the largest are 25 cm long. Some clasts are imbricated. Bedding is very poorly developed; cross-bedding is virtually absent.
The poorly sorted detritus is arranged in crudely fining-upward sequences about 7-9 m thick (Fig. 5) with a scoured base, multi-storied units of conglomerate, and calcareous patches and nodules (calcrete paleosol) in the upper sandier part.
Significant items:
1. Outcrop less than 5 mi from border fault.
2. Source probably less than 25-30 mi to N.
3. Clasts and matrix derived from Paleozoic rocks now stripped from the uplands.
4. Fining-upward sequence and calcrete common in alluvial fans.
5. Lensing and channeling well-displayed at south end of bluffs.
6. Rapid gradation southward into distal, finer-grained facies.
7. Fault in ravine between two major outcrops.

STOP 2. Middle Brunswick Mudstone
Long roadcut in essentially horizontal middle Brunswick Mudstone south of Spring Valley Road. Bright reddish-brown mudstone in patterned sequences about 950 m above base of formation (Picard and High. 1963).
Items along 0.2 mi traverse:
1. Normal fault at E end of exposure down to E. Conspicuous jointing.
2. Succession of about 30 massive mudstone and hackly claystone alternations averaging 1.5-3 m thick (Picard and High, 1963). Few units with persistent 1-2 cm beds of siltstone.
3. Abundant burrowing has destroyed lamination in mudstone. Absence of bedding in claystone may be result of small-scale physical disruption.
4. Distinct 2-6 cm layers filling abandoned channel (Fig. 6). Fine-to-medium grained feldspathic sandstone in lower part of each layer derived from southeastern Na-feldspar-rich source area. Some layers are graded. Tops are marked by burrows and shrinkage cracks. Abandoned channel may have been part of inter fluvial drainage of extensive alluvial plain (Allen and Williams, 1979) or a shallow waterway in a clay-flat playa.
5. Hammer Creek tongue of dark reddish-brown Paleozoic quartzite-clast lithic-rich sandstone 3 m above 11.1 road E and W of ravine and culvert.

Perkasie and Land M members of Brunswick
Fm
Dark gray Perkasie and Land M members of Brunswick
Formation 930 m above Lockatong Formation. These are highest of 8 recurring gray units in the Delaware Valley region, centered at 120-137 m intervals (Fig. 1). Several have been traced to NE into Hammer Creek Conglomerate (Fig. 4), as well as 25 km to SW where they interfinger with reddish-brown mudstone. Gray units consist of black, pyritic platy muddy limestone and calcareous mudstone. The Perkasie Member apparently is about 1400 m below the 1st Watchung flow. Intervals of reversed magnetic polarization have been identified below both the Perkasie and L and M units, as well as just below and above the Graters Member lower in the formation (W.C. McIntosh and R.B. Hargraves, 1980, Ms).

STOP 3. Middle Brunswick Mudstone
Middle Brunswick Mudstone, roadside excavation. Well-displayed bedding surface markings, including several sizes of shrinkage crack-patterns, burrows, and small tracks and trails, many probably made by small crustaceans (Boyer, 1979).

Gray units E through H
Gray units E and F exposed in ravine and along side road. Gray units G and H above 100 m higher in section constitute the Graters Member (40 m thick).

Gray unit D exposed in ravine of Warford Creek.

STOP 4. Lowermost Brunswick Fm, Tumble Falls.
Ravine and high roadcut in lowest reddish-brown unit and lowest gray unit C (40 m thick) about 75 m above base of formation (Fig. 1, 7). Reddish-brown mudstone units exhibit three distinctive disruption features:
1. Thin greenish-gray beds with scattered shrinkage wafers.
2. Layers of light brown-weathering dolomitic mudstone 1-3 cm thick, in both pull-apart structures and widely dispersed fragments.
3. Upward-concave surfaces of shearing in tent-like structures 15 to 30 cm high suggestive of gilgai formed in soils by repeated wetting and drying.
The uppermost platy part of gray unit C consists of:
1. Black pyritic mudstone layers 2-3 cm thick with wide, completely crumpled composite and injected shrinkage crack casts of brown-weathering muddy dolomite and minor calcite.
2. Lenses of pyritic peloidal dolomite 10-20 cm thick, with silty round and flattened burrow casts and thin arcuate calcitic skeletal debris (ostracodes?) in the upper part. Many of the peloids are crudely concretionary dolomite with internal shrinkage cracks filled with sparry calcite. They may be algal oncolites.
The overlying massive reddish-brown mudstone contains tiny flecks of pyrite and irregular tan calcareous nodules 1-5 cm long that may be algal structures. Many of them have irregular patches of sparry calcite or are crudely concretionary.

Double Red unit exposed in creek to E
Double Red unit exposed in creek to E is uppermost reddish-brown sequence of analcime-rich chemical cycles assigned to the Lockatong Formation. Thin reddish-brown intervals of this sort are the most analcime-rich and recur in a 105-120 m pattern of long cycles in phase with thick reddish-brown units in the Brunswick Formation

Triple Red unit in abandoned building-stone quarry
Triple Red unit in abandoned building-stone quarry to E about 1000 m above base of Lockatong Formation. Red units were favored for building blocks because of their more interesting variegated colors.

STOP 5A. First Big Red unit, Lockatong Fm
First Big Red unit about 35 m thick, Lockatong Formation, roadside outcrop, north end of Byram road cut. Short chemical cycles consist Of lower platy dark lavender analcime-rich argillite with intraformational breccia and conspicuous shrinkage cracks with large white patches of analcime and dolomite. Upper massive part is reddish-brown, and spotted with tiny specks of analcime and dolomite locally arranged in rosettes of radiating skeletal crystal casts.
Profile of ledges in long Byram roadcut to S (395-730 m above base of Lockatong Formation) outlines succession of short cycles (Fig, 2B).

STOP 5B. Short detrital cycles of Lockatong Fm.
Short detrital cycles in gray sequence of Lockatong Formation. Easily eroded black shale in lowest part and feldspathic (Na-feldspar predominates) siltstone and fine-grained sandstone in the upper part (Fig. 2A). Essentially a very fine-grained distal facies of Stockton Arkose.

First thin Red unit in Lockatong Formation.
Lowest of the several red units in the Newark section (Fig. 1).

STOP 6A. Short chemical cycles of Lockatong Fm
Short chemical cycles in gray unit of Lockatong Formation between 450-550 ft marks (Fig. 8). Gray analcime-rich chemical cycles 2-4 m thick (Fig. 2) are characterized by:
1. Platy lower part of alternating black mudstone and tan-weathering dolomitic layers disrupted by shrinkage cracks and pull-aparts.
2. More massive middle part with extensively disrupted dolomitic layers.
3. Upper more homogeneous analcime-rich part, commonly speckled with tiny patches of analcime and dolomite distributed in a pattern of minute shrinkage cracks. Locally analcime and dolomite occur in sprays of skeletal crystal casts.

Lockatong cancrinite-rich hornfels
Large abandoned quarry in Lockatong cancrinite-rich hornfels (chemical cycles; Fig. 8). Cancrinite is present 130 m (425 ft) stratigraphically above the faulted contact with the Byram diabase to the S. Two well-defined detrital cycles at top of quarry wall.

STOP 6B. Lockatong hornfels and Byram diabase sill
Lockatong hornfels and Byram diabase sill, to south end of roadcut (Fig. 8).
1. White sprays of cancrinite, albite, and calcite at 21 ft mark developed from analcime-dolomite crystals in a chemical cycle, as seen in First Big Red units (Stop 5a).
2. Nepheline developed in hornfels 25 m (11 ft mark) above Byram Sill. .
3. Metal disk 2 m above road at 10ft mark records flood level in Sept. 1955.
4. Faulted upper contact with diabase sill (Fig. 8) and essentially undisturbed contact with xenolith. Lockatong chemical cycles metamorphosed to nepheline cancrinite, calcite, pyroxene and amphibole, biotite-albite hornfels (an aphanitic syenite!).
5. Extensively fractured coarse-grained diabase with abundant joint minerals including calcite, epidote, prehnite, tourmaline, and amphibole. Conspicuous horizontal lineations marked by concentrations of joint minerals are not related to compositional layering in the sill.
6. Vague cyclic pattern of ledges of albite-biotite hornfels S of sill. Nepheline occurs about 30 m (100 ft) below the sill.

Southernmost roadside outcrop of Lockatong hornfels
Southernmost roadside outcrop of Lockatong hornfels, about 80 m below Byram sill.

Crossing estimated Lockatong-Stockton contact.

Uppermost Stockton Formation
Well-bedded reddish-brown sandy mudstone and sandstone in uppermost Stockton Formation.

Raven Rock.
Upper arkosic member 100 m thick (Fig. 1).

Lockatong Creek.
Quarry in Cutalossa Member of Stockton Formation (Fig. 1) high on west bank of river.

STOP 7. Middle Stockton Arkose
Quarry 1 mile N of Stockton. Upper Prallsville Member (Fig. 1) 61 m thick, 760 m above base.
1. Yellowish-gray, well-sorted, medium-grained arkose with only minor reddish-brown micaceous mudstone.
2. Horizontal bedding predominates; with local micro-placers of specular hematite (after magnetite) on bedding planes.
3. Large-and small-scale cross-bedding rare.
4. Intraformational mud-chip conglomerate common.
5. Isolated burrows in arkose and on bedding planes. Micaceous mudstone extensively burrowed.
6. Small yellowish-brown patches common in arkose are limonite after altered iron-rich carbonate cement.
7. Na.feldspar almost twice as abundant as K-feldspar.
8. Very coarse-grained, kaolinized arkose along upper rim of Quarry with clasts of quartz, feldspar, quartzite, and gneiss.

Conglomeratic Solebury Member
Conglomeratic Solebury Member (115 m thick) of Stockton Formation in schoolyard to E.

Arkosic conglomerate of Solebury Member
Roadcut in arkosic conglomerate of Solebury Member. Clasts as large as 8 cm mostly quartzite, rare feldspar and gneiss.

Crossing Flemington Fault at Brookville
Crossing Flemington Fault at Brookville (Fig. 4). To W in Pennsylvania uplifted Cambro-Ordovician limestone is overlain by conglomeratic limestone-clast facies of Stockton Formation.

Lockatong nepheline-cancrinite hornfels
Lockatong nepheline-cancrinite hornfels above Mt. Gilboa diabase. Nepheline and analcime syenites at top of sill probably formed by reaction of a xenolith of Lockatong chemical cycles with a granophyric differentiate of the coarse-grained diabase (Barker and Long, 1969).

Mt. Gilboa trap-rock quarry
Mt. Gilboa trap-rock quarry in unusually coarse-grained diabase (gabbro). Lockatong hornfels along south edge of quarry.

Dilts Corner Fault
Crossing southern branch of Flemington Fault (Dilts Corner Fault).

Brunswick Formation
Join US 202 to NE across Brunswick Formation north of Lambertville sill.

15A: BRITTLE FAULTS (RAMAPO FAULT) AND
PHYLLONITIC DUCTILE SHEAR ZONES (Saturday)
NICHOLAS M. RATCLIFFE
U.S. Geological Survey
Reston, Virginia 22190
Introduction and rationale for investigations
Field investigations at the northern end of the Newark basin begun more than 10 years ago led to the publication of several articles (Ratcliffe, 1971; Ratcliffe and others, 1972) in which a case was made for long continued fault activity in the vicinity of the border (Ramapo fault) in New York and New Jersey.
These articles also called attention to the observation that a series of low-level earthquakes appears to be spatially associated with these ancient faults (Fig. 1).
Since that time, seismic-detention capabilities of the Lamont-Doherty network have been greatly improved and further supplemented by a dense array of stations located on the northern extension of the Ramapo fault in the vicinity of Consolidated Edison's nuclear generating plants at Indian Point (Fig. 2).
Aggarwal and Sykes (1978) document a pattern of seismicity (Figs. 1 and 2) that illustrates that numerous low-level events (Nuttli magnitude 1.5 to approximately 3) are occurring throughout a 30 km-wide zone roughly centered on the trace of the Ramapo fault at depths of 0 to about 10 km. Fault-plane solutions (Fig. 2) obtained by them and by Yang and Aggarwal suggest that motion is currently taking place on northeast-striking
southeast-dipping surfaces. First-motion studies indicate southeast-to-northwest compression and therefore a reverse-faulting mechanism. They conclude that current seismicity in the Ramapo zone is being controlled by reactivation of the northeast-striking steeply southeast-dipping faults which make up the predominant structural grain in this area. They further suggest that the Mesozoic border fault, the Ramapo fault, and its northern splays (Fig.1) are the actual surfaces being reactivated.
The geologic framework of the Ramapo seismic zone, however, is extremely complex. A multitude of faults of differnt ages have different physical characteristics and contrasting histories. The northeast-trending structural grain of this zone is accompanied by faults of Proterozoic, Paleozoic, Mesozoic and possibly Tertiary and recent age.
Despite the abundant evidence for reactivation of older faults in the Mesozoic, (Ratcliffe, 1971) the Mesozoic and younger faults are not uniformly distributed and do not everywhere coincide with the traces of older faults. Unfortunately, it is not presently possible to produce a tectonic map of this area that accurately shows the distribution of Mesozoic as opposed to older faults. In general, previous studies have not attempted to differentiate Mesozoic faults except where Mesozoic rocks are actually offset. The geologic-tectonic template, therefore, is quite incomplete at present, and any plan to test the hypothesis that geologic structures of Mesozoic age are responsible for current seismicity is severly limited by the lack of appropriate geologic data. Figure 1 shows a new preliminary compilation of fault features

15: BRITTLE FAULTS (RAMAPO FAULT) AND
PHYLLONITIC DUCTILE SHEAR ZONES

Excellent crops of "First Watchung" basalt
Excellent crops of "First Watchung" basalt (Orange Mountain basalt in Olsen this guidebook) Minor faults strike N. 20° E. and dip 80° SE. and have broad shear zones with gouge and subhorizontal slickensides.

Crops of platy jointed basalts of Second Mountain
Crops of platy jointed basalts of Second Mountain (Preakness Mountain basalt of Olsen, this guidebook)

View in distance of Hudson Highlands and Ramapo fault escarpment.

Conglomerate at Montville of Carlston
Excellent crops of the conglomerate at Montville of Carlston (1946) here contain cobbles of hornblende granite, gneiss, epidote veined cataclastic gneiss, "Franklin Marble", and abundant clasts of basalt. These deposits are the youngest rocks in the Newark basin.

Turn left on Old Lane and crops of gneiss boulder conglomerate.

STOP 1. Mulbrook Lane.
Stop at end of circle -Sliver of Cambrian quarzite phyllonite and Ramapo fault breccia
At east side of circle is brown, very shattered, dioritic gneiss(?). To west up slopes by house are crops of vitreous quartzite of probable Cambrian age. Farther west, across small swale, are excellent crops of pale-green, phyllonite gneiss typical of the more ductile deformation zones in the Hudson Highlands.
Sericite, epidote, and needles of actinolite are found in the phyllonite which exhibits strong right-lateral strain slip folds. Ductile deformation is characteristic of these zones along the western edge of the Mesozoic basin.
This quartzite forms one of a series of similar slivers of Cambrian and Ordovician cover rocks that are found west of the Ramapo fault from Boonton north to Tomkins Cove and are interpreted as fault slivers within the ductile shear zones of pre-Mesozoic age. The phyllonite zone forms a continuous belt along the Ramapo to Riverdale where the shear zone may bifurcate with part of the zone extending northward into the Proterozoic rocks along the Lake Inez shear zone.
The cataclastic rocks east of the circle are more typical of cataclastic rocks associated with Mesozoic faulting on the Ramapo.

Low crops of what may be the 4th Watchung lava flow
Turn right on Indian Lane -low crops of what may be the 4th Watchung lava flow; excellent crops in gas pipeline.

STOP 1b. Optional stop. Roadcuts at entrance to golf course at Jacksonville.
Grey to greenish-grey coarse conglomerate (Jc) that contains fragments of "Franklin Marble," detrital graphite, coarse cobbles fragments of hornblende granite gneiss and epidote-veined phyllonite from the older phyllonite west of the Ramapo fault. To the south, a lava flow younger than the "Third Watchung" lava flow overlies fanglomerate. A waterwell drilled in 1979 penetrated 50 feet of basalt and bottomed at 130 feet in grey and red shale conglomerate near this site.
These sedimentary rocks and the lava flows are the youngest rocks known in the Newark basin, based on the palynology of Cornet (1977) who identified these rocks as Sinemurian (middle Early Jurassic).
The nonfolded outcrop pattern of these Sinemurian deposits as compared with the marked northwest-trending folds affecting the Watchung lava flows is notable. This suggests to me that the northwest crossfolds may have formed prior to cessation of fanglomerate deposition.

Stop 2. Large sandpit southwest of traffic circle
2011: Traffic Circle is gone, sand pit is gone, now we have Interstate 287, which in 1980 terminated somewhat south of here. As much of the discussion is about drill cores, it is all copied here. OHM
Just after traffic circle pull over to right. Stop 2 -cross over highway with caution to large sandpit. Bus will turn around and meet us on east bound side of Route 23.
Stop 2. Large sandpit southwest of traffic circle at Riverdale. (See Fig. 5,6,7).
Discussion of core drilling at Riverdale site and bedrock exposures of phyllonitic shear zones and epidote veined cross faults.
Excellent pavement exposures of phyllonitic hornblende granite gneiss and quartzite paragneiss can be seen. Isoclinal folds with axial planes of N. 35° E., 72° E. are crossed by cross faults locally marked by epidote veins cross-faults N. 65° E., 72° SE., N. 30° W., 90°, N. 25° W., 85° NE. show predominant left-lateral and reverse movement.
At the south end of pit, a mylonitic grey, quartzose gneiss is crossed by small crenulations and down-to-east faults. Along the entire border fault, phyllonite where present near the Ramapo is crenulated and micro-faulted with veins of calcite and laumontite. This is typical of Mesozoic mineralization. The phyllonite predates the epidote-rich crossfaults that are of unknown age.
In the sand pits to the south, two continuous core drill holes penetrated the Ramapo fault, see figures 6 and 7. The fault offsets fanglomerate of probable Sinemurian Age of the hanging wall against phyllonitic gneiss of the ductile shear zone.
The actual fault is expressed by 1 cm of soft gouge, consisting of pulverized rock material. Below the fault, green phyllonite, like that seen in the exposures here, is crenulated and displaced on normal faults. Excellent recovery of the fault zone material has permitted thin section examination of the actual fault. The sawtooth contact is preserved showing down-to-the-southeast sense of movement with no evidence for reactivation since this last normal movement. Chlorite-coated surfaces, microbreccia and cataclasite, and "mylonitic" cataclasite with a pronounced fluxion structure are common in the cores. The actual fault is remarkably sharp and well defined in each core. The fault dips 50° SE. assuming a N. 40° E. strike as indicated from outcrop data to the south.
Sections of the actual core will be available for inspection. PLEASE DO NOT REMOVE CORE FROM BOXES.

STOP 3. Lake Inez shear zone exposures in abandoned sandpit.
2011: Sand pit is evident on GE images from 1995. OHM
Pavement exposures of phyllonitic. amphibolite gneiss and pink pegmatite show right-lateral displacement of pegmatite on N. 15° E., 30° SE. dipping shear zones. Chlorite, epidote and sericite mark phyllonite zones. Later cross faults N.65° W., 60° SW. show left-lateral displacement of shear zones and are marked by veinlets of epidote. This is the northerly extension of the same shear zone seen at Stop 2.
Up the hillside to the east, exposure of gneiss show reactivation of gneissic layering. Within this area, all suitably oriented surfaces, gneissic layering, mylonite zones and more brittle thrust faults all show evidence of reactivation in the Mesozoic movement sense. Widespread reactivation in this area follows the steep northeast-trending structural grain developed in "Grenville" and Taconic tectonism.

Abundant brittle faults as well as more ductile ones
Turn right on Skyline Drive -excellent crops in Erskine area show abundant brittle faults as well as more ductile ones. Reactivation has been widespread.

Epidote-filled cross fractures
Near crest of hill at gas pipeline epidote-filled cross fractures with excellent wear grooves suggest Mesozoic reactivation.

Exposures of faulted basalt

Stop 4. (Optional stop) "Coal Mine"
Reports from a desultory mining operation in the late 1800's refer to small coal prospect on the west bank of the Ramapo River 1/4 mile north of Crystal Lake.
This exposure is a sliver of coal black graphitic phyllite ("Annsville Phyllite") similar to the exposure along the border fault at Riverdale. Sketch map figure 9 shows the relations. The sliver of black phyllite is found between two outcrops of gneiss. Very mylonitic gneiss is located to the west. Gneiss exposed east of the sliver has a composite fabric with brittle fractures and abundant microbreccia. The relationships seen here are similar to those seen at Stop 1 and those to be seen at Stop 9 on the Thiells fault. The brittle fractures are spatially related to Mesozoic faulting: the more ductile shears are associated with thrust and strike~slip faulting of probable Ordovician age and represent the southwestward extension of the Canopus zone fault exposed north of the Newark basin. Drill holes for water wells about 400 feet north of this site penetrated granite gneiss in holes 500 feet east of this locality. The "Annsville Phyllite" inclusion does not occur within the Mesozoic border fault but lies west of it as part of the footwall block.

Stop 5. Optional Stop. Cataclasite and fault fabric
Cataclasite and fault fabric in cataclastic gneiss at Ramapo fauit, Suffern.
These small exposures of black, chlorite-coated, cataclastic, hornblende-granite gneiss are much more instructive than the exposures north of Suffern commonly visited by field trips. Excellent chlorite-slick surfaces dip in conjugate fashion northwest and southeast and exhibit down-to-the-south right-oblique slip on southeast-dipping surfaces and down-to-the-west and left-oblique movement on southwest-dipping surfaces. The near-vertical attitude of the extension fractures here and in the Sky Meadow drill core suggests that the rocks of the footwall block have not undergone rotation after formation of the cataclastic fabric.

STOP 6. Union Hill trap quarry
Union Hill trap quarry and contact of lava flows with fanglomerate.
We are permitted entrance with the clear understanding that we will not attempt to enter the quarry proper. Please respect the owners' wishes. Use extreme caution near steep cliffs on west side of exposure.
Superb exposures at the south end of the quarry near the rock crushers show a vertical wall of coarse fanglomerate, enclosing a large boulder of brecciated dolostone in an apparent channel that, in turn, is overlain by an upward-fining cycle ending in fine red shale with greenish slate chips. Vesicular pillow lava directly overlies this shale.
Clasts in the fanglomerate include epidote-rich hornblende granite gneiss, Silurian Green Pond conglomerate, dolostone clasts, and several cobbles of basalt pillows. I interpret the large boulder as a block of breccia from the border fault, and the clasts of pillow basalt as blocks eroded from the southward-advancing Ladentown lava flows.
In the Ladentown-Suffern area, alluvial deposits such as those seen here contain boulders of felsic dikes uniquely traceable to the Rosetown dike swarm. These data indicate, as do the observations at the next stop, that a southerly-directed Jurassic drainage system was present near the border fault prior to eruption of the flows at Ladentown and Mount Union. Perhaps the debris flow material seen here are earthquake-activated deposits formed immediately prior to extrusion of the Ladentown basalt. The basalts seen here are correlated with basalts of the "First Watchung" on the opposite limb of the Suffern cross anticline.
2011 Older GE imagery shows the quarry in its prime, particularly before 2004. OHM

Sky Meadow Road -drill site is at base of mountain to left.

Stop 7. Basalt at Ladentown
Basalt at Ladentown and discussion of drill data from the Ramapo fault.
Note exposures and attitude of red quartz-pebble arkose by road and walk north to ridge behind house. Multiple basaltic lava flows with pahoehoe tongues and snouts as well as small pressure ridges may be seen. BE VERY CAREFUL NOT TO DISLODGE BLOCKS THAT WOULD TUMBLE INTO THE BACKYARDS OF THE HOUSES BELOW. Flow direction obtained from similar exposures suggest that the lava flows were flowing southwest toward the border fault and that the base of the lavas flows are at lower elevations to the southwest.
Drill-core data from Sky Meadow Road suggest that vesicular lava and multiple flows of lava more than 450 ft. thick accumulated near the border fault. These speculations would require a local relief in the basin adjacent to the border fault of approximately 450 ft.
Results of the drilling of the border fault will be discussed (see text).
2011: Very good GE image: 4/29/2004 OHM

Fanglomerate found immediately below Ladentown lava flows just past intersection.

Stop 8. Excellent exposures of Mesozoic fault features
(Optional stop). Excellent exposures of Mesozoic fault features on Cheesecoate Mountain north of Newark basin and view of Newark basin.
This block of Proterozoic gneiss lies east of the Ramapo fault but west of the Thiells fault. It may represent a horst of basement rock that was structurally high during Triassic sedimentation. The principal argument in favor of this contention is the dominance of northeast-striking faults that appear to pass into the basin but do not disrupt the continuous belt of intrusive and extrusive lava.

Traversing possible horst block
We are traversing a belt of gneiss that possibly forms a horst block between the Ramapo fault and the Thiells fault.

STOP 9. Thiells fault.
This small but significant exposure (Fig. 12) illustrates well the difference between Mesozoic faults as seen in drill record and the older mylonitic faults of probable Ordovician age. The Thiells fault is an oblique-thrust fault that juxtaposes the Manhattan Prong rocks against those of the Reading Prong. Abundant ultramylonite, pseudotachylite, and mylonite with metamorphic mineralization affects Proterozoic Y and Paleozoic rocks everywhere along the fault. Figure 12 shows the structural relaltionship exposed in the small quarry behind the houses.
K-Ar data on sericite that replaces mylonitic quartzite yields an age of 379± 13 m.y. (386 m.y. using newer constants). K-Ar data on pseudotachylite from a locality to the north gave an age of 259 ±9 m.y. (264 m.y.). The mylonitization and sericitization associated with the fault are totally unlike that found on any proven Mesozoic fault.
Fracturing in the quartzite at the east side of the exposure may be related to Mesozoic faulting. The similarity of this exposure to that seen at Stop 1 is striking.

STOP 10. Triassic quarzite-rich fanglomerate and cataclastic
Annsville at Cedar Pond Brook, Stony Point. (See fig. 14 for location).
Exposures of black cataclastic "Annsville Phyllite" may be seen at the banks of the small pond west of the dam. Thin-section examination of the east-dipping fabric reveals up-from-the-southeast microdisplacements and abundant clinozoisite and sericite replacement veinlets. This fabric is associated with the Thiells fault that crops out to the west.
A light-colored conglomerate of uncertain origin overlies phyllite and contains fragments of brecciated "Wappinger Limestone" and "Annsville Phyllite". This conglomerate may be a basal triassic conglomerate deposited unconformably on the cataclastic "Annsville Phyllite'. Light-grey carbonate-rich conglomerates similar to this are found along the unconformity at Tomkins Cove to the north.
Large crops of coarse fanglomerate are seen at the dam to the northeast. Quartzite clasts dominate. Cambrian Poughquag Quartzite crops out 1,000 ft to the west where it forms an unconformable cover on the gneiss of the Hudson Highlands west of the Thiells fault. This suggests very local source area for the fanglomerate and further suggests that little post-depositional separation has occurred in this area.
Drill data from cores and trenches 800 ft to the north are shown in figures 13 and 11. A normal fault dipping 70° SE. was intercepted in two vertical drill holes. Cataclasite and gouge typical of other Mesozoic faults marked the fault zone. Unexpectedly, gneiss forms the footwall in Cem. 1. A possible interpretation of the data is shown in figure 13. It is notable that none of the distinctive ultramylonitic rocks seen at the Thiells fault (Stop 9) were found at the border fault. This illustrates the difference between Mesozoic brittle fault products and ductile fabrics of Ordovician faults.

STOP 11. Fanglomerate at Stony Point
Fanglomerate at Stony Point at northern end of Newark Basin.
Limestone fanglomerate unconformably overlies Inwood Marble and "Annsville Phyllite" along the east-west Triassic outcrop belt at Tomkins Cove. Exposures in the railroad cut along the slopes contain inclusions of dolostone traceable to the immediately adjacent dolostone in the Tomkins Cove quarry. Small chips of distinctive biotite-rich hornfelsed Manhattan Schist typical of the contact facies bordering the Cortlandt Complex have been found in the fanglomerate at this locality. Very local sediment sources are suggested by these data.

15B: BRITTLE FAULTS (RAMAPO FAULT) AND
PHYLLONITIC DUCTILE SHEAR ZONES (Sunday)
NICHOLAS M. RATCLIFFE
U.S. Geological Survey
Reston, Virginia 22190
Introduction and rationale for investigations
Field investigations at the northern end of the Newark basin begun more than 10 years ago led to the publication of several articles (Ratcliffe, 1971; Ratcliffe and others, 1972) in which a case was made for long continued fault activity in the vicinity of the border (Ramapo fault) in New York and New Jersey.
These articles also called attention to the observation that a series of low-level earthquakes appears to be spatially associated with these ancient faults (Fig. 1).
Since that time, seismic-detention capabilities of the Lamont-Doherty network have been greatly improved and further supplemented by a dense array of stations located on the northern extension of the Ramapo fault in the vicinity of Consolidated Edison's nuclear generating plants at Indian Point (Fig. 2).
Aggarwal and Sykes (1978) document a pattern of seismicity (Figs. 1 and 2) that illustrates that numerous low-level events (Nuttli magnitude 1.5 to approximately 3) are occurring throughout a 30 km-wide zone roughly centered on the trace of the Ramapo fault at depths of 0 to about 10 km. Fault-plane solutions (Fig. 2) obtained by them and by Yang and Aggarwal suggest that motion is currently taking place on northeast-striking
southeast-dipping surfaces. First-motion studies indicate southeast-to-northwest compression and therefore a reverse-faulting mechanism. They conclude that current seismicity in the Ramapo zone is being controlled by reactivation of the northeast-striking steeply southeast-dipping faults which make up the predominant structural grain in this area. They further suggest that the Mesozoic border fault, the Ramapo fault, and its northern splays (Fig.1) are the actual surfaces being reactivated.
The geologic framework of the Ramapo seismic zone, however, is extremely complex. A multitude of faults of differnt ages have different physical characteristics and contrasting histories. The northeast-trending structural grain of this zone is accompanied by faults of Proterozoic, Paleozoic, Mesozoic and possibly Tertiary and recent age.
Despite the abundant evidence for reactivation of older faults in the Mesozoic, (Ratcliffe, 1971) the Mesozoic and younger faults are not uniformly distributed and do not everywhere coincide with the traces of older faults. Unfortunately, it is not presently possible to produce a tectonic map of this area that accurately shows the distribution of Mesozoic as opposed to older faults. In general, previous studies have not attempted to differentiate Mesozoic faults except where Mesozoic rocks are actually offset. The geologic-tectonic template, therefore, is quite incomplete at present, and any plan to test the hypothesis that geologic structures of Mesozoic age are responsible for current seismicity is severly limited by the lack of appropriate geologic data. Figure 1 shows a new preliminary compilation of fault features

Sunday Trip

STOP 12. Tomkins Cove quarry in "Wappinger Limestone"
Tomkins Cove quarry in "Wappinger Limestone" (Inwood Marble) and fault exposures north of the Newark basin.
This large quarry in "Wappinger Limestone" (Fig. 14) forms the axial portion of a westward overturned anticline bordered by "Annsville Phyllite" on the west and Manhattan Schist unit A on the east.
Well-layered beige-to-tan weathering quartzose dolostone with phyllite partings forms the central part of the quarry and is bordered on the west by southeast-dipping overturned but highly folded light gray nonquartzose dolostone and black phyllite.
Planetable mapping of the quarry at 1" = 200 with structural geology students at City College has shown that straight forward correlations of units across the quarry is not possible because of eight major fault zones that disrupt the structural continuity. These faults are expressed by red or green zones of clay gouge and phyllonite. Several of these features can be seen on the south face of the quarry exposed in all three levels.
Structural analyses of the fabric associated with these faults indicate that most are southeast-dipping reverse faults with left-lateral or right-lateral components of movement. Minor folds within shear zones plunge steeply down the dip of fault surfaces, commonly normal to slickensides. Faults are located on the limbs or isoclinal overturned folds exhibiting excellent metamorphic fabric and ductile fold styles.
Despite the young looking nature of these faults they appear to be compressional features formed during Taconic dynamothermal metamorphism. Reactivation may have produced the clay gouge and slickensides locally.
Within the quarry, at the extreme west in corner of level 2 and near the southeastern corner of level 3, N.S. steep north-trending faults offset the older clay gouge zones and produce drag folding of older slickensided surfaces.
The western fault is coated with fibrous palygorskite that forms an excellent slickenside lineation. K-Ar dating of this mineral by H. Kruger yielded an age of 183 ± 31 m. y. These data suggest that the prominent clay gouge seams seen in the quarry are older than 183 ± 31 m.y. The palygorskite-coated fault probably is Mesozoic. The fact that the red claygouge thrust fault zones are not recognized in the Triassic rocks immediately overlying the dolostone to the south also suggests that the main faults seen here are pre-Mesozoic in age.
From these observations, I conclude that the faults seen here are (1) Ordovician thrust faults possibly reactivated in Triassic time to produce gouge, and (2) steep Mesozoic normal and strike-slip faults.
If it were not for the K-Ar age from the palygorskite one might suggest that the clay-gouge zones represent zones of current thrust reactivation in the present compressive stress field related to present-day seismicity. This stop illustrates well some of the complexities in correlation of seismic events with fault surfaces. Any one or all of the faults seen in this area (Stop 9, 10, 12) and shown on figure 14 might satisfy the available fault plane solutions (see fig. 2) available for this area.

At swale, trace of Mott Farm Road fault
At swale, trace of Mott Farm Road fault and cataclastite typical of Mesozoic faults trending N. 70°-80° E. View of Indian Point reactors to east.

Hornblende granite gneiss and abundant semiductile faults
Long up-grade traverses hornblende granite gneiss and abundant semiductile faults with associated lamprophyre dikes on Dunderberg Mountain.

Trace of Timp Pass fault zone
In swale, trace of Timp Pass fault zone of a composite fault zone with evidence of Proterozoic Y, Paleozoic and possible Mesozoic fault activity. This is a major fault that is traceable northeastward through the Hudson Highlands as a metamorphic semiductile fault zone. Very distinctive blastomylonite and a zone of intense folding accompanied by injection of pegmatite mark this fault in many localities. Excellent exposures here of tectonic breccia with inclusions of calcsilicate rocks in a ductile matrix of marble.

Excellent exposures of rusty paragneiss and calc-silicate rock
Note excellent exposures of rusty paragneiss and calc-silicate rock with typical Mesozoic fault fabrics. Exposures of quartz plagioclase gneiss, amphibolite and white alaskite gneiss. Numerous semiductile faults are present in this area.

STOP 13. Overlook - view of River, Dunderberg Mountain
In the nearly continuous exposures along Route 206 from the Bear Mountain Bridge south to Camp Smith numerous faults have been mapped. These faults are predominantly the semiductile type with excellent phyllonite zones and abundant evidence for right-lateral oblique thrust faulting. Correlation of tectonic features across the Hudson to Dunderberg Mountain is excellent and northeast-trending Mesozoic faults are largely absent. Mesozoic faults are predominantly north- and northwest-trending suggesting that the left-handed bend in the Hudson River here is controlled by brittle fractures of Mesozic age.
These outcrops of biotite granite gneiss are not clearly either "Storm King Granite" or "Canada Hill Granite". However, intrusive relationship in amphibolite can be seen in the roadcuts. A comparison of this rock with the "Reservoir Granite" seen at the next stop is in order.

Excellent exposures
Excellent exposures of amphibolite, alaskite, and hornblende granite gneiss ("Storm King Granite") may be seen at sharp bend in road.

Trace of Wallace Pond fault.
Entrance to Camp Smith and trace of a major semiductile fault -- Wallace Pond fault.

STOP 14. "Reservoir Granite" and mylonite zones
The "Reservoir Granite" (Berkey and Rice, 1919) is a widespread granitic rock type east of the Canopus fault zone. Doug Mose has dated a collection of rocks from this locality and from northeast of here and obtained an Rb/Sr isochron of approximately 1250 m.y. for both collections (Helenek and Mose, 1976). The granite has intrusive contacts with amphibolite with which it is commonly associated and may represent either remobilized felsic volcanic rocks (interlayered with amphibolite) or truly intrusive granite.
Excellent mylonite zones cut this garnet-bearing granite. Biotite-rich blastomylonite zones contain syntectonic garnet and intrafolial folds indicating right lateral movement. "A" lineations are subhorizontal. The granite gneiss has biotite and muscovite growing in ductile shear zones and garnet is retrogressively altered to biotite. This tectonic fabric probably represents Ordovician retrogression. The regional grade in Middle Ordovician rocks at this locality is between biotite and garnet zone.

STOP 15. Optional Annsville fault - tectonic breccia
Low road cuts of phyllite.
Exposures of marble with rounded inclusions of gneiss were cited by Bucher (1957) and by Ratcliffe (1971) as evidence for Middle Ordovician erosion beneath the "Annsville Phyllite". I have changed my opinion of this strange rock and interpret this polymict breccia as a tectonic-mylonitic breccia resulting from large-scale extension and flowage in Proterzoic shear zones. Dismembered calc-silicate rocks form the inclusion within the strongly flow-banded marble. Breccias like this are present throughout the Hudson Highlands and are not restricted to zones of Paleozoic faulting.
A fault between "Annsville Phyllite" and this marble is exposed on the north side of these cuts, where the flow-banded marble is dragged in right-lateral sense into the N. 40° E. -trending Annsville fault. Right-lateral minor folds in fluxion banded rocks and minor thrust faults suggest right-lateral, oblique thrust faulting. Exposed contacts in the sand pits to the north, reveal ribbon-quartz mylonite and diapthoritic phyllonite. Syntectonic muscovite, tremolite, actinolite, epidote, and phlogopite are formed in sheared rocks of appropriate composition.
I interpret the Annsville fault as a post-Middle Ordovician, probably Late Ordovician fault, perhaps equitable with the Thiells fault.
Numerous earthquakes have been recorded in the Annsville area, most recently in January 1980 (Fig. 1). Despite the repeated activity, faults of probably Mesozoic age are largely absent. Faults seen at the surface are all characterized by mylonitic-ductile deformation. The northeast-striking, southeast- dipping phyllonitic shear zones satisfy the available fault-plane solutions.

STOP 16. Canopus pluton and western Canopus fault
Park at aqueduct crossing. Canopus pluton and westem Canopus fault: a probable Proterozoic Y fault zone. (See figs. 16a,b,c and 17)
Road cuts of quartz monzonite and granodiorite of the Canopus pluton. Large rectangular microcline-perthite phenocrysts, showing Rapikivi-like mantles, produce a striking igneous lamination trending north to northwest. Ductile shear zones related to the Canopus fault show right-lateral drag of the older fabric. Locally small pegmatite dikes crosscut augen, gneiss and sheared igneous rocks.
The Canopus pluton has been interpreted as a Proterozoic Y syntectonic pluton on the basis of Rb/Sr and K-Ar dating by Dick Armstrong (Ratcliffe and others, 1972). The pluton is deformed in a right·lateral shear couple.

STOP 17. Mylonite gneiss in western Canopus fault
Strongly mylonitic gneiss at the eastern border of the Canopus pluton are exposed in the road cuts. Biotite-rich blastomylonite and more felsic, mylonitic, quartz-feldspar layers produce a strikingly well-layered rock. Reclined, right-lateral, isoclinal folds plunge steeply southwest in the N. 20° E., 80° SE. dipping shear fabric. A strong lineation is produced by the intersection of compositional banding and mylonitic foliation. The tectonic fabric seen here is restricted to local shear zones of Proterozoic Y age.

STOP 18.Eastern Canopus fault
Eastern Canopus fault and overprint by probable Paleozoic fault fabric of the Dlcktown fault. (See fig. 17)
Walk east to base of small cliffs.
This is a complex fault zone, consisting of pink and black biotite-rich augen, gneiss, biotite-rich blastomylonite and intrusive pegmatite. Excellent right-lateral folds, adjacent to ductile shear zones, plunge S. 45° E.
A dark-gray mafic dike crosscuts sheared gneiss and blastomylonite. Metamorphosed dikes like this one are common throughout the Hudson Highlands and are possibly of Proterozoic Z age. Chemically these dikes are distinct from lamprophyres and from Triassic diabases and are currently being, studied. No definitive age data are currently available. However, K-Ar whole-rock dates range from 900 m.y. to 240 m.y. in six samples. The fact that they are metamorphosed, locally foliated, and confined to rocks of Proterozoic age suggests that they are old dikes. A series of small mafic stocks, dikes and small plutons are recognized in the Highlands in the vicinity of the Canopus pluton. Those igneous rocks are mafic to ultramafic and always are strongly metamorphosed. These mafic rocks and plutons represent a very obscure period of igneous activity in the Hudson Highlands but appear to be post- to very late syntectonic in the Proterozoic Y deformation. Locally they are extremely abundant.
A traverse up the hill from this point is instructive and shows increasing progressive overprinting of the Canopus fault fabric by the Annsville-Dicktown fault. In the Dicktown fault zone biotite and garnet are retrograded to chlorite and chlorite rich phyllonite is common. The contrast in the metamorphic grade of a retrogressive mineral assemblages within mylonite rocks may be useful in distinguishing Proterozoic Y faults from Ordovician ones in this area. To the east the Paleozoic grade increases to sillimanite zone and mineral assemblages within mylonites of both Proterozoic Y and Paleozoic age are not distinguishable. Outcrops at this stop, however, are well within the area of relict Proterozoic Y Ar40/39 biotite ages obtained by Dallmeyer and Sutter (1976). These data suggest that the Proterozoic rocks of this area never were heated above the biotite blocking temperature of approximately 350°C since the late Proterozoic. These data are consistent with the assignment of the biotite- rich blastomylonites seen here and at Stops 15 and 16 to Proterozoic Y fault zones. Chlorite-rich phyllonite associated with the Dicktown fault, however, is probably Ordovician.
Throughout the Canopus zone east to the California Hill fault (Fig. 1), no faults having Mesozoic fault characteristics have been recognized, despite detailed mapping. However, as at Annsville, earthquakes are recorded from this zone. The event near the California Hill fault (Fig. 1) is associated with a zone of very ductile, probably Proterozoic faulting.
Faults commonly dip 80° SE. or NW. but locally may dip 60° SE. These tectonic features (Figs. 1 and 4) probably extend through the continental crust and must be present as significant inhomogeneous (weak) zones at depths of 1-10 km where earthquakes are occuring. I interpret this highly faulted zone as the ancestral grain that localized Mesozoic faulting in the area to the south traversed on the first day of this field trip. (See fig. 16c)

Exposures of "Canada Hill Granite"
Exposures of "Canada Hill Granite" and rusty biotite-sillimanite paragneiss typical of the western block of the Hudson Highlands.

Canopus Lake - crossing Denny town fault
Canopus Lake - crossing Denny town fault that marks the beginning of Canopus fault zone, crops of rusty paragneiss, amphibolite marble, calc-silicate rock, and magnetite-bearing quartzite.

STOP 19. Dennytown fault, Poughquag Quartzite inlier
(See figure 1 for location)
This exposure marks the southwestern limit of a series of faulted slivers of basement gneiss and Poughquag Quartzite that extend southwest from the front of the Hudson Highlands along the Denny town fault. These inliers are surrounded by phyllonite zones marked by chlorite-sericite-epidote mineralization and ductile fold styles. Fold axes, within phyllonite plunge southeast in 80° to 60° SE. dipping surfaces. Excellent right lateral offsets and folds are seen in thin section and outcrop. A northeast plunging "a" lineation defines the probable slip direction.
I interpret this fault as an Ordovician, right-lateral, oblique thrust fault parallel to the Proterozoic Y fabric in the gneiss. The northward extension of these fault zones is uncertain but they probably extend out into the Paleozoic cover rocks north of the Hudson Highlands.
Participants from Saturday's trip may be struck by the similarity of these exposures to the quartzite-phyllonite zone seen on Stop 1 near Boonton, N.J. This similarity should drive home the point that phyllonitic shear zones of probable Paleozoic age are regionally important features within the Ramapo seismic zone. Earthquake activity here seems to be more associated with semiductile features such as the Denny town fault than with brittle-type Mesozoic faults.

16A: RIFT TECTONICS INFERRED FROM VOLCANIC
AND CLASTIC STRUCTURES (Saturday)
WARREN MANSPEIZER
Newark, N.J.
Tholeiitic basaltic lava flows and intrusives of Late Triassic and Early Jurassic age clearly mark and distinguish the upper part of the rift-valley stratigraphic sequence in the onshore and offshore basins of eastern North America and northwest Africa. These igneous rocks were emplaced over a vast area, perhaps 2500 km long and 1000 km wide, during an episode of crustal extension and sea-floor spreading and hence exhibit a variety of structures reflecting the complex history of the basin at that time. Where these volcanics are interbedded with sediments having paleocurrent and/or paleo-environmental attributes, important conclusions may be deduced about the tectonic behavior of the basin from each rock type.
The objective of this field trip is to study a typical rift facies of interbedded volcanics and sediments, thereby providing a frame-work for interpreting the tectonics of the basin during crustal extension and sea-floor spreading. Figure 1, a diagrammatic sketch through the section, shows the kinds of structures and facies that we shall observe on the field trip. Many of these features, such as tumuli, subaqueous flow lobes and palagonite forset bedding have not been reported from rift volcanics of eastern North America. Figure 2 shows the route of our field trip.

16: RIFT TECTONICS
INFERRED FROM VOLCANIC
AND CLASTIC STRUCTURES

Sandstones and mudstones
Alternating beds of red sandstone and mudstone with a few thin interbeds of gray siltstone and dark gray to black micaceous shale, occurring below the first overpass. These siltstones yield a probable Upper Norian palynoflorule and occur about 1100 m below the First Watchung Mountain Basalt (Cornet and Traverse, 1975, p. 27). Sporadic exposures of sandstones and mudstones with fining-upward sequences, chacteristic of meandering streams, occur along Interstate 280 for the next 4.4 miles.

STOP 1. Passaic Formation: Central Basin Facies
Objective: to examine a fluvial sequence of the central basin facies.
Background: information for this stop is found in the text under, 'Central Basin Facies: Fluvial-Playa.'
Figure 22, a stratigraphic section of this stop, shows characteristics of the fining-upward sequence, namely: cut-and-fill channels, channel lag concentrates, cross-bedded arkosic sandstones, overbank deposits of reddish-brown mudstone with calcrete paleosols, gray-green to green shales with plant fragments, worm burrows, roots (?) and copper mineralization (chrysocolla and malachite.)
Petrographic and paleocurrent studies along this highway, and elsewhere in this stratigraphic horizon, indicate that the sediment was derived from a deeply weathered metamorphic terrane to the north and east., and transported to the basin across a broad southwest-sloping pediment.

Great Notch, on the western horizon
Great Notch, on the western horizon, is a 'wind gap' cut into the First Watchung Mountain by streams draining Glacial Lake Passaic.

Contact Passaic Fm / Orange Mountain Basalt.
Contact of the Passaic Formation with the overlying Orange Mountain Basalt. The columnar basalts of the lower flow unit is well exposed as is the contact with reddish-brown ripple-marked sandstones of the Passaic Formation.

Passaic Formation / Orange Mountain Basalt.
Contact of the Passaic Formation with the overlying Orange Mountain Basalt. The columnar basalts of the lower flow unit is well exposed as is the contact with reddish-brown ripple-marked sandstones of the Passaic Formation.

Beginning of the upper flow unit
Beginning of the upper flow unit with its characteristic ropy pahoehoe-pillowed surface.

Transverse cross section of subaqueous flow lobes.
Transverse cross section of subaqueous flow lobes. Note the arcuate pattern of the pillow lava complex. These structures will be examined in the lower and upper New Street Quarries at Stop 3.

STOP 2. Contact of the Orange Mountain Basalt with underlying Passaic Fm.
Objective: to determine the paleoflow direction of the lava and the paleocurrent direction of the underlying sediments.
Background: see the text under, 'paleoflow structures in rift volcanics: pipe vesicles and pipe amygdaloids.'
Figure 6 is a composite sketch of the structures found at the outcrop. The section shows the lower flow unit of the First Watchung basalt with southwest plunging pipe amygdaloids and vesicles, overlying an irregular surface of cross-bedded (southwest dipping) pebbly arkosic sandstones and conglomerates with large clasts of rounded quartzite, carbonate and shale chips. Figure 7, a stereographic projection of the paleoflow and paleocurrent data, indicates that the lava flowed to the northeast transgressing a regional sedimentary paleoslope inclined to the southwest.
This site is also of some historical importance. Alexander Hamilton, inspired by the power of the Passaic River as it cascaded over the Great Falls of Paterson, informed the New Jersey legislature that he had found the ideal site for industry in the new nation.

STOP 3. New Street Quarry
Orange Mountain Basalt: Upper Flow Unit, New Street Quarry.
Objective: to examine subaqueous volcanic structures including: pillow lavas, flow lobes, fissure eruptions, a volcanic cone (?), and zeolite mineralization. Caution should be exercised in the quarry and participants should not climb the upper quarry walls.
Background: An extensive text is developed for this stop and found under 'pillow lavas and subaqueous flow lobes'.
The walls of this quarry and an adjacent quarry, long favorites of mineral collectors for their beautiful and diversified suite of zeolites, also exhibit a splendid array of subaqueous volcanic structures (see Fig. 11). Participants should first examine the structures of the east (or far) wall, noting the amygdaloidal and vesicular upper contact of the lower flow unit and the overlyng Tomkeieff sequence, which is overlain by bedded pillow lavas and a second Tornkeieff sequence. Note also spiracles in the lower colonnade and cross-sections of polygonal joint sets of the entablature. Follow the structures along the south wall, walking west, and note the increase in pillow lavas with a concomitant decrease in massive basalt. On the west wall we may observe the characteristic concave-downward arcuate form of overlapping flow lobes in transverse section. Pinching and swelling pillow buds elongated N-S in arcuate bundles distinguish the flow lobes from the overlying bedded pillows which appear to be stacked one on the other and elongated E- W.
Although the contact between the two types of pillows appears to be unconformable, the absence of eroded pillows along the contact indicates that they are comformable. Note the manner in which the younger pillows cascade off the flow lobe, building up slopes of about 40°. In general, the pillow buds are very dense with radial joint structures and few minute vesicles, indicating that they formed in deep water.
The absence of pillow-derived debris within the interstices of pillow complexes indicates that the debris was washed out of these pockets in a well-agitated lake. The occurence of interstitial angular basaltic fragments (surrounded with quartz, calcite, perhnite and other zeolites) indicates that the fragments were derived from the checkered exterior rinds of the pillows by circulating fluids, perhaps ground water. The original debris was probably redeposited in a deeper part of the basin, along the border fault.
The flow lobe appears to flare out and to plunge westward, where it may be studied in the walls of the lower New Street Quarry. At some appropriate time, we shall enter that quarry as a group. Figure 12, a field sketch of its east wall shows three distinct episodes of vulcanism: (1) an older episode of flow lobes; (2) a medial phase of massively bedded, moderately coarse-grained igneous rock that slopes away from a central point and overlaps the distal and advancing end of a flow lobe; and (3) a younger zone of bedded pillow buds that overlie both the steep slope of the subaqueous volcano (?) and the flow lobe. The origin of these features should encourage a lively discussion.

STOP 4. Feltville Formation
Feltville Formation in contact with the overlying Preakness Basalt.
Objective: Primarily to have lunch in a pleasant setting, and secondarily to examine a fluvial-deltaic (?) facies.
Background: A stratigraphic section of this site is found in figure 23, and shows two fairly complete fining upward sequences of point bar deposition, overlain by the Second Watchung lavas along an irregular contact with pahoehoe structures, pillows, soft sediment loading structures and injection features into the underlying mud.
Note the typical fining-upward sequence with its channel deposits of coarse clastics, overlying planar beds of sandstone, which is overlain by large, low angle crossbedded sets and then by a thick sequence of ripple drift cross-laminations with shale interbeds that are cut through by a very large channel with cross-bedded pebbly sands, plant debris and thin stringers of coalified plants. The channel sands are overlain by low angle planar cross-beds, trough cross-beds and finally by fine-textured ripple drift cross-lamination. Convolute bedding and parting lineations are common with the prevailing trend of the latter striking N 5O° E. Parting lineations, in conjunction with the cross bedding, indicate that the paleocurrent was to the southwest. We can easily follow these beds to the south (using the basalt as a marker bed) where they interfinger with distributary-type channel sands of the deltaic sequence.
Look for evidence of strike-slip movement on the far wall. The pockets of pillow lavas indicate that the lava flow dammed an existing lake or stream. The pillows are perhaps best exposed in the roadway adjacent to the lunch stop, where they may be examined against the fine-splintery columnar jointing so diagnostic of the Second Watchung lavas.

First Watchung lavas and Glacial Lakes
The road is underlain by basalts of the first Watchung lavas. Glacial lakes are abundant in the area. As we proceed west onto Long Hill Road we will descend the backslope of the First Watchung.

STOP 5. Feltville Formation
Feltville Formation: subaqueous fan, marginal border facies.
Objective: to determine the provenance and depositional setting of these massively bedded conglomerates.
Background: field descriptions of this stop are found in the text under 'Marginal rift facies: fan delta'. Note figures 26 and 27. The section, about 45 m thick of coarse-grained and poorly sorted clasts with average grain size of about -4 to -6 phi (16 mm to 64 mm), occurs immediately below the base of the Second Watchung lava. The clast population has a graphic mean (Folk, 1974) of -4.5 phi and is very poorly sorted with a standard deviation of 2.4 phi (Fig. 28). The clasts are composed principally of carbonate, quartzite, low-rank metamorphics and most notably, vesicular basalt. Many of the clasts are reasonably well-rounded, imbricated, and show subtle grading which is perhaps one of the most distinctive - but elusive - aspects of this facies. In order to determine grading patterns of sedimentation, we measured the grain sizes of all clasts with a phi-ruler on a 2.5 cm sampling grid drawn perpendicular to bedding. The data, included on representative graphs of that exercise (Fig. 29) show: (1) the cyclical pattern of deposition and subtle stratification; (2) each cycle seems to begin with an inverse grading sequence, marked by a subtle increase in grain size upward in section, and followed by an abrupt decrease in grain size; (3) reverse grading is repetitive with each episode transporting slightly coarser components; and (4) many cycles are symmetrical.
Each complete depositional cycle consists of an erosional basal contact followed by a depositional couplet of inverse grading, followed by normal grading and an upper contact marked by finely comminuted particles in ripple drift crossstratification (Fig. 26). Complete cycles are rare, and much of the section is marked by subtle and shallow cut-and-fill channels, (Fig. 27).
At the western end of the outcrop, the beds are graded and the bedding planes have a slightly arcuate pattern. Are we looking at a transverse section of a fan, or is this a drag structure along a fault?
Note that the section lacks features commonly associated with Triassic-Jurassic fluvial deposits, namely: rootlets, caliche deposits, plant fragments, dessication cracks, red beds, dinosaur footprints, worm burrows and overbank deposits.
Observe clast rounding, imbrication and composition.
Although quartzites, carbonates, and low rank metamorphics are fairly common, perhaps the most significant clasts are the vesicular basalts. Together with the imbrication direction, it suggests that the lavas of the First Watchungs flowed westward over a low-lying fault escarpment.

Most of the lakes in the area resulted from glaciation.

STOP 6. Boonton Formation (Fanglomerate).
Marginal Border Facies
Objective: To examine an alluvial fan facies within the border fault zone.
Background: Field descriptions and photographs of this section are included in the text under, 'Boonton Formation: Marginal Border Facies'.
Because the section has been polished by glacial scour, conglomeratic structures are displayed in great detail. Cyclical and laterally continuous beds of poorly sorted debris flows grading upward into cross-bedded and ripple marked sheet-flood deposits are characteristic of the section (Fig. 34). Many of the cycles are incomplete, having been partially eroded by a subsequent debris flow. Each section is about 2 to 3 cm thick and occurs within larger cyclical units of about 1.5 m thick. The clast population has a graphic (Folk, 1974) mean size of -3.3 phi, and an inclusive graphic standard deviation (Folk, 1974) of 2.2 phi (Fig. 28); it is, therefore, very poorly sorted. In general, the grains are angular and primarily composed of a quartzite, gneiss and vesicular basalt with subordinate amounts of amphibolite, slate and greenstone schists. They appear to have been derived from a local source.
Some of the primary structures seen at the section include: ripple drift cross-lamination, dessication cracks, cut-and-fill channels, normal and inverse grading, sand waves, parting lineations, antidunes (?), random fabric, sand shadows, dreikanters and oriented clasts (Fig. 33).
Particle orientation was determined from clasts having a length to width ratio of at least 1.3: 1. The prevailing long axis orientation is west-to-east with clast imbrication to the west (Figs. 31 and 32). This is compatible with a preliminary paleocurrent study showing that the clasts were transported to the basin by east-flowing streams. The occurrence of aligned ventifacts indicates that the wind was an effective agent of erosion, and may explain the deficiency of fine sand and clay size particles on the alluvial fan.

Boonton Reservoir
Boonton Reservoir on left-site of famous Boonton fish fossils.

Glacial Lake Passaic
We are traveling on the lake bed of glacial Lake Passaic, which formed as the meltwaters became impounded between the N.J. Highlands on the west, the Second Watchungs to the east and south, and the moraine to the south. At its greatest extent, the lake was 30 miles long, 10 miles wide and 240 feet deep (Kummel,1940).

Passaic River

Third Watchung lava flow on S horizon (see Olsen, this book).

Backslope of the Second Watchung lava flow.
Coarse-grained diabasic texture may be examined near upper part of the exposure.

Lava / Feltville Fm contact
Contact of lava flow with the underlying Feltville Formation. Note the fine-textured joints of the entablature. When exposed during road construction, the formation consisted of cross-bedded feldspathic sandstone (10 m) underlain by thin stringers of coal with underclay. A similar section may be studied in the parking lot of the Daughters of Israel Nursing Home, 1155 Pleasant Valley Way, West Orange (about 3/4 mile south).

Backslope of the first Watchung lava flow
Outlines of pahoehoe toes may be studied in roadcut.

STOP 7. Orange Mountain Basalt; lower flow unit
Objective: To examine a Tomkeieff sequence of colonnades and entablatures near the classical site of O'Rourke's Quarry. (See photograph facing the title page of this article.)
Background: This structure is described in the text under 'Columnar Jointing'.
When built in 1969, this road cut was the deepest federally-financed highway cut east of the Mississippi River. About 33 m deep, the cut exposes a complete section of the lower flow unit of the Orange Mountain Basalt, and a broad array of joint patterns that formed as the basalt cooled. The large "basin" structure on the southeast wall was first described about 100 years ago by J.P. Iddings (1886) of the U.S. Geological Survey in John O'Rourke's Quarry, about 300 m south of the roadcut. While such complete structures have not been observed elsewhere in the Watchungs, similar joint structures, e.g. chevrons, oblique and reverse fans and rosettes (terminology of Spry, 1962) may be studied in this roadcut and in almost every quarry along strike for a distance of 80 to 100 km.
This structure (about 33 m thick) conformably overlies a fluvial red bed sequence of shales and sandstones and, when first exposed, displayed a complete Tomkeieff sequence of: (1) a lower colonnade (10-15 m); (2) entablatures (20-30 m); and (3) an upper colonnade (1-2 m) (Fig. 17). While the lower colonnade is composed of massive 4-5 or 6-sided polygonal and subvertical prisms, the entablature is composed of long (25-30 m) slender narrow joint prisms that radiate from an apparent focus. Several juxtaposed bundles or sheafs of radiating prisms may be observed in the roadcut, comprising fan and chevron-like features. Cross joints, intersecting radiating prisms at high angles, are prominent and appear to be concentrically arranged about the apex of radiation. An incomplete section pseudo-columns overlie the entablature.
Figure 18, depicting mineral and textural variations within the structure, shows an increase in grain size, an increase in the abundance and size of the interstitial glass, and an increase in the olivine content in the entablature (Fig. 19). This suggests that although cooling may have proceeded very slowly from the sediment-volcanic interface, once a ground mass capable of transmitting stress was established the remaining melt cooled almost instantly. The obscure joint pattern in the upper colonnade may form from convective heat loss near the upper part of the flow.
The early cooling history of the magma is manifested by well-developed horizontal striations observed on the joint surfaces of the lower colonnade. While Iddings (1886) may have been the first to report horizontal striations on joint surfaces (from O'Rourke's quarry), James (1920) speculated that these striations represent successive stages or pulses in which the rock broke and the columns formed. Recent studies by Ryan and Sammis (1978), and Justus and others (1978) at this site show that the striations are records of discrete thermal events, characterized by sudden periods of crack advance in the cooling basalt. Features such as chisel marks, pinch and swell and kink structures on the curvi-columnar joints may also represent an episodal cooling history. Each of these features may be observed on the walls of the highway cut.
The striations reported by Iddings (1886) show up on joint surfaces of the lower colonnade as cyclical bands of smooth and rough zones, about every 5-7 cm. Ryan and Sammis (1978) report that as the crack growth procedes, the first-formed zone is smooth and associated with a thermal shock event; the second zone is rough, has positive relief, and is associated with the halting of each crack advance.
Joints of the entablature are also cut by concave-upward "dish-like" joints that are cut by strike-slip faults. While the origin of this structure is debatable, it trends N 50° E and evidently formed after the basalt cooled and before faulting occurred.

Dike intrusion into fluvial channel sands.

16B: RIFT TECTONICS INFERRED FROM VOLCANIC
AND CLASTIC STRUCTURES (Sunday)
WARREN MANSPEIZER
Newark, N.J.
Tholeiitic basaltic lava flows and intrusives of Late Triassic and Early Jurassic age clearly mark and distinguish the upper part of the rift-valley stratigraphic sequence in the onshore and offshore basins of eastern North America and northwest Africa. These igneous rocks were emplaced over a vast area, perhaps 2500 km long and 1000 km wide, during an episode of crustal extension and sea-floor spreading and hence exhibit a variety of structures reflecting the complex history of the basin at that time. Where these volcanics are interbedded with sediments having paleocurrent and/or paleo-environmental attributes, important conclusions may be deduced about the tectonic behavior of the basin from each rock type.
The objective of this field trip is to study a typical rift facies of interbedded volcanics and sediments, thereby providing a frame-work for interpreting the tectonics of the basin during crustal extension and sea-floor spreading. Figure 1, a diagrammatic sketch through the section, shows the kinds of structures and facies that we shall observe on the field trip. Many of these features, such as tumuli, subaqueous flow lobes and palagonite forset bedding have not been reported from rift volcanics of eastern North America. Figure 2 shows the route of our field trip.
This trip contains only those places not visited on trip 16A.

16B: RIFT TECTONICS INFERRED FROM VOLCANIC
AND CLASTIC STRUCTURES (Sunday)

STOP C. Lower Flow Unit Preakness Basalt.
Objective: To examine tumuli (also known as pressure domes or schollendomes, Macdonald, 1953).
Background: Information about this structure is found under Tumulus, also figures 8 and 9. The exposed tumulus structure, about 7 m high and 15 m wide, consists of a central core of massive basalt with columnar joints (1-1.5 m wide), an overlying zone of radiating entablature joints (0.5-1.0 m wide), and an upper colonnade with poorly defined columnar joints and vesicular to brecciated basaltic glass. The structure is overlain by a pillow-pahoehoe complex that thins along its crest and thickens along its flanks and adjacent troughs. A second flow unit overlies both structures and consists of massive colonnades with bent pipe amygdaloids, indicating that the lava flowed towards the crest of the tumulus. Although this tumulus did not feed the second flow unit, it appears to have fed (through the overlying brecciated zone) the pillow-pahoehoe complex.
The section also shows an interesting assemblage of ellipsoidal bunlike structures, including: pahoehoe toes with concentric layers of vesicular and non-vesicular basaltic glass, and with flat bottoms and rounded tops; (2) flattened lava tubes (?) with concentric structures and hollow interiors in transverse cross section; and (3) pillow buds with circular transverse sections and ellipsoidal longitudinal sections, vesicular cores and pipe amygdaloids elongated radially near the bud edge. and radial and concentric joints in cross section. Moreover, note: the variety of bun shapes and sizes; the volcanic debris separating these bun-like structures; the occurrence of several tumuli crests at different heights along the exposures; and the surface topography of the lava flow as expressed by the tumulus surface.
Did this structure form in water? When did it form relative to the pillow-pahoehoe complex? How do these bun-shaped structures compare to those at the New Street Quarry? Are the buds a tangled mass of independent sack-like structures or a tangled mass of cylindrical interconnected pillow buds, lobes and pahoehoe toes? What does the structure tell us about the relationship between topography, isotherms and the formation of columnar joints. We shall continue our discussion of this point at our next stop.

2nd flow unit of the First Watchungs
Vesicular pahoehoe flows of the 2nd flow unit of the First Watchungs behind stores on right.

A wind gap cut into the First Watchung Basalts.

Eagle Rock Reservation. Park Buses -Lunch Stop.

Trap rock quarry
Trap rock quarry, entablature structures may be seen from the road.

Red beds with fining upward cycles.

Entering the South Mountain Reservation
Back slope of the First Watchung Mountains on the left (east); the Second Watchung Mountain on the right (west).

STOP E. Feltville Fm contact Orange Mountain Basalt.
Feltville Formation in contact with the underlying Orange Mountain Basalt.
Objective: Primarily to determine whether the second flow unit is intrusive or extrusive. And secondarily to examine the carbonate sequence near the base of the Feltville Formation.
Background: This section is discussed in the paper under 'Emplacement of the Watchung Lavas', and 'Central Basin Facies: Lacustrine-Deltaic Facies', see figure 20. The issue before us at this site is the same as the one confronted by a group of emminent geologists more than 100 years ago, including: Cooke (1868), Russel (1878), Davis (1882) and others. Figure 20 will be helpful in your examination. Note the irregularity of the contact, the 'baked' mudstones and sandstones, vesicular sandstones, the occurrence of marble float along the carbonate horizon, the occurrence of pillow lavas, and the stratification in the basalt. Moreover, note pillow vesicularity, pipe vesicles and amygdaloids elongated radially near the bud edge, and brecciated clasts of basalt and red beds within pillow interstices.
Are the pillow buds independent sack-like structures or are they interconnected cylindrical-to-sack-like masses? Do they rest directly upon each other, or are they separated by baked sediment, weathered sediment or basalt, or an old soil horizon? Is the basalt stratification a relict sedimentary structure or a primary volcanic structure? Is the irregular sedimentary-igneous contact an old soil horizon or an intrusive-baked contact? Recall that this horizon is stratigraphically equivalent to the section that we studied at the New Street Quarry.
Upstream the pillow buds become larger, more numerous, bedded, and overlain by a complete Tomkeieff sequence. This part of the section is quite similar to the upper part of the section at New Street.
The second reason for examining this section is to study the sequence of shelf carbonates and siltstones that unconformably overlie the basalt, and crop out sporadically from Feltville to Pluckerman's Ravine.
The carbonates occur as thin discontinuous limestone lenses, about 5-20 meters above the igneous contact, and interbedded with gray and reddish-brown shale and gray calcareous thinly laminated siltstone. A trench dug into the hillside exposes the section (Fig. 24)(McGowan. 1980). The limestones, about 10 cm thick and 100 m long, display a variety of shallow water structures including: cross-bedding, dessication cracks, rounded intraclasts cemented with sparry calcite, ripple marks, abraded algal debris and erosional lower contacts. Although some of these features are ambiguous with respect to environments of deposition, the assemblage of structures point to a shallow water carbonate bank. See also McGowan (1980), who has made an extensive study of this formation. Olsen (pers. comm.) also reports the occurrence of thinly laminated deep-water carbonates with whole fish fossils stratigraphically beneath the shelf carbonates. Plant fragments, dinosaur footprints, fish fossils, algal mats, ostracods, and one branchiopod shell are reported from this section (Olsen, 1975; Dahlgren, 1975; McGowan, 1980). Flaser bedding, ripple drift cross-laminations, parting lineations and small scale trough cross beds may be observed in the overlying siltstones and sandstones. The average direction for the trough cross beds and parting lineations is 180° and 145° respectively (McGowan, 1980).

17: FOSSIL GREAT LAKES OF THE NEWARK SUPERGROUP IN NEW JERSEY
PAUL E. OLSEN
Bingham Laboratories, Department of Biology
Yale University, New Haven, Connecticut
Because Newark Basin lacustrine rocks are (1) often composed of sedimentary cycles, (2) traceable over very large areas, and (3) unusually rich in fossil remains, they are among the most interesting and challenging of Newark Supergroup deposits. While lacustrine sequences are found in all sedimentary divisions of the Newark Basin, those of the Lockatong, Feltville, and Towaco formations are known in greatest detail and are therefore the focus of this field trip. I concentrate on the interpretation of the lake sediments, paying special attention to some fundamental problems in their interpretation. In addition, I touch on some relevant paleozoology.
2011: Views along I 80,which duplicate those from NYSGA 1980 Trip 1, have not been reproduced here.

17: FOSSIL GREAT LAKES OF THE NEWARK SUPERGROUP IN NEW JERSEY

Passaic Formation
Newark Campus sits on late Norian or earliest Rhaetic sandstones and siltstones of the Passaic Formation.

Newark Museum on left

Along the strike of the Passaic Formation.
Route 21 follows the west bank of the Passaic River along the strike of the Passaic Formation.

Pass Belleville Avenue
Just north of Belleville Avenue and 1.1 miles east of Route 21 is the old Schuyler Copper Mine worked from about 1720 to about 1900 (Lewis, 1906). The ore occurs in gray arkosic sandstone and gray siltstone invaded by small dikes and sills of diabase. Lewis (1906) lists chalcocite, chrysocolla, and malachite as the major copper minerals with minor amounts of azurite, cuprite, and native copper.

Fragments of phytosaur skull
Fragments of phytosaur skull and reptile footprints found in Passaic Formation "brownstone" quarry near here (Edwards, 1895; Lull, 19S3).

Route 3 cuts across strike through Passaic Fm.
Route 3 cuts across strike through Norian and Late Carnian Passaic Formation. This portion of the Passaic Formation is the lateral equivalent of the entire Delaware River section of the Passaic and upper Lockatong (see Van Houten, this Fieldbook)

Entering Hackensack Meadows.
About 0.2 mi. southwest of this point are excellent exposures of Passaic Formation including a series of gray sandstone beds (ca. 2 m) stained with chalcocite, malachite and azurite. Old (?exploratory) shafts are evident in the outcrops. Lithology of copperbearing units very similar to beds at Schuyler Mines. I have found reptile footprints assignable to Rhynchosauroides brunswickii and Grallator sp. and in addition, horseshoe crab tracks called Kouphichnium and Scoyenia burrows in the fine red siltstones surrounding the gray sandstone. Lower red beds of exposure contain well developed caliche horizons similar to those described by Hubert (1977) from more or less contemporary beds of the New Haven Arkose (Hartford Basin). Futher southwest, (0.3) mi are additional exposures along former Erie Lackawanna Railroad tracks showing an unusual reverse fault dipping to the west and downthrown on the east. Slickensides confirm the dipslip nature of the fault. Hackensack Meadows, over which Route 3 crosses, are underlain by relatively finegrained red and minor gray beds of Passaic Formation.

Lateral equivalent of Graters Member?
Ridge just south of here (Secaucus) has exposures of gray sandstones and siltstones which could be lateral equivalent of McLaughlin's (1948) Graters Member.

Open cut in Stockton Formation
On right is open cut in Stockton Formation and west portal of tunnel for Penn Central Railroad. Cut exposes upper Stockton beds described by Darton (1883). At east end of cut at tunnel is excellent exposure of the contact between the Stockton Formation and the Palisade Diabase. Stockton beds dip at 15° NW while the irregular contact dips at 60° NW. This contact is locally welded according to Darton (1890) and Lewis (1908). This is one exposure where the Palisade Sill is described as having a dike-like appearance. Actually, these exposures and similar ones nearby are perhaps better explained by a local stepping up of the Palisade Sill as shown in Figure 26.

Stockton / Palisade Sill contact
Contact of uppermost Stockton with Palisade Sill directly on right (east). Stockton dips 15° NW and the contact dips 45° to 80° NW. This appears to be a continuation of the contact surface exposed at the Penn Central tunnel previously described. Recrystallized arkose of Stockton Formation is sheared and dragged upwards close to contact with fine slickensides indicating down-dropping to the west. There are no indications of movement in the diabase, however. Basal Lockatong hornfels 100 m to the north, dip 15° NW and lie concordantly on the Palisade Sill. A possible interpretation of these exposures might be that the apparent movement in the Stockton occurred during intrusion of the sill.

Dip slope of Palisade Sill
Dip slope of Palisade Sill mantled by northwesterly dipping Lockatong Formation. Contact appears concordant from here to Granton Quarry.

STOP 1. Abandoned Granton Quarry
Abandoned Granton Quarry in lower Lockatong Formation hornfels and overlying Granton Sill. Turn left off Route 1 and 9 into parking lot for Shop-Rite employees at Diana Stores Corporation.
Eleven Lockatong cycles are exposed on the sill-capped hill: seven are exposed on the south facing exposure (Figure 27); three additional cycles are exposed on the east facing exposure; and all 11 cycles are exposed on the north facing exposure but are not accessible without special permission. The base of the section appears to be 38 - 46 m above the contact with the Palisade Sill (Van Houten, 1969). This contact may be following what was, prior to intrusion, the Stockton-Lockatong contact.
According to Van Houten (1969) these Lockatong hornfels include calc-silicate varieties in the middle carbonate-rich part, and extensively feldspathized and recrystallized diopside-rich arkose in the upper part. Some beds of arkose show well developed crossbedding (Figure 28). Because of the buff arkose at the top of nearly every cycle, these are the most visually graphic of the detrital cycles seen on this field trip; here the many correlated changes occurring though individual cycles can be easily seen (Figure 29).
Cycles 3 and 7 (Figure 29) have produced representatives of all the known (skeletal remains of) Lockatong holostean Semionotus, and the amphibian Eupelor. The basal portions of division 2 of both of these cycles have extremely high densities of fossil fish, expecially the coelacanth Diplurus newarki Schaeffer (1952). Small reptiles are also surprisingly abundant (Figure 30). Many important fish and unique reptile skeletons have been discovered here by dedicated amateurs, and donated to various museums through the years (Colbert, 1965, 1966; Schaeffer, 19S2; Schaeffer and Mangus, 1971; Colbert and Olsen, In Prep.; Olsen and Colbert, In Prep.).
At the south-facing exposures, cycles 1 and 2 are broken and injected by diabase of Granton Sill (Van Houten, 1969). Notice the absence of prominent folding at the diabase-sediment contact. The total thickness of the sill is 20m.
One or two bedding plane thrust faults, always thrusting to the east, are present in division 2 of nearly every cycle at Granton Quarry, Slickensides are usually present and indicate that movement occured parallel to dip. All joint sets are cut by these thrusts, their displacement indicates each fault has a net slip of .5 to 1.5 cm. This type of minor thrust fault is evident in virtually all Newark Supergroup lacustrine cycles and can be seen at every stop of this trip.

Lockatong hornfels and Palisade Sill
Cloverfleaf at this intersection rests on Lockatong hornfels and Palisade Sill (Fluur, 1941).

Open cut for Route 495 in Palisade Diabase.
Construction of cut exposed a number of easterly down-dropping dip slip faults which were described by Fluur (1941).

Reentrant in Palisade Escarpment
Reentrant in Palisade Escarpment at this point created by differential weathering along a series of dip slip faults, the cumulative dip slip amounting to about 70 - 80 m.

One of the larger faults
This street parallels one of the larger faults, in this case one responsible for the abrupt truncation of the western portions of Kings Bluff directly to the left (east) (Flurr, 1941).

Small fault striking nearly E-W.
According to Fluur (1941), construction along this road revealed a small fault striking nearly E-W.

STOP 2. Kings Bluff, Weehawken.
East face of Palisade ridge with exposures of long series of Lockatong cycles, tongues of Stockton-like beds, and alternating concordant-discordant contacts with the Palisade Sill. Park in lot on west side of road near the railroad tracks.
This is the first of three stops designed to show the lateral continuation of individual detrital cycles and the lateral change in sedimentary and metamorphic facies.
Lockatong and Stockton sediments and their contacts with the Palisade Sill are exposed at numerous places along the Palisade escarpment from Hoboken, New Jersey to Haverstraw, New York. Study of these exposures is permitting a cycle-by-cycle correlation of the Lockatong for at least 15 km of this distance, the cycles mapped so far are designated informally in Figures 31, 32, and 33. To the south at Hoboken the Palisade Sill rests near the base of cycles 5 and 6 (Figure 31). To the north towards the Lincoln Tunnel Toll Plaza, the contact drops more than 250 m into the Stockton Formation. At Kings Bluff, this contact abruptly rises again to cycle 0, staying within division 2 of this cycle for at least 300 m north. The olivine zone of the Palisade Sill produces an obvious bench along the escarpment, essentially paralleling the lower contact of the sill as observed by Walker, 1969 (Figure 31).,
Note the thin sill which branches off from the main sill intruding between cycles a and b. This sill definitely runs north for at least 400 m and was encountered during the excavations for the ventilation buildings for the Lincoln Tunnel (Figure 31) (Fluur, 1941). It may go at least another 200 m (Figure 36).

STOP 3. Gorge and River Roads
Gorge and River Roads exposures of cycles 1' - 6 and a and b. Turn right into empty lot outside entrance for Celotex Corporation.
Cycles 1 - 6 exposed along Gorge Road and cycles a-c on west side River Road opposite Mobil Service Station (Figure 37). These are the same cycles seen at Stop 2. Cycles 5 and 6 are virtually unchanged with the exception of an increase in ostracod density in the upper parts of division 2 of both cycles, fewer fish in division 2 of cycle 6, minor color changes, and the presence of calcareous nodules in division 2 of cycle 5. Cycles 1,3, and 4 appear unchanged from Stop 2, while cycle 1' is less disturbed and cycle 2 has more fish than at Stop 2.
In contrast with the relative lack of change from Stop 2 in cycles 1'-6, the siltstone units between cycle 6 and cycle a (Figures 32 and 33) are nearly completely replaced by 5.5 m of arkose with cross-bedding indicating transport to the west and southwest (Van Houten, 1969). I believe this arkose tongue and the thin siltstones present in this interval at Stop 2 to be the lateral equivalent of chemical cycles present in the central Newark Basin. Cycles a and b appear virtually the same as at Stop 2.
The detailed correspondence between beds and vertical changes in lithology and paleontology in cycles 5 and 6 (Figure 38) between Stops 2 and 3 is illustrative of the large area over which the factors responsible for the details of the cycles operated. The region represented by stops 2 and 1 was evidently far enough from shore (during the deposition of division 2) that the normal heterogeneous depositional environments of the shore had virtually no influence on cycles 5 and 6. This, in turn, is indirect evidence that the size of the lake which produced cycles 5 and 6 was considerably larger than the 15 km traced so far.
Note that Gorge Road follows fault-line ravine north of Lockatong exposures; eastern block is downthrown abou: 53 m (Van Houten, 1969).

Large xenoliths exposed on left (west)
Large xenoliths exposed on left (west) in excavation behind Virginia Lee Lace Co. (Van Houten, 1969).

Passing over eastern portal of tunnel
Passing over eastern portal of tunnel for former New York Susquehanna and Western Railroad. Directly under bridge for River Road is complete section of Lockatong cycles 1 '-6 and a. This same section is then repeated by a fault striking north. Cycle 2 is unusually fossiliferous, producing large numbers of well preserved Turseodus and fragmentary large Diplurus. At west portal of tunnel is a large open cut in upper Stodcton and lower Lockatong. Contact with sill dips 65° NW while Stockton and Lockatong dip 15° NW.
These exposures appear to be a repeat of the pattern seen at mileages 13.6 and 14.3 as shown in Figure 26.

Old quarry on left
Old quarry on left with excellent exposures of cycles 4 - f and underlying Stockton Formation. Small fault exposed at back of quarry which drops down the western block.

Series of outcrops along abandoned trolley route
Up hill on left on west side of Undercliff Avenue is long series of outcrops along abandoned trolley route (Van Houten, 1969). Exposures include upper Stockton Formation and lower Lockatong including cycles 5 and 6 and a, b, and c. The base of Palisade Sill is well exposed with large xenolith of cycle 5 suspended about 5 m above Lockatong-sill contact. Cycle 5 below contact contains scapolite-aegirine and Na-feldspar hornfels, while xenolith of same unit consists of very course grained biotite, Na-feldspar hornfels with minor pyroxenes, and beds of cordierite, biotite Na-feldspar hornfels (Van Houten, 1969).

Large phytosaur skeleton
A significant portion of a large phytosaur skeleton was found in upper Stockton beds near here in 1911. The skeleton, named Rutiodon manhattanensis by Friedrich von Huene (1913), is not generically determinate because it lacks a skull.
Reentrant in Palisade escarpment at this point is due to a few east dipping normal faults.

Olivine zone of Palisade Sill on left.
Diabase below olivine zone has distinct laminated appearance.

Contact of Palisade Sill with Lockatong Fm.
Irregular contact of Palisade Sill with Lockatong Formation -stratum uncertain (Figure 39).

Lockatong-sill contact
Additional exposures of Lockatong-sill contact on left - largely conformable. On the right, at the base of the hill, is a foot path along which are exposures of buff arkose and red and purple siltstone of the upper Stockton Formation. These are the most southerly exposures of a facies of the Stockton Formation visible along the Hudson from here to Haverstraw, New York (Olsen, Baird, Selden, and Salvia, In Prep.).

Circle in park road at base of shear face of Palisade Sill.

STOP 4. Ross Dock, Palisade Interstate Park
Lunch and extensive exposures of cycles 1' - 6 and a - c and irregular lower contact of Palisade Sill. Park in lot, have lunch, then take stone steps up hill (west) to road at level of circle (River Road of park) and walk north along road to exposures of Lockatong (Figure 40).
Proceed north along road, slowly walking down section (Figures 40 and 41). Cycle 1' and overlying 4 m of arkose with no sign of cycle 0 which presumably pinched out or was cut out south of here. Cycle 1 is present but poorly exposed. Cycle 2 is very well exposed and contains the same fossils as at mileage 24.8, although there are fewer whole Turseodus. Cycles 3 and 4 are evidently replaced by buff, crossbedded arkose. Cycles 5 and 6 very well exposed. Middle part of division 3 of cycle 6 contains distinctive nodular calcareous bed resembling caliche. Cycle 5 still shows the same basic sequence of beds and vertebrates as previous stops, but cycle 6 is noticeably coarser with fewer less well laminations and there are less fish. Upper division 1 of cycle 6 has produced a partial arthropod of uncertain relationships about 20 cm long.
The tongue of buff arkose between cycles 6 and a is thinner than at Stop 3 and coarsely crossbedded. Lower arkose cuts down into cycle a at this exposure, eliminating its division 2 (Figure 42). Mean paleocurrent vector for these crossbeds is N 59° W (based on 8 readings).
Cycle a is penetrated by numerous Scoyenia burrows (which were definitely not present at mileage 26.3) as are what appear to be cycles b and c. We are clearly in the shallow water facies of division 2 of cycles a - c at this point but only just leaving the deep water facies of division in cycles 2, 5, and 6.
Cycle a shows well developed fracture cleavage in division 1. Cleavage dips 25° to 30° and strikes S 78° W. Cleavage is strata-bound but discontinuous, passing laterally into breccia or non-cleaved beds. What is the significance of these structures?
The facies trend in the Lockatong from Stops 2, 3, and 4 is from a more central basin facies to a marginal facies. The monotony in horizontal continuity gives way laterally to heterogeneity (Figures 33 and 38). Those cycles with the best developed microlaminae and the best preserved fish at Stop 2 are also those which persist the longest with the least change.

Towaco Formation
Proceed on Route 46 west over broad flat expanse of Towaco Formation mantled by Pleistocene and Recent deposits.

Type section of Hook Mountain Basalt is on right
Type section of Hook Mountain Basalt is on right (north) in cuts for Hook Mountain Road and Route 80. Pass into Boonton Formation.

Buried portion of Hook Mountain Basalt
In this area we cross back over buried portion of Hook Mountain Basalt which links up Riker Hill and Hook Mountain (see Olsen, this Fieldbook).

Contact between Towaco Fm and Hook Mountain Basalt
Excellent exposures on left (east) of contact between Towaco Formation and Hook Mountain Basalt in Nob Hill Apartment complex (former east half of Roseland (Riker Hill Quarry). Two flows of Hook Mountain Basalt visible here (cumulative thickness 110m).

Follow along the back slope of Riker Hill.

STOP 5. Geology Museum, Walter Kidde Dinosaur Park
Geology Museum and Walter Kidde Dinosaur Park (former west side Roseland (Riker Hill) Quarry). Park in lot and look over exhibits at Geology Museum. Then take access path from Geology Museum over the crest of Riker Hill and down, through wooded area into Dinosaur Park. Always get permission before entering park.
As it stood in 1975, the Roseland Quarry occupied 55 acres, exposed 95 m of upper Towaco Formation - including two complete Towaco cycles, and exposed about 50 m of the overlying Hook Mountain Basalt (Figures 43 and 44). The quarry became very well known in the late 1960's and early 1970's for its prolific dinosaur footprints. Because of the scientific and educational potential of the site the then owners, Walter Kidde and Co. Inc., donated the most productive 15 acres to the Essex County Park Commission. The site now awaits development.
Before the other 40 acres were developed as the Nob Hill development, the following features could be seen:
1 , lateral changes in facies within divisions 1 - 3 of the lower cycle (Figure 45). The microlaminated beds of division 2 produced many fossil fish, all Semionotus (Figure 46) as did a number of the thinner (30 cm) turbidites.
2 , two upwards coarsening turbidite sequences, the lower being by far the larger (Figure 45). The lower sequence shows large scale slumped beds resembling "wild f1ysche" associations. Some of the "roll over" structures are 2 to 3 m in diameter. Transport was from the east.
3 , abundant dinosaur footprints in possible crevasse splay (in division 3) of channels about 70 m to north of tracks (Figure 47). Orientation of trackways proved to be parallel to paleocurrent directions derived from ripple marks within the footprint-bearing bed and oriented plant debris in overlying beds.
4 , Series of 7 fining-upwards cycles of division 4 of the lower Towaco cycle in the Quarry. Middle3 cycles had extensively developed dolomitic nodules and deeply mudcracked beds. Second fining-upwards cycle from the bottom with laminated silty beds (?flood basin) with abundant clay filled root casts, many of which are surrounded by dolomitic nodules (Figure 48).
In the presently exposed beds the following can be seen:
1, uppermost fining-upwards cycle of lower Towaco cycle still exposed along eastern boundary of park. The upper and middle parts of this cycle have the best reptile footprints in the quarry and hold the key to the park's development. Footprints are especially abundant in interbedded sequences of possible crevasse splay sandstone and flood basin siltstone. Basal sandstone portions of cycle are locally deeply down cut into underlying beds and contain beds of mud-chip conglomerate and casts of tree limbs and roots. Uppermost portions of the cycle consist of fine siltstone transitional into the lower parts of division 1 of the upper Towaco cycle. Transitional beds with numerous red siltstone roots surrounded by greenish halos.
2, exposure of complete Towaco cycle. Division 1 contains prominent fine sandstone beds with large calcareous concretions which weather out to form limonite filled cavities and extensive large (1-4 cm) coalified roots which probably belong to conifer trees. Crevasse splay beds in division 1 covered with little dinosaur footprints. Identical beds occur in division 2 of this cycle exposed in Chatham, New Jersey, 13 km south of here.
3, microlaminated portion of division 2 has very well developed white-black microlaminae (Figure 15) - but no fish have been found yet, however. Upper parts of microlaminated beds contain distinctive nodules of black chert. Black, coally-looking siltstone surrounding chert bed has several bedding thrusts similar to those seen in the Lockatong at Stops 1 - 4. Microlamillated beds locally involved in disharmonic folds (Figure 15). Like the beds of division 1, these portions of division 2 look exactly the same in the Chatham exposures.
4, casts of a salt present in coarse siltstone beds above microlaminated portion of division 2.
5, massive fine gray siltstone in upper parts of division 2 have well-preserved conifer foliage, pollen and spores, individual fish scales (Semionotus), and rare insect fragments.
6, complex series of sandstones and siltstones of division 3 showing features suggestive of both laterally migrating channels and prograding deltas.
7, lowest fining-upwards cycle in division 4 (Figure 49) shows slip-off faces of point bar and beds of intraformational conglomerate with coprolites, fish scales, reptile bone fragments, and abundant dinosaur footprints. The latter features could represent a dinosaur "wallow".
8, 10 successive fining-upwards cycles of division 4. Rill marks very well developed in bank portions of one of the middle cycles (Figure 50) These sorts of rill marks, typical of channels with rapidly dropping water levels, have long been confused with plant remains (it is easy to see why) and have received the name Dendrophycus (Newberry, 1888).
9, unique small reptile footprints with structure highly suggestive of advanced mammal-like reptiles or mammals (Figure 20) are present in upper fining-upwards cycles. If they do represent mammals,they will be the oldest North American record.
10, very badly weathered "tuff" between normal Towaco Formation and Hook Mountain Basalt. This unit is enigmatic but very widespread at this stratigraphic position. Fresh exposures were described by Lewis in 1908 (see Olsen; this Fieldbook).

Preakness Mountain Basalt
Head east on 280 up dip slope of Preakness Mountain Basalt. Outcrop width of Preakness Basalt is very large in this area, suggesting a thickness of 500 m for the basalt. I believe this is due to a number of small strike faults and the true thickness is closer to 300 m. These faults in combination with the multiple flow character of the Preakness Basalt produced the many small ridges visible while driving up the dip slope.

Type section of the Preakness Basalt
Type section of the Preakness Basalt in deep open cut for Route 280. Section exposes about 100 m of the lower flow. Note distinctive "splintery" nature of the lower 50 m (see Olsen, this Fieldbook). This section is cut by a series of faults all apparently left lateral and all showing little or no apparent dip slip offset (Figure 51).

Preakness Basalt / Feltville Fm contact
Contact between Preakness Basalt and Feltville Formation poorly exposed on south side of road.

Unexposed contact
Unexposed contact between Feltville Formation and underlying Orange Mountain Basalt below this point.

Exposures of ?second flow of Orange Mountain Basalt.

Type section of Orange Mountain Basalt
Type section of Orange Mountain Basalt in very long and deep open cut for Route 280 (see Olsen, this Fieldbook; Manspeizer, this Fieldbook). Section exposes about 55 m of lower flow as well as a number of left lateral faults similar to those seen at mileage 64.8. Left lateral faults are present here as they are at mileage 64.8. At one portion of the cut, on the north side is 20 m long horizontally slickensided fault plane. Note the very different appearance of basalt (in terms of jointing) from the Preakness Basalt.

Contact Orange Mountain Basalt / Passaic Fm
Contact of Orange Mountain Basalt and Passaic Formation was well exposed during construction of this cut, at this point.

Triassic-Jurassic boundary
Cuts in uppermost Passaic Formation here have produced phytosaur footprints called Apatopus and the possible crocodillo-morph tracks called Batrachopus. The Triassic-Jurassic boundary lies somewhere within the upper few tens of meters of the Passaic Formation here.

Passaic Formation formerly exposed here
Sedimentary cycle in Passaic Formation formerly exposed here. A very well preserved palynomorph assemblage recovered from fine gray siltstones of this unit suggest a lower Rhaetic age (Comet, 1977). This unit has also produced a series of reptile footprints including large and small Grallator and Chirotherium sp. Scoyenia is abundant as is the conchostracan Cyzicus. Equivalent beds are exposed at the same stratigraphic position in New Brunswick, New Jersey. The entire Passaic Formation section from this unit to the Orange Mountain Basalt is above the entire Delaware River section of the Passaic Formation, which extends upwards only into Norian beds (Cornet, 1977).

53RD ANNUAL MEETING 18-20 SEPTEMBER 1981
BINGHAMTON, NEW YORK
GUIDEBOOK FOR FIELD TRIPS IN SOUTH-CENTRAL
NEW YORK
Paul Enos, Editor
State University Of New York At Binghamton
Published by the New York State Geological Association. Guidebook available from the executive secretary: Manfred P. Wolff, Department of Geology, Hofstra University, Hempstead, New York, 11550.

A1: THE WEST FALLS GROUP (UPPER DEVONIAN) CATSKILL DELTA COMPLEX: STRATIGRAPHY, ENVIRONMENTS, AND SEDIMENTATION
James R. Ehrets
University of Rochester
Rochester, New York
Since the last meeting of the NYSGA in Binghamton (Coates, 1963), significant advances have been made in the refinement of correlation and environmental interpretation of Upper Devonian strata in south-central New York. One purpose of this article is to summarize the updated stratigraphy in this region and to review how the stratigraphy has been developed. The main theme of the article is the result of recent study in the Binghamton area (Fig. 1). By tracing thin units of dark-gray shale to the east of Binghamton, a stratigraphic framework was developed which permitted further analysis of environmental and sedimentologic relationships of the Catskill delta complex in the area. Through the demonstration of the dark-shale framework and discussion of deltaic environments, a few of the interpretations are presented. The accompanying field trip is designed to illustrate a variety of deltaic environments and how they fit into the stratigraphic framework.

A1: THE WEST FALLS GROUP (UPPER DEVONIAN) CATSKILL DELTA COMPLEX: STRATIGRAPHY, ENVIRONMENTS, AND SEDIMENTATION

STOP 1. Distal Platform.
(Field locality 4) The relatively thin beds of fine-grained sandstone interbedded with gray shale are characteristic of middle- and distal-platform environments. Sandstone beds of approximately one foot in thickness have basal coquinites 1-2 inches thick; thicker sandstone beds have basal coquinites up to one foot thick. The coquinites are typically composed of disarticulated and articulated brachiopod shells with significant numbers of crinoid columnals. Some sandstone beds are graded coarse-to-fine. The shales are generally not very fossiliferous, but localized areas of bedding planes can produce quite a few well-preserved brachiopods and molluscs. A zone of large pillow structures is distinctly visible near the top of the exposure. The zone is laterally persistant for the length of the exposure. These pillows (denoted as type I) are composed of fine-grained sandstone; the distorted matrix of shale in which they are situated suggests that these structures formed as a result of vertical foundering. Smaller, solitary pillows are present at the base of the exposure near the parking area. These are denoted as type II pillows and are probably formed in a similar manner as type I pillows.
This portion of the platform was well-removed from the effects of rivers and streams. Sand which reached this area was supplied in the form of "sheets" from distributaries, which had merged with each other closer to the shoreline. Grading in the sandstones as well as the presence of basal coquinites indicates a "proximal turbidite" origin.

STOP 2. Dark Mud And Proximal Platform Environments.
(Field locality 7) The dark-gray and rust-brown mudstones and shales of the Roricks Glen Member are exposed in the basal portion of this exposure. Outcrops of the Roricks Glen on the delta platform are all about 20 feet thick and are composed predominately of mudstone with smaller amounts of shale. Thin-bedded lenses of fine-grained sandstone and siltstone are present in the dark-shale member; fossils are few in number. Flagstones and sandstone lenses near the top of the exposure indicate a return to normal deltaic conditions. The large block of cross-bedded sandstone at the very top of the bank (although slightly dislodged) is of channel origin in what is inferred to be the subaqueous delta plain. Cross-bedded sandstone is present in the form of scattered blocks on the hillside above the roadside exposure. The Roricks Glen will be seen again in a similar environmental association later in the field trip.

View of Susquehanna River Valley.

STOP 3. Subaqueous Delta Plain
(Field locality 18). The flagstone deposits in the quarry are typical of the subaqueous delta-plain environment. The large-scale crossbedding in the south wall of the quarry is evidence that this portion of the delta plain is gradational with a.distributary-mouth bar within the delta platform. This interpretation is supported by a nearby shale pit which exposes normal delta-platform deposits. Current and wave ripples, low-angle crossbedding and parting lineations are common sedimentary structures at this locality. Orientations of the structures indicates a southwesterly average current direction. With the exception of oriented plant fragments on a few bedding planes, fossils are rare.

STOP 4. Proximal Platform
(Field locality 42). The numerous lenses of sandstone exposed here are subaqueous extensions of distributaries which flowed westward from the subaqueous delta plain. Near the base of the exposure on this road is a zone of organic-rich sandstone that is interpreted to be the result of a rapid regressive (storm) event which interrupted normal progradation of the deltaic environments. A thin stringer of quartz-pebble conglomerate is associated with this sand deposit. This conglomeritic horizon has been found to exist elsewhere in the study area to the west. In addition to a variety of ripple marks which can be observed on the terraces in the upper portion of the outcrop, a lens of large pillow structures and a variety of crossbedding are among the more obvious sedimentary structures.

STOP 5. Proximal Platform And Subaqueous Delta Plain
(Field locality 49). The interbedded flagstones, cross-bedded sandstones, and shales in this exposure illustrate the variety of lithologies which coexist at the margin of the subaqueous delta plain. The beds and lenses of sandstone are small distributary-mouth bars formed as a result of the reworking of sand at the fronts of streams. The relatively dark shale was deposited behind the bars in restricted waters of small bays. Cross-bedded, organic-rich sandstone lenses are the remains of distributaries which migrated laterally in this region. The bar deposits gradually give way to subaqueous delta-plain channel deposits which are composed of more poorly sorted, cross-bedded sandstone. Higher up in the exposure is a 10-foot thick bed of dark shale and mudstone which is correlative with the Roricks Glen Member. This fine-grained deposit grades upwards into drab-colored overbank deposits of the subaerial delta plain.

STOP 6. Subaqueous And Subaerial Delta Plain
(Field locality 46). The extensive exposure in this quarry (formally called the Ostrander quarry) displays a variety of flagstone and cross-bedded sandstone of stream origin within the delta plain. Ripple marks and scour marks are very common on the surface of terraces in the quarry. Burrowed and mud-cracked mudstone forms the floor on the second terrace (west face of mountain). These and similar deposits in the quarry are of floodplain origin. Red-orange, conglomeritic debris scattered around the area are levee deposits which can be seen in place as lenses associated with channel sandstone in the quarry walls. A thin red bed is visible about two thirds up the sheer face on the western wall. Just above the red bed (one of only a few in the study area) is a dark-shale bed that is correlative with the Roricks Glen Member. A thin coquinite at the base of the overlying sandstone bed contains shell material left as a lag deposit resulting from winnowing of the very top of the Roricks Glen.

STOP 7. Distal Platform
(Field locality 35). The conspicuous zone of extremely large pillow structures in the lower section of the quarry is a feature which is cnaracteristic of the distal platform environment. These pillows are referred to as type III and are interpreted to have formed due to repeated foundering of relatively coarse platform sediments which were continually supplied to submarine topographic lows by the reworking effects of waves and currents at the edge of the platform. The mudstone and siltstone matrix of the pillows contains a random distribution of small fossil material consisting mostly of crinoid columnals. The matrix as a whole displays a weak cross lamination in places. The number of lenses and thin beds of sandstones increases upsection indicating the westward progradation of the shoreward environments. Basal coquinites are common in these sandstones. (The top of this section, which is exposed along Farm-to-Market Road at the top of the hill, contains a horizon of dark shale within the Dunn Hill Member).

STOP 8. Distal Platform And Dark Mud Environments
(Field Locality 11). Once again, the presence of extremely large (type III) pillow structures indicates the distal platform environment. Here, the pillows are resting upon and within the Dunn Hill Member. The pillows are compositionally similar to those at STOP 7. Currents on the delta platform were active during the deposition of the Dunn Hill as evidenced by these relatively "coarse-grained" structures as well as lenses of sandstone which display crossbedding. Although not shown here, deposits of fossiliferous, cross-bedded "delta-front sands" can also be fairly well developed only a few feet above a given dark-shale member. Thus, a normal deltaic environments rapidly redeveloped after transgression.

A2: THE MIDDLE AND UPPER DEVONIAN CLASTIC WEDGE IN NORTHEASTERN PENNSYLVANIA
W. D. Sevon
Pennsylvania Geological Survey
Harrisburg, Pennsylvania 17120
Throughout most of the Paleozoic, much of what presently constitutes the eastern half of North America was part of an inland sea which intermittently received clastic sediment from an eastern source area. The Appalachian basin was the central focus of this sedimentation.
The largest integrated wedge of clastic sediment in this basin was deposited by the Catskill delta system during the Middle and Late Devonian. The purpose of this paper is to present an overview of Late Devonian sedimentation, with particular reference to Pennsylvania. The purpose of the field trip is to examine some of the rocks from which interpretations about the Catskill delta system are made. The information presented here derives from the literature as well as my own work. The term "delta system" as used here refers to multiple contiguous deltas operating in the same sedimentary basin at approximately the same time. The Catskill delta system is also a tectonic delta complex in the sense defined by Friedman and Johnson (1966, p. 185-186) for New York State and used by Humphreys and Friedman (1975, p. 369-370) in Pennsylvania: "a deltaic complex built into a marine basin contiguous to an active mountain front and dominated by orogenic sandstone derived from the nearby tectonic highland."

A2: THE MIDDLE AND UPPER DEVONIAN CLASTIC WEDGE IN NORTHEASTERN PENNSYLVANIA

STOP 1. Prodelta Environment
Rocks at this stop are exposed in an outcrop along the west side of the road and along the west side of the stream below road level. Stream elevation is 970 feet.
The rocks exposed here comprise dark-gray shales and siltstones of the Lock Haven Formation. The siltstones have sharp bases, overlie shales, and fine upwards into shale. Burrow traces and fossils of marine invertebrates occur. Lateral continuity of beds is good within the extent of the small outcrop.
This is a good problem outcrop. If examined as an isolated entity, how much information can be gained from the outcrop itself? How much does it help to know the relative position of the outcrop in the vertical sequence of Figure 7? How important is context in the study of (1) rock lithology, (2) depositional environment, (3) stratigraphy, and (4) geologic history?

STOP 2. Marginal-Marine Environment
The flagstone quarry at this site was opened into rocks of the lower part of the Catskill Formation. The flagstone derives from the planar-bedded sandstones exposed in the floor of the quarry at elevation 1660 feet. The sequence of lithologies exposed here (Fig. 9) is interpreted to represent deposition in an offshore bar environment and the following information about the stop is from Krajewski and Williams (1971b, p. 13-15) .
"Characteristics of this type of quarry include:
a) a convex upper surface;
b) parallelism of the parting lineation orientation and the down-dip direction of the cross-bedding;
c) a steep front in the seaward direction;
d) replacement seaward (northwestward) by darker, fossiliferous, marine shales;
e) replacement landward (southeastward) by siltstones, smallscale rippled sandstones, and red shales; and,
f) uniformness and regularity of the joint systems (the high walls of the quarry parallel the joint systems).
"Two offshore bars are visible in the diagram, the larger lower one, and another smaller one in the south end of the quarry. The long direction, or paleogeographic trend, of these bars would be perpendicular to the parting lineation shown in the diagram, or northeast-southwest and east-west for respectively the lower and upper bars. The rock sequence represents a marine transgression onto the tidal flats and shore zone."
Examine this stop with the following questions in mind: (1) How easily can the depositional environment be determined from the physical properties of the rocks? (2) Does the interpretation of this outcrop aid in the interpretation of the rocks at Stop 1? (3) What information can be gained about the source area from this stop?

STOP 3. Fluvial Environment
Pull off and park on wide berm at south end of road cut and examine the rocks along the terrace above the road.
The rocks at this stop are exposed in the southernmost of three large roadcuts on the west side of Interstate Route 81, all of which expose similar rocks. Elevation here is 1640 feet.
Exposed here are a variety of sandstones, both gray and red, which contain lag gravels, cross beds, planar beds, and ripples (Fig. 10). Interbedded red siltstones are locally burrowed. Lag gravels comprise predominantly calcium-carbonate nodules. Cross-bed forsets are oriented mainly to the southwest while parting lineations are to the northwest. Lateral and vertical relatonships are complex, but the whole can be interpreted in terms of a fining-upward cycle formed by a meandering stream (Allen, 1970).
What features of this outcrop are critical to the interpretation of its depositional environment? How many levels of context are involved in studying this outcrop? What information about the source area can be gained from this outcrop?

STOP 4. Nay Aug Park - Lunch
This stop is principally for the purpose of ingesting food, but some interesting things can be seen.
The Brooks Model Coal Mine area has the entrance to an underground anthracite mine and some old coal cars. The sandstones exposed throughout the park are part of Llewellyn Formation of Pennsylvanian age. This formation contains a number of anthracite coal seams which have been mined, principally by underground methods, in the Wyoming-Lackawanna basin (the northern anthracite field). Exposures along the railroad track along the east side of the park allow evaluation of the depositional environment of the rocks exposed here.

Basal Pottsville Formation conglomerate.
Outcrops on both sides of road of basal Pottsville Formation conglomerate. Outcrop to left is upper part of Stop 7.

To right across Roaring Branch is dip slope
Outcrop to left is Spechty Kopf Formation and site of start of Stop 7. To right across Roaring Branch is dip slope underlain by Spechty Kopf Formation sandstones. Shale exposed below sandstone.

STOP 5. Fluvial Environment
The rocks at this stop are exposed in cuts on both sides of Interstate Route 84 east at the point where entrance ramps from Interstate Route 380 east and west join. Park on wide berm on the south side of the road and examine the rocks in the cut on the north side of the road. Cross the interstate with care!
The rocks exposed here are near the uppermost part of the Poplar Gap-Packerton Member of the Catskill Formation (Fig. 8). The sequence (Fig. 11) comprises mainly gray sandstones with some red mudstones. Sandstone and siltstone contacts are sharp. The gray sandstones are cross bedded, contain some lag gravels, and are locally calcareous (calcareous cement weathers brown). Scattered red-shale clasts are common near the bases of some sandstone bed sets. The lag gravels contain some quartz pebbles, but mainly calcium-carbonate nodules, many of which look like oncolites. Root traces occur locally in the sandstones.
The lower red mudstone is burrowed in part and contains abundant calcium-carbonate nodules. Note the thinly laminated character of some of the mudstone enclosing the nodules.
There are many questions to be asked about these rocks. Would information on context be useful in making an environmental interpretation? What information can be gained about the source area? Is source-area information at this outcrop more or less abundant than at Stop 3? What is the significance of the presence of calcium carbonate? How were the calcium carbonate nodules formed in the red mudstones and in the gray sandstones? What is the evidence for a fluvial origin for this sequence? What specific fluvial environment best fits these rocks?

STOP 6. Fluvial Environment
The rocks exposed here are near the lowermost part of the Duncannon Member of the Catskill Formation (Fig. 8). The rocks comprise one complete and two partial fining-upward cycles (Fig. 12). Two cycles have a sharp base with gray sandstone overlying red mudstone. Above the base there is an upward decrease in grain size from sand to clay and change to red color.
The lower sandstone has some calcium-carbonate cement, a few root traces, and bedding changes upward from crossbedding to planar bedding. The overlying red mudstones contain repeated zones with abundant burrows and root traces. The mudstone between these zones is generally thinly laminated. The upper third of the lower major cycle is a smaller cycle which has a grayish red sandstone above a sharp base. Calcium-carbonate nodules are abundant in the mudstone below the sharp base of the upper major cycle. Several large channel cuts occur in the gray sandstone of the upper cycle.
What is the probable origin of the excellent fining-upward cycles displayed in this exposure? How do these cycles compare with that at Stop 3? What is the significance of the alternating burrowed and nonburrowed zones in the mudstone? How do the calcium-carbonate nodules in the red sandstone compare with those at Stop 5? What differences in depositional environment are suggested by the differences in the rocks exposed here and at Stop 5? Is context of particular value in interpretation of the depositional environment of these rocks? What information about the source area do these rocks provide?

STOP 7. Spechty Kopf Formation And Local Subsidence
Park well off road on berm to right before guard rail starts and just after junction of entrance ramp to Interstate Route 380 west. Bus will proceed 0.8 farther to end of upper outcrop for pickup.
This stop occurs at roadcuts on the east side of Interstate Route 380 just south of Dunmore and consists of two parts: a long, high roadcut just north of the entrance ramp (lower outcrop) and a long, low roadcut about 0.7 miles farther north (upper outcrop). The exposures are separated by a covered interval.
The identification of the rocks at this stop is different from that indicated on the 1960 edition of the geologic map of Pennsylvania (Gray and others, 1960), but is in agreement with the 1980 edition of that map (Berg and others, 1980). The changes result from the work of Sevon (1969) and subsequent reconnaissance mapping. The Pocono Formation occurs in the covered interval between the lower and upper exposures.
The lower outcrop (Fig. 13) consists of dark shales and sandstones of the Mississippian-Devonian Spechty Kopf Formation. The shales are here about 300 feet thick and are underlain (in exposures along Roaring Branch) by polymictic diamictite. Interbedded thin siltstone layers exposed in the lower third of the shale in the former Nay Aug quarry across Roaring Branch have bottom-surface flow structures and upper-surface ripples which indicate current flow of N12E. Very large and relatively small slump structures occur in the upper third of the shale and are very well exposed here. The contact of the shale and sandstone is gradational through a zone of interbedding. A zone of load casts occurs just below the first sandstone interbed.
The sandstone comprises relatively uniform and moderately well-sorted grain size throughout, is very light gray in color, weathers tan, and is about 160 feet thick. Bedding in the lower part defines wedge-to-irregularly lens-shaped bed sets which dip northwestward at a steeper inclination than the overlying planar beds. The planar bedding is remarkably uniform and persistent. Some beds have ripples, but most are apparently structureless.
What are the environments of deposition of the rocks exposed in this outcrop? The rocks underneath the basal polymictic diamictite are those of the Duncannon Member seen at Stop 6. Does this aid or complicate the interpretation? Also of importance is the fact that 5 miles to the north on the other side of the basin, this sequence is compressed to 110 feet in thickness and is totally absent along all margins of the basin within 20 miles of this locality. The unusual thickness of this sequence and its lateral variation is interpreted to indicate local subsidence at the time of deposition. The regional aspects of these facies (Sevon, 1969; 1979b) are interpreted as part of the demise of the Catskill delta (see earlier text).
The upper outcrop (Fig. 14) is capped by a white conglomerate of the Pottsville Formation of Pennsylvanian age. The conglomerate is underlain by a sequence of siltstone, sandstones, and limestones which are unlike any other rocks at similar stratigraphic positions anywhere in eastern or central Pennsylvania. The sequence is correlated with the Mississippian Mauch Chunk Formation on the basis of stratigraphic position, but the rocks are very dissimilar from the red siltstones and sandstones which characterize the Mauch Chunk as near as 20 miles to the southwest. However, known facies changes along the southeastern margin of the Wyoming-Lackawanna basin and the abundance of calcium carbonate suggests that such correlation is valid. What environments of deposition may be represented by these lithologies--particularly the thin limestone? Do these rocks, including the Pottsville conglomerate, tell much about the source area?

A3: MIDDLE AND UPPER DEVONIAN SHALES AND ADJACENT FACIES OF SOUTH-CENTRAL NEW YORK
Brent K. Dugolinsky
State University College - Oneonta
GENERALIZED STRATIGRAPHY OF MIDDLE AND UPPER DEVONIAN SEDIMENTS OF NEW YORK
The Devonian section in New York is the standard reference section for eastern North America. Early workers recognized that major facies changes occur in the Middle and Upper Devonian sequence as a result of deposition of the Catskill delta. Consequently, older units originally mapped as formations or groups in a particular area were recognized as portions of major facies (Catskill, Chemung, Portage) cutting across time lines. Later workers concentrated on finding thin, widespread key beds within the thick deltaic sequence that are unaffected by rapid facies changes characteristic of rocks above and below. These key beds, which are believed to represent time planes, divide the deltaic sediments into several time-stratigraphic units.
The main purpose of this field trip is to observe the field relationships and subtle lithologic changes within and between the shales and adjacent facies in the "Catskill Delta" sequence and to interpret these characteristics in terms of the depositional environment. By the end of the trip, you should have a better understanding of why detailed mapping and identification of facies relationships remains complex and problematical in spite of exhaustive study by numerous workers for over a century.

A3: MIDDLE AND UPPER DEVONIAN SHALES AND ADJACENT FACIES OF SOUTH-CENTRAL NY

STOP 1. East Beecher Hill Roadcut, Owego, N. Y.
(Description partially from Woodrow and Nugent, 1963, and Patchen and Dugolinsky, 1979).
Exposures of Beers Hill and Roricks Glen Members of the Rhinestreet Formation. Elevation at bottom of exposure is 950'.
The Rhinestreet Shale defines the base of the West Falls Group from Lake Erie eastward to Seneca Lake. East of Seneca Lake workers at the University of Rochester under the direction of Robert Sutton have traced fingers of dark-gray shale that define the eastern Rhinestreet equivalent. In the area from Elmira to Binghamton, four dark shales and three intervening lighter colored shales and siltstones (including the Beers Hill Member exposed here) are defined as members of the Rhinestreet Formation (Sutton, 1963; Woodrow and Nugent, 1963).
The Roricks Glen is represented by scattered, very dark-gray shales at the upper end of the exposure. However, many of the darker shale layers have been covered and are difficult to locate. Also, the land above the troadcut is posted and it is therefore recommended that you limit your observations to the exposure along the road. Most of the exposure is in the Beers Hill Member, with flow rolls well developed in the section near the bottom of the hill, just above a landslide scar. Fossils are scarce, but worm burrows and trails (Fucoides graphica) are often found, particularly on the base of the thick, resistant coarser-grained beds. Flute casts, cross bedding and other current indicators are also found.

STOP 2. Richford, N. Y.
The base of the Middlesex Shale Member of the Sonyea Group may be seen exposed in the stream bed across the road from the parking area. The basal few feet of stream exposure is West River Shale, followed by brownish-black shale and siltstone of the Middlesex. Only a few feet are clearly exposed at this location.
Well-developed groove casts and burrows may be found on the base of silty beds. Most of a steep roadcut on the same side of the road as the parking area is covered, but a little digging will expose the Middlesex.
The Middlesex Shale gets progressively finer grained and darker farther west, towards the type section. This facies relationship is generally true for all Upper Devonian shale units.

STOP 3. Finger Lakes Stone Co. Quarry,
(Descriptions from Chute, 1970 and Dugolinsky, 1972)
The entire quarry exposure is within the Rock Stream Formation (previously named the Enfield Formation) of the Sonyea Group. Layers of sandstone alternate with layers of shale and siltstone. The Rock Stream has been interpreted as representing a shelf deposit (300-500 depth), although much shallower depths are likely. Its westward equivalent, the Cashaqua Shale, represents a slope and basin environments in deeper water.
Many of the silty and sandy beds pinch out rapidly. Fossils and sedimentary structures are very common and well developed. Sole marks may be best seen on the base of silty layers. Worm burrows are common. Excellent sole marks, including flute and groove casts, are usually most accessible on quarried slabs.
The quarry is presently operated by the Finger Lakes Stone Company. Slabs of sandstone are obtained without blasting by drilling holes on seams and separating them with wedges. The slabs are cut to the desired sizes in the mill by diamond and wire saws. Pieces with good joint surfaces are used for special surface effects. The stone is laid in various patterns with different finishes, as illustrated by the exterior of the company's office at the quarry.

STOP 4A. Railroad Cu
Railroad Cut Between Salt Company And Abandoned Cement Plant, North Of Ithaca
Exposure of the King Ferry Shale of the Ludlowville Formation.
About 25 feet of the King Ferry Shale is exposed here, with a noticeable dip to the south. Many concretions may be seen in the siltstone beds, which are lighter colored than the shales. The darker shales are commonly cross-laminated. A coquina (fossil-rich layer) is evident at the base and top of the siltstone unit.
Much of the unusual weathering characteristics of this exposure is thought to be due to salt contamination from passing railroad cars coming from the salt plant just to the north of the exposure.

STOP 4B. Gulf Stream (Shurger Glen)
Exposured are the upper King Ferry Shale, the Portland Point Limestone, Moscow Shale and Tully Limestone.
The upper King Ferry Shale of the Ludlowville Formation may be seen in the exposures in and below the lower falls in Gulf Stream. The overlying Portland Point Limestone, near the lip of the lower falls, is very fossiliferous. Note the peculiar curved fracture pattern in the shales just below the falls.
The lower falls may be scaled on the left side (facing upstream) with care, where the approximately 5 feet of Portland Point Limestone may be examined. The Portland Point is coarsely crystalline and weathers brown. Slickenslides may be observed in the lower 8 inches of the member.
Float at the base of the lower falls includes samples of Tully Limestone, which is finer-grained and less fossiliferous than the Portland Point limestone.
The Moscow shales overlie the Portland Point and are roughly 100 feet thick in this area. They are well exposed upstream from the lower falls. A nearly complete exposure of the entire 100 feet may be seen about 5 minutes upstream. The overlying Tully Limestone is visible at the top of the cliff exposure and forms the lip of the upper falls which is about another 20-minute walk farther upstream. Dark shales (Geneseo) may be seen in the float below the upper falls and are probably exposed above the upper falls. There is excellent joint control in the stream at and immediately below the upper falls.
The gray silty shale and siltstones of the Ludlowville and Moscow demonstrate a high diversity fauna and represents sediments deposited in a subtidal shelf-delta platform (Grasso, 1978).

STOP 5. Buttermilk Falls State Park
A recent study (deWitt and Colton, 1978) has revealed that 14 feet of Renwick Shale are exposed at the base of the lower falls, overlain by 478 feet of Ithaca shales and sandstones, which in turn are overlain by 135 feet of West River Shale. The Renwick Shale is easily accessible here, particularly for large groups. Note the darker color of the shale with the interbedded lenticular silty beds exposed. The precise contact of the Renwick with the overlying Ithaca is not easy to pick out.
The Renwick here separates coarser-grained clastics: the underlying Sherburne and the overlying Ithaca Formation. Westward, the Renwick merges with the Penn Yan Shale, which is the lower of two shales in the finer western facies. A travertine deposit may be seen on the vertical exposures at the left of the main swimming pool (looking upstream). It is assumed that these deposits are very recent (post-glacial) and result from the deposition of materials in groundwater.

STOP 6. Taughannock Falls State Park
Park on left (before bridge) in Taughannock Falls State Park. Walk into gorge, using trail on the left bank.
(Descriptions from Cornell University Department of Geology, 1959, and from deWitt and Colton, 1978).
Note: At 215 feet, Taughannock Falls is the highest falls in North America east of the Mississippi River.
The main falls is at the head of a deep post-glacial gorge one mile long, with walls from 200 to nearly 400 feet high. The falls is determined partly by the superior resistance of the Sherburne sandstones and partly by the jointing pattern within the rock units. The upper 90 feet of the Geneseo Shale is exposed in the gorge walls from the level of the plunge pool to a point marked by a change in lithology and color. Much of the Geneseo is covered with talus in places. The entire Penn Yan (about 80 feet thick at this locality), the overlying Sherburne (also about 80 feet thick) and the Renwick Shale (about 35 feet thick) are exposed here, along with the lower portion of the Ithaca. At the mouth of the gorge, near the lake, is the lower falls (about 15 feet high), over the resistant Tully Limestone, (also about 15 feet thick here), between the weak basal Geneseo shales above and the shales of the Moscow Formation below.
Both the Sherburne and the Renwick facies are lost only about 15 miles west of this location, where they merge into the Penn Yan Shale.
Note particularly the interfingering nature of the contact between the Tully and the overlying Geneseo, easily seen in the stream bed above the lower falls. This indicates that although there may be an unconformity at the top of the Tully Limestone farther west, there is none here.
Joint control is well developed, particularly within the Geneseo Shale, and is best seen in the cliffs below the main falls and in the stream bed just below the main falls. Alnoite dikes, each less than one inch thick, are present in the stream bed beneath the main falls.
We are now on the northern flank of the Fir Tree Anticline and a slight northern dip may be seen easily if you look at the water flowing over the Tully Limestone, following a bedding plane, just above the lower falls where the stream bed is wide. En echelon fractures are well developed in the Tully Limestone exposed in the stream bed.
This gorge was used in pre-World War II days for sets in "western" movies and some of the wooden shacks precariously perched on the face of some of the cliffs were used to house the cameras during filming.

STOP 7. Fayette Town Dump
(Description partly taken from Cornell University Department of Geology, 1959).
This quarry was originally operated by the Town of Fayette for road material and is now used as a dump. The upper 40 feet of the Levanna Shale and lower 20 feet of the Centerfield Limestone are exposed here. The Levanna is the upper member of the Skaneateles Formation whereas the overlying Centerfield Limestone is the basal unit of the Ludlowville Formation of the Hamilton Group.
We have observed the upper of two general facies within the Hamilton Group at Stops 4-A and 4-B: The Ludlowville and Moscow Formations. Here, we can see a different gross facies represented by the dark, fissile Levanna Shale Member of the Skaneateles Formation, which represents an anerobic, distal basin (Grasso, 1978). The overlying Centerfield Limestone separates this facies from the lighter colored, silty Ludlowville.
This is a good fossil-collecting site, particularly near the base of the Centerfield Limestone. Most common fossils are brachiopods, pelecypods, gastropods, plant fragment and fish remains. Mineral-filled fractures are common and asphaltic-filled fractures are occasionally found. Pyrite is commonly seen, particularly in the dark Levanna Shale. Large septarian concretions are seen in several layers within the Levanna Shale.

A4: SUBMARINE DISCONTINUITIES, ETC., IN THE UPPER HAMILTON GROUP
Gordon C. Baird
Field Museum of Natural History
Chicago, Illinois 60605
Carlton E. Brett
University of Rochester
Rochester, New York 14627
As defined by Jenkyns (1971) condensed sedimentary sequences are differentially thin deposits recording minimum rates of net sediment accumulation. Such sequences are shown through correlation to be greatly condensed equivalents of thicker deposits; these latter typically display convergence of coeval zones or beds along their lateral periphery. It is possible for stratigraphic sequences to thin from hundreds or even thousands of feet to tens of feet or less while preserving or partly preserving the internal sequence of fossil zones or lithologic subunits. Stable depositional settings such as oceanic-rises and seamounts, regions of the open ocean floor, and broad epeiric shelf areas are commonly characterized by condensed sedimentary sequences. Selective winnowing of fines by currents and bioturbation effects, periods of nondeposition, inorganic degradation and biocorrosion of carbonates, exhumation and reburial of concretions and fossils, and juxtaposition or commingling of fossil zones are all variably characteristic of such condensed sedimentary sequences. Association of these sequences with local and regional discontinuities is also common as will be shown for part of the New York Middle Devonian section in this paper.
The upper Hamilton Group (Ludlowville and Moscow Formations) of the Cayuga Valley includes a thick sequence of marine mudstone characterized by widely spaced, thin limestone units and numerous mappable fossil zones. Several of these are associated with a widespread paraconformity and condensed sedimentary sequence at the base of the Moscow Formation; the differentially thin strata include the Portland Point and Kashong Members which are most compressed stratigraphically in the southeast part of the Cayuga Valley. These units thicken northwestward across the Cayuga and Seneca Valleys, 9.5 feet of strata (Portland Point and Kashong Members) at the Portland Point type section expanding to 100-110 feet in the Canandaigua Valley. The Tichenor-Portland Point Members disconformably overlie the King Ferry Shale in the Cayuga Valley, although evidence of erosion is lacking in most outcrops.

A4: SUBMARINE DISCONTINUITIES, ETC., IN THE UPPER HAMILTON

Cross mouth of Taughannock Creek
Cross mouth of Taughannock Creek at Taughannock State Park. To the left (upstream) from the road bridge a low waterfall is visible; this section includes the Tully Formation (limestone) overlying the uppermost Hamilton Group (Windom Member). Farther upstream is a splendid gorge-waterfall section exposing sediments of the lower Genesee Group (Upper Devonian: Frasnian Stage).

Cross Sheldrake Creek.

Cross Barnum Creek

Cross Bloomer Creek

STOP 1. Big Hollow Creek Section
(1 hour): At this stop we will examine both the Barnum and Bloomer Creek beds; these can be seen in the creek bed below the small farm north of the creek. The Barnum Creek bed is thin, but characterized by abundant flattish to ovoid hiatus concretions which are encrusted by Cladochonus and small bryozoans. The Bloomer Creek bed occurs about 150 feet upstream from the lower discontinuity and 12 feet higher in the section. This 8-inch-thick mudstone bed has numerous small corals (Pleurodictium, Stereolasma) which are commonly attached to phosphatic nodules and hiatus concretions. Above this unit is 25-30 feet of dark-gray and black shale. In a borrow pit upstream from the road crossing, the black shale grades upward to calcareous mudstone marking the base of Jaycox-equivalent King Ferry Member.

STOP 2. Bloomer Creek Section.
(1 hour and 20 minutes): We will walk north for 1500 feet crossing the main branch of Bloomer Creek to a more accessible section on its northern tributary. At this section we will observe the Mack and Bloomer Creek beds below the small waterfalls and study basal Moscow beds both at and slightly above the falls. This is one of the northernmost sections at which the Mack Creek bed can be observed. The Bloomer Creek bed occurs 8 feet above this unit; it is rich in brachiopod and molluscan debris and hiatus concretions are common; these display abundant epizoans.
The Tichenor Limestone Member occurs in the recess under the falls; it yields abundant pelmatozoan material including articulated crinoids. The Menteth and overlying Kashong Members occur upstream from the falls. Fossils are plentiful in the Kashong sequence, and they can be easily extracted from the Rhipidomella-Centronella Bed. The phosphatic pebble bed of the upper Kashong is inconspicuous, but it yields phosphatic pebbles and occasional phosphatic brachiopod and trilobite steinkerns. Return to vehicle and proceed back to main road.

STOP 3. Barnum Creek, Upper Ludlowville Section.
(2 hours, lunch first before examining the rocks): We will proceed around the waterfall, which is capped by the Menteth Member, and reach the creek by a safer downstream route. Wading up the creek, we will examine, in order, the Barnum Creek bed, Mack Creek bed, and Bloomer Creek bed. This is a classic complete profile shown schematically in Figure 2. Both the Barnum and Bloomer Creek beds yield a rich, shelly biota and numerous hiatus concretions. The disontinuities overlie intervals of mudstone bearing numerous in situ concretions which are the erosional source of hiatus concretions. Of particular interest is the occurrence of reworked, prefossilized conulariids in the Barnum Creek bed. Moreover, large differentially bored hiatus concretions occur in the Bloomer Creek bed; these show intense Trypanites borings on their upper surface and no boring underneath (Figure 6A). The nodules have different epizoan assemblages on their upper and lower surfaces, indicating development of microhabitats along their exterior.

STOP 4. Sheldrake Creek, Lower Moscow Condensed Stratigraphic Section.
(45 minutes): The Tichenor-basal Windom interval is represented by only 17-18 feet of section. The Deep Run Member is only 4.5 feet thick as opposed to 10 feet at Stop 2. The Menteth Limestone is thin and irregular in this section, and the Rhipidomella-Centronella bed of the Kashong Member is juxtaposed on it. The Tichenor Member is represented by a massive calcarenitic ledge with a sharp basal contact with the Ludlowville. Medial King Ferry beds will not be examined here, but the Mack Creek bed and the Bloomer Creek bed are both visible in the creek bank below the falls.

Portland Point quarry on left.
The Tully Formation (limestone) is quarried here, and the uppermost beds of the Moscow Formation (Hindom Shale) are exposed. For description of this locality see Grasso (1970) N.Y.S.G.A. field trip D and H, Stop 9. An excellent Tully-Windom exposure is developed to the right of the road in Minnegar Brook.

Salt mine to right.
The Morton Salt Company is mining salt from the Salina Group (Upper Silurian).

STOP 5a. Portland Point Type Section
(25 minutes): (see Figure 4). It occurs in a railroad cut along Cayuga Lake shore 300 feet south of entrance to Gulf Creek. There is noticeable southward dip to the strata so that 10-15 feet of uppermost King Ferry is visible below the Portland Point; the Portland Point-Kashong interval descends to railroad level over a 100-150 foot distance.
Originally, the Portland Point was described as including 9.0-9.5 feet of calcareous strata with a prominent calcarenite bed at the base and shell-rich limestone at the top (Cooper, 1929, 1930). The Portland Point is now redefined to include only the calcarenitic (Tichenor-equivalent) bed and overlying 2-foot muddy, Deep Run-Menteth equivalent limestone (Baird, 1979). 5.5 feet of succeeding beds are assigned to the Kashong Member. A prominent calcareous siltstone bed believed to be equivalent to the phosphatic pebble bed to the west occurs 8.5-9 feet above the base of the Moscow Formation; this may have been the top marker bed of Cooper's Portland Point section.
This bed occurs about one foot below a calcareous siltstone bed marking the base of the Windom. Above the base of the Windom are numerous Windom brachiopods including Athyris spiriferoides, Ambocoelia umbonata, and chonetids.

STOP 5b. Shurger Falls.
(20 minutes): We now walk back north to the mouth of Gulf Creek. Proceeding east (upstream) for 100-150 feet we come to Shurger Falls. The Portland Point is now at much higher elevation, capping the 40-50 foot waterfall. We will not climb the falls but will collect fossils from loose blocks which have fallen down.

A5: PALEOCOMMUNITIES OF THE ONONDAGA LIMESTONE (MIDDLE DEVONIAN) IN CENTRAL NEW YORK STATE
Richard H. Lindemann
Skidmore College
Saratoga Springs, New York
Howard R. Feldman
American Museum of Natural History
New York, New York
The Onondaga Formation of New York State is a 21-50+ m unit of Middle Devonian marine limestones. The formation's outcrop belt runs east-west from Buffalo to the Helderbergs and southward from the latter to Port Jervis, a distance in excess of 550 km. Over much of this area the limestone strata have been eroded into extensive escarpments and flats.
Onondaga stratigraphy and paleogeography have received a great deal of attention during the past three decades. Formational lithofacies have been identified and interpreted. The lithofacies and paleocommunities of at least ten Onondaga bioherms have been investigated. However, until recently non-reef paleocommunities have been neglected. Feldman (1978, 1980) and Lindemann (1980) filled this gap through separate studies of Onondaga paleosynecology using similar yet divergent approaches. It is the purpose of this trip to familiarize participants with Onondaga stratigraphy and with the results of these recent paleoecologic investigations. To these ends, this article describes the formation and its faunas. In the field, we will consider the formation's paleoenvironmental setting and the degree to which temporal changes in environmental conditions influenced and are revealed by vertical successions of Onondaga paleocommunities.

A5: PALEOCOMMUNITIES OF THE ONONDAGA LIMESTONE (MIDDLE DEVONIAN) IN CENTRAL NEW YORK STATE

STOP 1. Indian Reservation Quarry
This is the Indian Reservation quarry described in connection with Feldman's Leptaena-Megakozlowskiella community.

STOP 2. Type section of the Edgecliff Member
This is the type section of the Edgecliff Member which is named for Edgecliff Park, located just to the west. The member's full thickness of 2.3 m is exposed in the upper areas of the main quarry. Its erosional base is marked by the presence of phosphate nodules. In the southern quarry wall, 3 m of the Nedrow Member are exposed. The top of the Nedrow has been removed by erosion.

STOP 3. A nearly complete section of the Onondaga
Turn left into the broad flat quarried area adjacent to Route 91 and park. The Onondaga is exposed in the upper quarry. Walk up into it by way of the unpaved road which comes down to Route 91 just south of where you've parked.
A nearly complete section of the Onondaga is exposed in this quarry. Only the top of the Seneca is gone. Thicknesses of the members are given below. An excellent exposure of the "Springvale" can be found to the west of the large storage building seen from Route 91. Here the "Springvale" contains a sparse brachiopod-bryozoan fauna and phosphate nodules. The main quarry floor is in the Edgecliff Member which is best seen along the south wall; it is at your right as you enter. Most of the quarry wall consists of the Nedrow and Moorehouse Members. This is the type locality of the latter. Fracturing and jointing of the rock have made hand and foot holds insecure. Please avoid falling or dropping rocks (or yourself) on other trip participants. The Seneca Member can be closely observed above and to the east of the main quarry. You can get to it by walking around the quarry to the north.
Seneca Member | 1.5 m
Moorehouse Member | 7.0 m
Nedrow Member | 4.4 m
Edgecliff Member | 5.2 m
"Springvale" | 1.5 m

STOP 4. Reef in Edgecliff Member
East of Taylor Road in the clump of trees across from the first house on the left is exposed a small section of a reef in the Edgecliff Member. While exposure does not permit a three-dimensional study of the reef, the fauna which includes Cylindrophyllum, Acinophyllum, Emmonsia, and Favosites indicates that what we are seeing is part of the core facies.

STOP 5. Full Edgecliff and some Nedrow
Going up hill and out of town there will be what appears to be a wooded and scrubby area on the left (north) side of the road. This is sharply broken by the school athletic field. Turn left into the western corner of the field and park near the storage shed. Frog Pond quarry is the scrubby area west of the athletic field. You can get into the quarry by way of any of the foot paths which lead in that direction.
The full 5.8 m of the Edgecliff Member are exposed here as is the lower 1 m of the Nedrow. The base of the Edgecliff is exposed on the middle of the quarry face which overlooks the frog pond in the southwest corner of the quarry. Rock weathering and extensive exposure of bedding surfaces make sampling and fossil collection here excellent.

STOP 6. Seneca Member
Proceed uphill until you see black shale to the right and Oneida Creek to the left. Look for and park in the wide road shoulder to your left as the road leans right. Watch out for eastbound traffic!
While virtually all of the Onondaga can be pieced together in the creek bed downstream from here, we will observe only the Seneca Member, 3.7 m of which are present in the stream. If water levels and recent sediment transport have been kind, we will be able to see a rare exposure of the contact between the Onondaga and the Union Springs Shale. For those who are interested, the full thickness of the Cherry Valley Limestone, about 1 m, is exposed on the north side of the road. There is no need to scramble up the shale for it, just trace the bed along until you meet it near road level.

A8: GLACIAL GEOLOGY OF THE CHENANGO RIVER VALLEY BETWEEN BINGHAMTON AND NORWICH, NEW YORK *
Donald H. Cadwell
New York State Geological Survey
Albany, New York, 12230
REGIONAL SETTING
The field trip area (Fig. 1) is located in the southern part of the Chenango River valley, a tributary to the Susquehanna River drainage system. The region is included in parts of the Binghamton West, Castle Creek, Greene, Chenango Forks, Brisben, Tyner, Oxford, Norwich, and Holmesville 7.5 minute U.S.G.S. topographic quadrangles. The area has a total relief of 341 m (840 to 1980 ft). The bedrock is predominantly Devonian shale, siltstone,and sandstone (Fisher et al., 1970).
GLACIAL GEOLOGIC SETTING
Brigham (1897) recognized the extent of the glacial sediments within the Chenango River valley between Binghamton and the Mohawk Valley. Tarr (1905) described the characteristics of the glacial deposits near the Finger Lakes. Fairchild (1932) named the thick drift units in the Finger Lakes region the Valley Heads moraine. He delineated other areas of drift deposits: the Olean at the terminal moraine in Pennsylvania and the Susquehanna Valley kames. MacClintock and Apfel (1944) used the term "Binghamton moraine" to describe the Susquehanna Valley kames of Fairchild, indicating that the drift was deposited during a separate advance. They suggested that the Olean was the oldest Wisconsin, Binghamton - middle Wisconsin, and the Valley Heads - youngest Wisconsin. Peltier (1949) correlated terraces along the Susquehanna River in Pennsylvania with pre-Wisconsin, Olean, Binghamton, Valley Heads, and Mankato ice advances in New York. Denny (1956) questioned the presence of the Binghamton advance in the Elmira region. He theorized that (1) the Binghamton border may be north of the Valley Heads border and therefore concealed, (2) the Binghamton border is incorporated within the Valley Heads border, and (3) the character of the Binghamton materials is completely changed between the type locality (Binghamton) and Elmira. Connally (1960, 1964) on the basis of heavy-mineral analyses indicated that the Binghamton is related to the Valley Heads advance. Moss and Ritter (1962) suggested that the Binghamton was not a separate advance, but a phase of the Olean. Coates (1963) suggested that a single ice sheet deposited the drift with the Olean as the upland facies and the Binghamton as valley facies. Hollyday (1969) showed that the drift in the valleys in the vicinity of the field trip ranges between 15 and 76 m (50 and 250 ft) thick. I have presented the idea of a single Woodfordian ice sheet that deposited the Olean and Binghamton deposits, with a miminum age of 16,650 ± 1800 radiocarbon years B.P. for wood at the base of a bog (Cadwell, 1972a, 1972b, 1973a, 1973b, 1974, 1975, 1978). Incorporated in this idea is the concept of "valley ice tongue" retreat. An ice tongue may have extended several miles down valley beyond the upland ice-margin position. Krall (1977) described the Cassville-Cooperstown moraine as a late Wisconsin recessional moraine. Aber (1978) described the erratic-rich drift in the Appalachian Plateau of N.Y.
* Published by permission of Director, Science Service, New York State Museum, State Education Department, Journal Series No. 326.

A8: GLACIAL GEOLOGY OF THE CHENANGO RIVER VALLEY BETWEEN BINGHAMTON AND NORWICH, NEW YORK

View south across Binghamton.
Binghamton is built on outwash sands and gravels greater than 50 ft (15 m) thick.

Note kame terrace to right.

Outwash sand and gravel exposed in the kame terrace.

Route 7 rises onto kame terrace at Hillcrest.

Note gravel pits in sand-and-gravel outwash to the left of Route 369 as you proceed north.

Kame is on left.

STOP 1. Chenango Valley State Park
All of the glacial features preserved in this park were formed at the retreating Woodfordian ice margin. Massive amounts of sand and gravel was deposited around disintegrating blocks of ice (Refer to the topographic map of the state park and vicinity). These horizontally stratified sands and gravels are at least 200 feet (61 m) thick. An ice-channel filling is preserved between Lily and Chenango Lakes. The pebble lithologies are 10 percent limestone; 75 percent local siltstone, sandstone and shale; and 15 percent exotics (from outside the Chenango River drainage basin).

Note the sand pit to the left.
These sands were deposited in relatively quiet water adjacent to stagnating ice in the Page Brook valley. Meltwater was flowing from the north.

Meltwater channel.
The sand and gravel here is at least 175 ft (53 m)thick.

Note large kettles in outwash gravels.

A radiocarbon age date of 16,650 yBP
A radiocarbon age date of 16,650 ± 1800 yBP was obtained from wood at the base of a kettle to the right, over the hill.

This kame terrace has at least 250 ft (76 m) of sand and gravel.

Large kame terrace
Enter Chenango County. This road is on a large kame terrace built when an ice tongue occupied the Chenango Valley. The sand and gravel is at least 196 ft (60 m) thick.

Gravel pit in outwash gravels
A gravel pit to the right (up the road) has outwash gravels. An ice tongue occupied the main valley as meltwater flowed from the ice margin to the east. The lithologies present are 4 percent limestone, 76 percent locals, and 20 percent exotics.

Proceed across the kame terrace.

View across meltwater channel and outwash gravels.
These sands and gravels are as much as 100 ft (30 m) thick.

STOP 2. Wheeler Creek Esker
This will be a brief stop to discuss the formation of the Wheeler Creek esker (Refer to the topographic map). A thin ice margin was located at this point. Meltwater flowed westward from this margin toward the main Chenango Valley. The kame terraces and the esker were deposited adjacent to and beneath the ice, respectively.

Esker on left.
The esker can be seen on the left as you descend from the kame terrace. Meltwater flow was to the south.

Road is located on the crest of the esker.

Note the massive hummocky topography
Note the massive hummocky topography (valley plug) on the east side of the valley. This sediment and ice served as a base-level control for deposition to the north. The significance of this will be discussed at STOP 3.

This road is on top of a large kame terrace.

STOP 3. Lynk Delta
The Lynk Construction Company removes sand and gravel from this large delta/lacustrine complex. Meltwater was flowing from the east along Lyon Brook and sedimentation occurred in a lake adjacent to an ice tongue. Note the planar-surfaced features to the north. The elevation of all these features was controlled by the valley plug noted at mileage 40.1. The lithologies present are: 20 percent limestone, 52 percent locals, and 28 percent exotics.

Note pit in kame delta to the right.

Cross alluvial fan.
The thickness of drift in the valley is at least 350 ft (107 m).

STOP 4. Wedge Or Pop-Up?
Walk up into the bedrock quarry. This pit is used by the state for maintenance of the roads. The face of the exposure is oriented N20E along one of the joint planes. The wedges are developed along N75W. One wedge is well developed. Two others are partially developed. The wedges persist for at least 3 ft. to the east.

STOP 5. Picture stop of kame terrace.
When this kame terrace was deposited an ice tongue occupied the main Chenango valley. Note kame delta on the west side of the valley.

STOP 6. Chenango County Sand Pit
The exposure in this pit illustrates lake sands, silts,and clays, with current-ripple laminations. Several years ago exposures in this pit had a section beneath the well-stratified lake sands. In this lower section are examples of strata with vertical bedding; horizontal bedding that abruptly ceased into an unstratified zone; and cross-bedded sands with inclinations of up to 85 degrees. The lithologies present include: 18 percent red sandstone, 25 percent limestone, 42 percent locals, and 15 percent exotics.
It is hypothesized that a supraglacial lake developed with deposition of the lower sands. The lake abruptly drained causing frozen blocks of sediment to be rotated. Sedimentation continued around the rotated blocks depositing the ripple-drift sediments.

Kame delta on right
Kame delta on right, with foreset beds dipping to the South.

Note exposure in kame terrace on right.

Good exposure in kame delta.

STOP 7. Emerson Pit
This kame delta illustrates the variety of sediments and orientations in a delta deposited adjacent to an ice tongue. Refer to the topographic map for STOP 3.

Note ice contact kame delta to right.
Stop if you have time.

View to the left (east) of valley plug
View to the left (east) of valley plug that controlled the elevation of the deltas examined at STOPS 3 and 7.

View to left (east) to outwash units associated with Wheeler esker (STOP 2).

View east to Chenango Valley State Park area.

STOP 8. Till
The drift in this valley includes Olean-type till, Binghamton-type stratified units, and thick lacustrine clays. These units are interspersed between bedrock outcrops. Rotational slump blocks develop by a process of piping in the silt and clay beds.

Good view to the south of Chenango River valley.

A9: HYDROLOGY IN RELATION TO GLACIAL GEOLOGY ALONG THE SUSQUEHANNA RIVER VALLEY, BINGHAMTON TO OWEGO, NEW YORK
Allan D. Randall
U.S. Geological Survey
Over the past 20 years, several regional and localized studies have increased our knowledge of aquifers in the Susquehanna River basin of New York. This article extracts and summarizes some results of these studies that pertain to sites visited on this field trip along the Susquehanna valley from Binghamton downstream to Owego.
DISTRIBUTION OF AQUIFERS WITHIN THE GLACIAL DRIFT
About 85 percent of the Susquehanna River basin of New York is an upland in which shale, siltstone, and fine sandstone of Devonian age is dissected by narrow valleys and mantled by till. Stratified drift is confined largely to broad valleys, 1,000 to 8,000 feet wide, which occupy the remaining 15 percent of the basin.
During the waning stages of glaciation, tongues of ice extended southward along the broad valleys beyond the main ice sheet. Lakes formed near the ends of the shrinking ice tongues, temporarily filling any space vacated by melting of the ice that lay below the level of stratified drift previously deposited downstream. Many of these lakes were extensive, particularly in the deeper valleys, and trapped much clay, silt, and very fine sand. Elsewhere, particularly in relatively shallow valleys such as the Susquehanna River valley from Binghamton to Owego, smaller lakes and stream channels formed atop and against ice tongues that became too thin to flow. As each small lake filled with sediment, others formed nearby, and water velocities were often great enough to keep fine-grained sediment in suspension. The resulting stratified drift is heterogeneous but predominantly coarse grained, like the idealized sketch in Figure 1 and the actual cross sections in Figures 2 and 3.
Only the coarser sands and gravels within the stratified drift yield enough water to be considered aquifers.

A9: HYDROLOGY IN RELATION TO GLACIAL GEOLOGY ALONG THE SUSQUEHANNA RIVER VALLEY, BINGHAMTON TO OWEGO, NEW YORK

Note level terrace surface on right.

HESITATION STOP. Pit on left
Pit on left, in the highest (oldest) stratified drift in this part of the valley: cobble-boulder gravel to coarse sand variably silty (piles of coarse gravel rejected by operator are visible); pebbles are relatively drab (few limestones); topography is irregular, maximum altitude 880 feet; wet areas on pit floor suggest till at shallow depth. Barn on right marked "Tioga Manor"; trip will return past this barn.

Route 17C is on nearly level surface of valley train.

Pit owned by Concrete Materials, Inc.
Entrance (on left) to pit owned by Concrete Materials, Inc.

Pit owned by C & C Ready Mix Corp.
Entrance (on left) to pit owned by C & C Ready Mix Corp.

STOP 1. Kame Delta, Bright Gravel.
Stop 1 will be in whichever of these two pits offers the better exposures on the date of the trip. Topset and foreset beds of bright gravel have been observed beneath the valley-train surface; lower terraces are capped by bright fluvial gravel overlying fine-grained lake-bottom sediments.

STOP 2. Kames And Ice-Channel Filling, Drab Gravel.
Turn right at second driveway; proceed to gate at entrance to pasture and gravel pit owned by Kenneth Pipher. Be sure to close gate after entering.
Several pits in the kamic features in this locality revealed drab gravel and sand with very few limestone or other exotic rock types; west-dipping foresets have been observed. Maximum altitude is 860 feet, well above the bright valley-train surface to the east.

STOP 3. Ground-Water Recharge From Thorn Hollow Creek.
In 1967-68, streamflow measurements on 15 dates showed a loss of about 0.02 ft3/s (10 gal/min) per 100 feet of channel upstream from Glen Mary Drive and 0.16 ft3/s per 100 feet downstream. During most of the year, this stream goes dry somewhere on its alluvial fan.

Note road bordered and arched over by large maples.

Tioga Manor barn on right.
Behind barn is a hummocky surface 820-830 feet in altitude; a small pit revealed 1.5 feet of highly calcareous, bright, fine-pebble gravel with abundant limestone atop several feet of drab gravel.

HESITATION STOP. View to right of oval hill
View to right of oval hill in midvalley, composed of (or perhaps heavily mantled with) till. Terraces at about 830 feet altitude between the road and the hill, now largely excavated, were capped by bright fine-pebble gravel and coarse sand.

HESITATION STOP. Tracy Creek
The reach of Tracy Creek beneath the bridge visible to the right was dry on all eight occasions when visited by the U.S Geological Survey in the summers of 1962-65 as part of a study of low streamflow in the Susquehanna River basin. Like most tributary streams, Tracy Creek suffers severe seepage loss when crossing the stratified drift in the Susquehanna River Valley. Upstream 2,000 feet, where the creek has cut a gorge through till and bedrock, a small flow continued throughout the 1962-65 drought.

Cross Choconut Creek

Vestal municipal well is in well house on right.

STOP 4. Vestal Water District 1 Well Field.
Three municipal wells tap sand and gravel between 70 and 150 feet in depth. Induced river infiltration is potentially an important source of recharge; temperature profiles in April 1981 indicate river water infiltrated past well 1-3 at a time when only well 1-2 was in use. The sand and gravel seems to be relatively drab, perhaps totally drab near the base.

STOP 5. Vestal Water District 4 Well Field.
To the west is municipal well 4-2, water from which was found to contain organic solvents in 1980 (see text). To the north are two more municipal wells. To the south are numerous oil tank farms. To the east, the land was once level with Prentice Road, but has been excavated for gravel; the owner plans to mine gravel below the water table by dragline both east and west of the road. The pit to the east was once considered as a site for a municipal landfill

Flood-control reservoir
Flood-control reservoir is on right, on little Choconut Creek.

STOP 6. View Of Housing Cluster.
All homes in this area have public sewers and on-lot wells tapping bedrock. In 1981, water levels were as deep as 100 to 130 feet seasonally in some wells on Rhodes Road, and yields of a few wells were not as large as desired by occupants. Further building has been proposed downslope.

A10: GEOMORPHOLOGY OF SOUTH-CENTRAL NEW YORK
Donald R. Coates
Dept. of Geological Sciences
SUNY-Binghamton
The purpose of this trip is to examine geomorphology in the region to the east and south of Binghamton. The evolution of the Chemung, Delaware, Susquehanna, and Tioughnioga Rivers will be discussed. A variety of erosional features will be seen and much emphasis will be placed on glacial deposits and the landforms they create. The starting point of the trip will be the upper part of the SUNY Binghamton campus.

A10: GEOMORPHOLOGY OF SOUTH-CENTRAL NEW YORK

STOP 1. Campus Overview.
This site is the southernmost of three east-trending ridges which comprise a ribbed moraine sequence. The SUNY campus is situated on two of the ridges. Furthermore, the campus is nested in a reentrant in which the bedrock hillslopes have a scalloped form. Roundtop Hill, an umlaufberg, can be seen to the north. The drainage divide to the south contains a col, or saddle, which was the position for override by the glacier. The moraine is composed of bright till (Binghamton-type) with a fabric transverse to the ridge (or parallel with ice transport). Bedrock is more than 120 ft below land surface. All glacial deposits on this trip are Late Wisconsinan. Embark. Travel east on ribbed moraine with SUNY nature preserve and wetlands to south.

STOP 2. Stair Park.
Walk into park going south along Fuller Hollow Creek. Stream flows on bedrock, yet the floodplain appears to be in alluvial materials. Why has stream chosen a more difficult channel to occupy? Walk to 30-ft exposure of bright till (Binghamton lithology). What is the fabric of the till? Within Fuller Hollow there are good examples of fabric wherein some show extending flow and other compressing flow characteristics of the glacier. Such bright drift shows the history of materials. The ice moved south over the valley-fill sediments of the Susquehanna River, incorporating them into the basal load and then depositing them south of the river along thrust planes as the ice was forced to move up and over the hillsides. South from this stop the drift changes composition, passes into a transitional facies and finally becomes true "drab" till (Olean lithology) higher up on the hillsides.

In distance note the Roundtop Hill umlaufberg.
The highway uses the meltwater channel that separates the hill from the former upland parent spur to the south.

The river flows west on valley-fill sediments.
The river flows west on valley-fill sediments about 200 ft thick comprised largely of glacio-fluvial and glacio-lacustrine materials. Near Route 17 wood at about an 8-ft depth in alluvial materials was dated at 1690 ± 100 ybp.

STOP 3. Drab till (Olean lithology)
This 25-ft exposure east of Oakdale Mall consists of drab till (Olean lithology). This is typical of lodgment till plastered on the south sides of hills that produce asymmetry of hills, or the "till-shadow effect". What type of fabric would you anticipate from such a depositional environment?

Upper Rhinestreet Formation
Bedrock exposure of Upper Devonian Rhinestreet Formation consists of marine shale with some siltstone.

Chenango River.
Note flood walls, and revetment-type levees (armored with riprap) built by U.S. Army Corps of Engineers. Near this

Hillside quarrying of Rhinestreet Formation.
Binghamton brickyard and hillside quarrying of Rhinestreet Formation. The highway is adjacent to old Chenango Canal that connected Binghamton with the Erie Canal. The trend of the canal along here is called the "tow path" by residents.

Kame-terrace valley-train sediments
Exposure of kame-terrace valley-train sediments that comprise Hillcrest. Note highly cemented character of materials.

Cross Chenango River
Here valley fill is less than 100 ft thick. Note the umlaufberg, which is double crested. This part of the valley is more youthful because river was diverted from its earlier course on north side of umlaufberg.

Old valley of Chenango River
Note the route has been along west side of umlaufberg into the old valley of the Chenango River. This is now a "dry valley" filled with a congestion of glacial deposits and sand and gravel pits.

STOP 4. Rose Gravel Pit (now owned by Barett Paving, Inc.).
Travel into east part of pit, 1.2 mi. These materials occur in a very complex sedimentary environment. This can be considered a pitted outwash plain (sandur), that also includes valley train, kame, kame terraces, and extensive pro-gradational deltaic sequences. Although the deposits were formed during a single glacial stade and are comprised by materials of the same general provenance, there is great heterogeneity in the sediments from outcrop to outcrop. Thus the pit contains both pure outwash-type sediment as well as ice-contact deposits. There is a full range of textures from clay to silt, sand, gravel, cobbles, and boulders. Bodies of till also occur within some sequences. The extent, both laterally and vertically, of the cemented units pose serious problems for the miner. Geologically the problem is to determine the origin and time of cementation. For example, did it form in the vadose or groundwater zone? Did it form soon after deposition, or later in the Holocene? Aber (1979) has attempted to answer some of these points. Although much of the material is bright, there are also occurrences of drab drift. Why?

Highway ascends a wind gap.
This is one of three high-level notches along a north-trending ridge formed as overflow channels when ice occupied the Chenango Valley and meltwater streams discovered high outlets.

STOP 5. Chenango Forks.
This is junction of the Chenango River flowing southwest and the Tioughnioga River flowing southeast. The exposure typifies the many different sedimentary features at junctions of two different ice lobes, with contrasting histories and meltwater regimes. This is a kame environment with deposits that range through glaciofluvial, glaciolacustrine, and unsorted materials. What is the origin of the large bouldery unit? Possibilities include flowtill, mudflow - debris flow, ablation till, etc. Are there others?

STOP 6. Landslide.
This landslide consists of a series of slumps that cover a 7-acre area. It was caused when the road was cut into the lower hillslope. The increased slope and removal of material destabilized the materials. The hydraulic head increased and drainage from a road above the slide funneled water onto the mass. The hillside materials are composed of sediments susceptible to piping which enhance lubrication and movement of materials in the mass. Some pipes have been measured to be about 2 ft in diameter and extend many feet into the hill. The south side of the area is composed of drab till. Most of the slide occurs in glaciolacustrine silt and fine sand with clay more than 60 ft thick. Glaciofluvial beds occur immediately north of the slide area. What was the environmental setting when the deposits formed?

Bedrock.

Drab (Olean lithology) till.
These sequences are typical of the Tioughnioga River, a multicycle sluiceway or beaded river. The river is anomalous because it flows southeast across the structural grain of the region. The valley alternates between narrow walls which are younger parts of the system, and wider valleys which represent positions where the river discovered its previous valley.

Many kettles comprise this pitted valley train.
The road passes between many kettles which comprise this pitted valley train. Cadwell (1972) dated peaty materials in a kettle as 16,650 ± 1,800 ybp.

Old gravel pits on both sides of road.
Sedimentation is outwash type.

STOP 7. Chenango Valley State Park.
Separating Lily Lake to the north and Chenango Lake to the south is a crevasse filling. The lakes occupy kettle holes. The park contains tens of kettles of various sizes. These were stranded "land icebergs" that were overwhelmed by meltwater deposits when active ice was to the north.

STOP 8. Hale Gravel Pit.
Good example of outwash deposits. Bedding shows characteristics of the shifting meltwater channels that provided avenues for deposition of the materials. Although these are outwash deposits, they contain deleterious ingredients and so fail to pass state (magnesium sulfate soundness test) requirements for use as highway concrete (>18 percent loss on 10-cycle test). Why? What is the lithology of the sediment?

Bedrock - more youthful part of system
The Chenango River enters a more youthful part of its system, with the umlaufberg separating it from the former thalweg. Bedrock in or near a stream invariably means the channel is not located at the major thalweg.

Belden Hill. One of highest elevations in this area.
Drainage divide between the Susquehanna and Chenango Rivers.

On east side of Susquehanna is "The Plains"
On east side of Susquehanna is "The Plains" one of largest terraces in the region. Along the road there are many stagnant ice features.

Start of 0.6-mi - long esker
Start of 0.6-mi - long esker that parallels the highway on east side.

The road arcs around the Windsor umlaufberg.

STOP 9. Town Of Windsor Gravel Pit.
Turn right onto dirt road and proceed to working area. This is a beautiful "textbook" example of a kame, a hill composed of ice contact deposits. Meltwater erosion was responsible for dissecting the umlaufberg from the upland connection to the east. The deposits fall within the range of drab lithology and contain glaciofluvial, glaciolacustrine, and poorly to unstratified drift. What is the origin of the latter?

Kame-and-kettle topography, character of the umlaufberg
Note kame-and-kettle topography and the character of the umlaufberg, which can be considered "youthful" because of the lack of tributaries on it and the adjacent highlands.

Damascus.
Continue east on old "17" which now rises on a steep grade up Tuscarora Mountain.

Sky Lake, one of three natural lakes in Fly Creek.
This is drainage divide between the Delaware and Susquehanna Rivers. We are now in the Catskill Mountains, both geologically and geographically. The bedrock now consists mostly of terrigenous sandstone. Relief is 1500 ft and more, and the Delaware system drains the west and southwest part of the mountains.
2011: Sky Lake is 1.2 miles from here, over the hill to the NE. The road to Sky Lake is a few hundred meters back along the highway.

Deer Lake, second in the lake chain in Fly Creek.

STOP 10. Fly Pond. Picture stop.
A till barrier impounds this and the others have similar dams. What is the origin of these barriers? Depth to rock is reported to be 160 ft in the valley. There are also two smaller till mounds in Fly Creek.

STOP 11. Kame Delta.
At 1450 ft elevation this is an unusually high level deltaic deposit. However, it forms part of the large picture with a major lake that occupied the Gulf Summit area.

Major topographic low.
Note this area appears to be a major topographic low. Within it are numerous kames and kettles.

Spillway for drainage of the proglacial lake
Travel down road and observe character of the drainage divide at Gulf Summit. Return to railroad and view the deep bedrock notch. This was the spillway for drainage of the proglacial lake that occupied this topographic low. Although Wisconsinan-age meltwaters helped to incise the lowermost 70 ft, the higher features may have been initiated during earlier glacial stages.

STOP 12. View Of Spillway And Overflow Channel.
This is headwater area of Cascade Creek, a Susquehanna River tributary. The Catskill sandstone shows vestiges of stream erosion. North of the road the hill slopes contain varying degrees of blockfields, a reminder of periglacial climatic conditions.

Triple cities of Lanesboro, Susquehanna, and Oakland.
This is the Great Bend area where Susquehanna River arcs from a south flow, to an east flow, then a north flow. The unusual stone masonry bridge was built in 1848 by a Scotsman, Kirkwood, after several earlier contractors had gone broke attempting to build a span across the valley.

STOP 13. Oakland Esker,
Oakland Esker, largest in the region, with total length about 4 mi. Here it is on north side of the river but it can be followed northward where the river has incised it and the esker continues again on east side of river. The esker is not a simple ridge, but is double in several parts, such as near the outlet on the west side of Oakland. Side slopes are steep and esker exceeds a height of 100 ft. At the top there are depressions and undulating topography. Exposures here and at other outcrops show bedding ranging from horizontal to some units whose dips exceed 45°. Till and flow till are interpreted to be part of some sequences. The sparse number of exotics indicate the drift is drab type. Was this a supra-glacial (open to the sky) or subglacial esker?

Western limit of esker.

Penny Hill on north side of road.
There is a "rock city" at top of the hill, another indication of periglacial conditions.

Hanging delta on east side of highway.
This is the valley of the north-flowing Salt Lick Creek. The straightness of the valley, truncation of spurs, and anomalous southern extension indicate valley sculpture by ice and meltwater erosion.

Enter the New Milford sluiceway.

The most recent meltwater erosion starts here.

STOP 14. Picture Stop For The New Milford Sluiceway.
This is the south-trending Martin Creek valley, with bedrock walls of Catskill cross-bedded sandstone. This is a "youthful" type or first-cycle sluiceway because of the imperfect development of tributaries and absence of till. The feature was developed when meltwaters from a proglacial lake to the north drained south through spillways formed during earlier glacial times. The Great Bend region had a long and involved history throughout Quaternary times. The unusual geometry of the Susquehanna River implies it is an ice-marginal valley, such as parts of the Missouri and Ohio Rivers.

STOP 15. Hanging Delta.
This delta owes its development to events in Little Egypt Creek, the north-flowing stream on the east side of Maunatome Mtn. Along this north-south ridge there are a series of high level notches occupied by ice and meltwaters during different glacial and proglacial times. Drainage in Little Egypt was blocked by ice to the north causing the eventual overflow of the proglacial lake into Salt Lick Valley, where another lake received the sediments. Typical deltaic structures occur: topsets, foresets, and a general lobate pattern of strata that dip away from the central core. The materials are drab and currently used by the Pennsylvania Highway Department. The deposits are more than 150 ft thick. How did the massive sandstone block become emplaced within the sediments?

STOP 16. Doubleday Glen.
The Rhinestreet Formation forms bedrock of the area. Note the fabric of unconsolidated materials on top of rock. This is colluvium. Although composed of till it is not in place, having moved downslope by solifluction processes which produced the preferred orientation of the slabby clasts. Walk into the glen. Evolution of this feature is somewhat similar to the famous Finger Lake glens. They developed during postglacial time when a high-level consequent stream starts its new trajectory. Because till covered the preglacial valley and diverted streams to the south, many of the newly developing consequent streams were forced to carve new bedrock chasms. Thus when streams miss their former valleys, they incise rock and form narrow, steep-walled valleys. Where former valleys were encountered, the walls are gentler, not in rock, and wider.

B6: BIOCLASTIC CARBONATE UNITS IN THE CATSKILL CLASTIC WEDGE
Donald L. Woodrow
Hobart and William Smith Colleges
Geneva, New York
Paul Enos, Richard J. Bottjer and Charles Minero
State University of New York at Binghamton
Binghamton, New York
This trip we will visit two quarries in northern Pennsylvania (Fig. 1) which expose thick carbonate units nearly unique in the "Catskill delta". Our purpose is to examine these units and to discuss their origin, which in many respects remains enigmatic despite considerable study.
Each of us has contributed to this guidebook in a different manner.
All of us have examined both quarries in varying levels of detail. Woodrow and Bottjer measured sections in the Case quarry and considered the trace fossils and petrography there. Minero measured the Ashcraft quarry sections. Enos and Woodrow have supervised the work of several students in both areas.
STRATIGRAPHIC CONTEXT OF THE CARBONATE ROCKS
Rocks seen in the two quarries are part of the Catskill clastic wedge (Woodrow, 1968). Carbonate-rich rocks are unusual in this sequence which is typified by sandstones, siltstones, and shales. Both units were worked initially for agricultural lime, and quarries were later opened because the carbonates provide the best material for riprap available for many miles.

B6: BIOCLASTIC CARBONATE UNITS IN THE CATSKILL CLASTIC WEDGE

Esker on north (right) side of N.Y. 17.
Much of esker and associated kamic deposits have been removed for aggregate.

Small exposures of Chemung
Steep wooded hill with small exposures of Chemung (shallow marine) facies.

Road cut, Chemung facies.

Exposure of Chemung facies on right (W).

Road cut in Wiscoy Fm. (?)
Road cut in Wiscoy Fm. (?), Chemung facies, (shallow marine).

Road cut in lower Towanda Fm.
Road cut in lower Towanda Fm. Cattaraugus facies; red beds, some coquinite.

Road cut in Towanda Fm.
Road cut in Towanda Fm. with abundant flow rolls (pillow structures).

STOP 1. Louis Case Quarry, Burlington, Pa.
Enter Louis Case quarry on right (N) side of U.S. 6. Obtain permission from Louis Case in house at west edge of quarry.
Start in small face below main bench of quarry. Work upward toward east end of quarry.
The points of similarity between the two carbonate bodies (Table 2) are such that we conclude that both were formed in tide-influenced marine environments. However, contrasts between them are sufficient to make it clear that the local geography of the Catskill shoreline at the two sites must have been different. The abundance of brachiopods and the presence of crinoids and in situ bryozoa demonstrate that the environment of deposition of the coquinite was subtidal marine. Tidal effects are indicated by material from both marine sources (shells) and terrestrial sources (plant fragments, red muds), by the intimate intermixture of sandstone and shale (including flaser bedding), and by some examples of reversals in current direction. Most of the large-scale cross-strata record flow toward the west or northwest suggesting ebb-dominated deposition.
If the question of process is tentatively answered. we are left with the question posed by the mixture of materials in the coquinite. The source of the shell material was the local sea floor, despite the apparent ebb dominance, but the source of the red mud is less obvious. A source of highly oxygenated muds is required, perhaps from the higher, subaerial parts of a tidal flat or nearby alluvial plains. Plant debris could derive from the same sources. Shells in great quantity require a large community of epifauna either close to or as part of a tidal shore. The bryozoan clusters, at least, point to some production in situ.
The coquinites of the Case quarry have been interpreted as a part of a tidal delta (Woodrow) and as a subtidal zone of a tide-dominated fluvial delta (Bottjer). Strata above the coquinite indicate alternations of shallow marine and non-marine or supratidal environments. They contain mudcracks, in situ pedogenic carbonate nodules in red mudstones, and the enigmatic burrows or root cases; interlayered are beds containing marine fossils.
The local Upper Devonian shoreline was dominated by tidal processes, not by large streams and fluvial-dominated deltas. Material delivered to the shore appear to have been carried by small streams draining an alluvial plain or in channels of a tidal coast. Evidence of a large tidal range is lacking; a range of less than a couple of meters would probably account for the tidal features. Flow velocities were high enough in some areas, however, to move coarse material (shells and sand) as well as fines and to deposit them as migrating dunes and ripples. The localization of thick carbonate units may result from local amplifications in the tidal range or tidal velocity perhaps caused by indentations in the shoreline (bays).
In summary, both sequences appear to result from the concentration of shell debris, quartz, rock fragments, nodules, and wood by high-energy sedimentary processes in ebb-dominated tidal environments. Differences in lithology and geometry between the two units probably reflect local differences in the shoreline.

Kiln on left (N) side of road
Kiln on left (N) side of road where coquinite was exploited for agricultural lime and mortar. This is the type locality of the Luthers Mills Coquinite.

Large blocks of coquinite
Jct. township road. Large blocks of coquinite exposed in bed of Sugar Creek at sharp curve to west approximately 1/2 mi. north of U.S. 6. Long road cut in Towanda Fm. beginning at curve on township road.
2011: The township road is called Buttermilk Falls road, I believe. OHM

Overview of Susquehanna Valley to north

Overview up Susquehanna Valley to north.

Road cut in Towanda Fm.

Road cut in Wiscoy Fm. (?)

Potential lunch stop.
Rest area at Tioga Park race track (a monument to human folly).

Outcrops of Rhinestreet Fm.
Outcrops of Rhinestreet Fm., Chemung facies, to right in bed of Tracy Creek.

STOP 2. Ashcraft Quarry, Little Meadows, Pa.
Permission to visit quarry is obtained from Ashcraft Excavating Co. on Pennsylvania Ave., 2.5 mi south of N.Y. 434 in Apalachin, N. Y. Start in pit near east end of quarry. Work along main face to west end. Climb onto bench at west end.
The features of the limestone unit and of the strata surrounding it are explainable in terms of sedimentary process operating in shallow-marine environments where both tidal currents and waves were effective. There are few features of the limestone which suggest subaerial exposure, while the presence of brachiopods and crinoids and the development of a variety of sedimentary structures suggests deposition in shallow marine water. Reversals in current direction indicated by the paleocurrents, the textural maturity of the sand lenses within the limestone, and the lack of mud within the carbonate suggest a shallow-marine setting in which strong tidal currents winnowed out the fines and abraded the shell materials.
Shells, quartz sand, shale clasts, reworked nodules, plant fragments, and bones were all transported to this locality. The nodules and shale clasts must have been transported by strong currents from sources not too far distant, judging from the large clast size and relative lack of abrasion. The shells must have been transported from the nearby sea floor with extensive concentration and reworking to account for their numbers and abraded condition.
The internal plan of the carbonate mass seems to require three kinds of sedimentary processes: a) erosion and transport of sand, shells, nodules, etc. to the site; b) vertical accretion to form positive depositional relief; and, c) lateral accretion to produce the ultimate accumulation as either an isolated mound or a tabular body.
Thus, the carbonate mass appears to have been an accumulation built up above its surroundings by currents bringing to the site materials from the nearby sea floor or lagoon and from nearby terrestrial sources. Five hypotheses of accumulation have been suggested, no one of which is completely satisfactory or can be tested adequately with the available data. They are offered here as a basis for discussion.
Deposition as a subaqueous "shell mound" seaward of a beach/lagoon complex and/or a tidal flat was suggested by Krajewski and Cuffey (1976). Bowen (1978) postulated a "break-point bar" offshore from tidal flats. Both Krajewski and Cuffey (1976 and Bowen (1978) suggested significant contributions of skeletons produced in situ once initial relief above the sea floor was established. Another possibility is deposition on the subaqueous part of a land-tied accretion lobe or spit (Enos and Minero). Accumulation in the form of a tidal delta with both ebb and flood deposits represented has been suggested by John Bridge (pers. comm., 1981). Finally, some of the features in the unit are compatible with development as a small, mostly submerged, barrier bar as hypothesized by Woodrow.
In any event, nodules and other clastics were brought to the site of accumulation as the result of fluvial or shore-zone erosion and transport. A swamp seems the most likely source of ankerite nodules and abundant plant material. Shale clasts could have come from either the landward side or the seaward side of the carbonate accumulation. The source must have been one where mud normally accumulated and was periodically eroded. Wave and/or tidal scour of the nearby shelf provided the shells. Tides and waves reworked these particles into the limestone we see now.

B7: SOME ENVIRONMENTAL PROBLEMS OF THE BINGHAMTON AREA
Marie Morisawa and Burrell Montz
Department of Geological Sciences and Environmental Studies
State University of New York at Binghamton
Binghamton, New York 13901

B7: SOME ENVIRONMENTAL PROBLEMS OF THE BINGHAMTON AREA

STOP 1. Pierce Hill Cut.
This is a slope with active movement of material downslope. Originally a borrow pit. the slope has been cut back even more for the commercial development you see. Debris slides, slumps, rilling and rock fall are modes of downslope movement of the glacial materials. Both Howard's Florist and the Red Lobster have gone to considerable expense to stabilize the slope. One debris flow behind the Red Lobster reached the back door, covering several cars in the way. Subsequently. the wall and drainage pipes were installed.

STOP 2. Lower Fuller Hollow Creek.
Here the creek has been riprapped to prevent erosion of the bed and further down the banks are riprapped. The riprap has progressively deteriorated, large blocks have removed and side-walls have slumped.

STOP 3. Middle Fuller Hollow Creek.
Evidence of destructive erosion can be seen here. The foot bridge was washed out in the spring of 1981. Note widening of the channel. Excessive runoff from storm drains have caused much erosion here. Along the downstream reach many landowners are losing their back yards.

STOP 4. Upper Fuller Hollow Creek.
From this viewpoint. one can see the 300 home Stair development. The whole hillside was wooded until approximately 1974-75. Tributaries and storm runoff are piped underground directly to the creek, greatly augmenting flow during storms. Directly below is a meadow through which the main creek flows. This would have been an ideal spot for a detention pond to which runoff could have been piped.

STOP 5. Vestal Plaza Slope.
This cut has failed in many places since it was made. The north-facing slope has moved much more and did so more quickly than the south-facing slope. The cut is in glacial material. Much of the fine sediment has been removed by mud flows which cover the road whenever it rains. Buildings and parking lots on the surface above the slopes have contributed to mass movement.

STOP 6. Rockbottom Dam.
This dam is currently being rebuilt after years of deterioration on the older one. The dam is designed to retard the flow of water and to produce ponding so that the water intake for the City of Binghamton's water supply is below the surface even in dry years.

STOP 7. Susquehanna River.
The bend in the river at this point led to flooding of the area between the river and the gas station during the ice jams in February.
2011: This is the second Stop 6 on the road log. OHM

STOP 8. Conklin Park.
This park was flooded entirely during the February 1981 flooding. Water levels reached up to the park sign. Although there are some buildings in the park, they are for storage, primarily. This park is a good example of how flood plain areas should be developed.
2011: This is Stop 7 on the road log. OHM

Note the houses in this area
Note the houses in this area (which was also flooded in February). Each has a nice view of the river and gets flooded-almost annually. These are obvious examples of uneconomic floodplain development.

B11: DEPOSITIONAL ENVIRONMENT OF THE ONEONTA FORMATION (CATSKILL FACIES), NEAR UNADILLA, NEW YORK
John S. Bridge And Lorraine E. Dingman
State University of New York
Binghamton, New York 13901
A large roadside exposure on Interstate 88 near Unadilla (Fig. 1) offers a unique opportunity for detailed study of both vertical and lateral lithofacies variations in the Upper Devonian Catskill facies.
The rocks are assignable to the Oneonta Formation (Fletcher, 1963; Rickard, 1975), and the postulated early-middle Frasnian age (Polygnathus asymmetricus conodont zone) of this formation is supported independently by the miospore studies of J. B. Richardson (pers. comm.). This paper presents a detailed description and interpretation of the lithofacies, and a brief comparison with other published studies of Catskill-facies sedimentology. For convenience, the rocks were separated into two main facies associations which can usually be clearly distinguished in the field.

STOP 1. Oneonta Formation, Catskill Facies.

NEW YORK STATE GEOLOGICAL ASSOCIATION 54th ANNUAL MEETING
Amherst, New York
GUIDEBOOK FOR FIELD TRIPS IN WESTERN NEW YORK, NORTHERN PENNSYLVANIA AND ADJACENT, SOUTHERN ONTARIO
Edward J. Buehler and
Parker E. Calkin Editors
Held in Conjunction with 11th Annual Meeting Eastern Section American Association of Petroleum Geologists
Published by the New York State Geological Association. Guidebook available from the executive secretary: M.P. Wolf, Geology Department, Gittleson Hall, Hofstra University, Hempstead, New York 11550.

A1: UPPER MOSCOW-GENESEE STRATIGRAPHIC RELATIONSHIPS IN WESTERN NEW YORK: EVIDENCE FOR REGIONAL EROSIVE BEVELING IN THE LATE MIDDLE DEVONIAN
Carlton E. Brett
University of Rochester
Rochester, New York 14627
Gordon C. Baird
SUNY College at Fredonia
Fredonia, New York 14603
A widespread regressive episode, immediately preceding the late Middle Devonian Taghanic onlap, has long been recognized in eastern North America (Grabau, 1917; Cooper, 1930; Cooper and Williams, 1935; Heckel, 1973; Dennison and Head, 1975; Rickard, 1975). Regional erosive overstep of Hamilton beds by Tully and Genesee strata was documented in the Finger Lakes area (Cooper and Williams, 1935) and was recognized west of Canandaigua Lake (Cooper, 1930), but the nature of pre-Taghanic unconformity in western New York remained obscure due to supposed lack of stratigraphic controls in the upper Moscow (Windom) shales. Indeed certain workers (Stover, 1956; Fulreader, 1957) believed that upper Windom beds were relatively little affected by erosional truncation.
Contacts of the Middle Devonian Windom Shale Member, previously examined and discussed (Brett, 1974a; Brett and Baird, 1975), have received continued study by the present authors; results of new work on the Windom-Genesee paraconformity and adjacent strata in the Erie County region are discussed herein.
Detailed correlation and study of Windom Shale component zones has been undertaken. At least fourteen mappable Windom marker beds and intervals have been correlated across all, or part, of Erie County; these are summarized in the present text. Mapping of Windom units immediately underlying the Genesee Formation permits detailed inference as to the nature of this unconformable contact. These beds also provide insight into the processes of marine mud sedimentation during deposition of the Windom and its influence on fossil community distribution. Particularly notable is the discovery that the thickest Windom sections in the county are the least stratigraphically complete and the thinnest generally display the full complement of marker beds and zones.

A1: UPPER MOSCOW-GENESEE STRATIGRAPHIC RELATIONSHIPS IN WESTERN NEW YORK: EVIDENCE FOR REGIONAL EROSIVE BEVELING IN THE LATE MIDDLE DEVONIAN

Roadcuts in cherty limestone of Onondaga Limestone
Roadcuts in cherty limestone of the Clarence Member, Onondaga Limestone (Middle Devonian). This is the site of the Vogelsanger Quarry; prior to construction of the highway, this quarry exposed a well developed reef in the Edgecliff Member (now covered).

STOP 1. Bay View (Penn Dixie) Quarry.
(1 1/2 hours): This abandoned shale pit, previously described in detail (Brett, 1974b), provides an excellent reference section for the Windom Shale and its upper contact with the Genesee Formation. Here the Windom Member is approximately 13 m (42 ft) thick; 14 units described in the text can be recognized at this 1ocation. The disconformable basal contact with the Tichenor Limestone is excellently exposed in a low domal outcrop in the northeast corner of the shale pit.
The basal Ambocoelia umbonata beds Bav View Coral bed (type section) and Smoke Creek bed are accesslble in this area. Barren shales of unit 4 occupy much of the flat floor in the center of the shale pit. Near the top of this interval is a narrow zone containing abundant fossils including highly compressed brachiopods (Pseudoatrypa, Mediospirifer, Mucrospirifer consobrinus) and rare pyritized sponges and blastoids; this unit is termed the Big Tree bed (unit 5). The A-E limestones (units 6-11) crop out as uniform, white-weathering bands which trend roughly east-west across the quarry. Soft shales above the highest limestone band (unit 12) yield abundant pytitlzed burrow fil1ings and fossil steinkerns including nuculid clams, gastropods and cephalopods. This interval of approximately 2 m (6 ft) thickness, termed the Penn-Dixie pyritic beds, is characterized by small specimens of the brachiopods Tropidoleptus carinatus and Ambocoelia cf. A. nana. The calcareous Amsdell bed unit 13; = "Praeumbona bed") caps a low bench near the southern end of the quarry. Beyond this the Penn-Dixie shale pit terminates in a low (2-3 m high) bank which exposes uppermost Windom beds (unit 13) and the contact with the overlying Genesee Formation. The upper beds of the Windom comprise soft, gray shales with concretionary beds near the top; the top of the Windom is marked by a concretionary layer of 20-30 cm (8-12 in) thick containing Ambocoelia? praeumbona, followed by a thin band of argillaceous limestone which has been partially torn up and incorporated in the overlying North Evans Member.
The North Evans Limestone of the basal Genesee Formation comprises 3-10 cm (1.5-4 in) of buff-weathering, dark-gray crinoidal, calcarenitic limestone, which contains very abundant conodonts of mixed zones (lower asymmetricus subzones). Angular intraclasts, up to 10 cm (4 in) across, derived from the upper Windom occur abundantly in the North Evans. Black shales (Geneseo and Penn Yan) are absent from the lower part of the Genesee Formation and the Genundewa Member, a thin Styliolina-rich limestone rests directly on the North Evans.
At Penn Dixie Quarry as at most localities in western Erie County, the Windom is thin, but stratigraphically quite complete. However, ironicaily, in these sections unlike those farther east, the upper contact exhibits evidence for erosional scouring. Presumably the scouring of the upper Windom beds and presence of pebble imbrication within the North Evans remanié sediments reflect a late episode of erosion, associated with the pre-Genundewa erosion surface. This event post dates the development of a south dipping truncation surface, prior to Tully deposition, which had left upper Windom beds relatively intact in southwestern Erie County sections.
2011: Now owned and operated by Hamburg Natural History Society, Inc. http://www.penndixie.org/welcome.html   OHM

STOP 2. Cazenovia Creek Section.
Park near location where power lines cross Northrup Road. At utility poles on east side of road turn right and walk down dirt path to the base of cliff on the flood plain of Cazenovia Creek. At bottom of path turn left and walk north for about 600 ft, following the base of cliff (swampy ground), to exposures along the west bank of Cazenovia Creek.
(1 1/2 hours): This east facing cliff provides an excellent, long section of the Windom/Genesee contact. The Genundewa Limestone is nearly at water level at the southern (upstream) end of this section; however, downstream about 1/10 mile some 2 m (7 ft) of Penn Yan and upper Windom shales are exposed beneath the Genundewa. Lowest beds, exposed in the creek floor, are the Penn Dixie pyritic beds of the upper Windom. Diagnostic small specimens of Tropidoleptus carinatus can be obtained in abundance at this location. Overlying beds contain a zone of distinctive ellipsoidal concretions, typically with pyritic cores. The Amsdell bed (unit 12) forms a prominent, light-gray weathering calcareous band about 1 m thick near the top of the Windom. Near the southern end of the section this bed forms a small waterfall in Cazenovia Creek. Note the absence of upper shales (unit 13) in contrast to Penn Dixie Quarry (Stop 1).
The contact between the Windom and the overlying Genesee is sharp and planar with little evidence for erosive scour. Four or five lenses of the Leicester Pyrite, ranging from 1-15 cm thick and up to 2 m across, occur along the Windom/Penn Yan contact at widely spaced intervals. The pyrite contains abundant, reworked, pyritic burrows, diminutive brachiopods, mollusks, fish bones and wood. One lens along this section exhibits interfingering with the black Penn Yan shale. Lower surfaces of the pyrite lenses exhibit parallel ridge and furrow marks suggestive of current scour of the underlying Windom muds. At this locality about 0.5 m (1.6 ft) of barren, black, laminated Penn Yan Shale overlies the Windom; the upper portion of this shale contains large septarian concretions that locally protrude up into the overlying Genundewa. The Genundewa forms a prominent overhanging ledge about 40 cm (15 in) thick. The lower surface of this ledge is undulatory and is marked by a veneer of encrinite, conodonts, carbonized wood, and abundant fish bones and rare hiatus concretions. This unit probably is correlative in part with the typical North Evans a few miles west of this locality. The upper contact of the Genundewa with the silty, dark-gray West River Shale is gradational. Lower West River beds here yield abundant Pterochaenia, wood, chonetids, pyritized goniatites and rare crinoid columns. Higher units exposed in the upper cliff face include the black Middlesex Shale and gray, concretionary Cashaqua Shale, members of the Sonyea Formation.

Northrup Road bridge over Cazenovia Creek.
Note falls in creek over the Tichenor Limestone of the basal Moscow Formation, just upstream (east) of the bridge. High cliffs visible in the distance, upstream from the falls, expose about 12 m (40 ft) of Windom shale, capped by the Genesee Formation. The Smoke Creek bed is near the base of the cliff. At the upper contact, the Amsdell bed has been largely eroded away.

Note exposures of black Rhinestreet Shale (upper Devonian).

STOP 3A. Buffalo Creek At Old Bullis Road Bridge.
(1/4 hour): From bridge, view exposures along Buffalo Creek. Downstream (north) and just south of new bridge a series of ledges crop out in the creek floor, representing a condensed upper Ludlowville/lower Moscow section; the lowest ledge is a basal bed of the Jaycox Member, followed by Tichenor Limestone, and calcareous ledges of condensed Deep Run, and basal remnant of Menteth Members followed by highly calcareous Kashong Shale Member. The Windom/Kashong contact, marked by scattered phosphatic nodules is exposed in the floor of the creek directly beneath the old bridge. Looking upstream (south), note high bank exposures of gray, lower Windom Shale. A light-weathering calcareous band about 4 m (13 ft) about the creek floor represents the Smoke Creek bed; concretionary shales beneath this level for about 1 m (3 ft) comprise a local manifestation of the Bay View Coral bed. Note the thickening of the lower Ambocoelia-rich shales, here about 3 m thick, compared to about 15 cm (6 in) at Penn Dixie Quarry (Stop 1). At the next stop we will see higher beds of the Windom Member, the lowest of which are slightly higher than the top of this cliff section.

STOP 3B Buffalo Creek, Upper Windom Shale Section.
(1 hour): This bank exposes about 5 m of upper Windom overlain by Genesee Formation. The lowest shales exposed in the creek bed contain abundant Zoophycos spreiten and thin layers rich in the chonetids, Pseudoatrypa, Mediospirifer, and other brachiopods. Pyritized fossils including nautiloids and one cluster of blastoid Hyperoblastus have been discovered at this level. These shales appear to represent the Big Tree fossil bed (unit 5). They are overlain by two or three horizons of large, flattened ellipsoidal concretions probably equivalent to the A and B limestone bands farther west. Large irregular masses of pyrite occur associated with these concretions. Above the concretions is an interval of friable, dark gray shales, with abundant pyritic burrow tubes and scattered pyritized nautiloids, nuculid clams, wood and other fossils, herein designated the Buffalo Creek pyritic beds (unit 8). The C,D and E limestone beds (units 9-11) are clearly visible in the upper part of the bank. At the far south end of the section it is possible to examine the upper contact of the Windom with the overlying Genesee. The last meter of soft shale immediately beneath the contact contains abundant, small Tropidoleptus diagnostic of the Penn Dixie beds (unit 12). Small ellipsoidal concretions just beneath the contact may correlate with those in the upper Penn Dixie beds at Cazenovia Creek. Note the absence of Amsdell and upper shale beds (units 13 and 14) in contrast to Cazenovia Creek and localities farther 'west. These upper units have been truncated pri or to depos ition of the overlying Penn Yan Member. Lenses of Leicester Pyrite are present at the contact in sever~l location~, but are not readily access i b 1 e, although the Leices ter can be observed in fallen blocks. The Genundewa Limestone ranges from 0 to 10 cm in thickness; Styliolina limestone and g1ausonite coated hiatus-concretions occur in depressions on an undulatory erosion surface at the top of a ledge-forming concretionary band 1.6 m above the base of the Penn Yan.

STOP 4 Little Buffalo Creek, Upper Windom Section.
(1 hour): This small creek exposes an excellent section of the Upper Windom, Leicester, Penn Yan Shale (here about 1.8 m thick) and Genundewa Limestone. Lowest exposures include the richly fossiliferous Big Tree bed in the Windom, slightly below a layer of flat concretions. This fossil bed yielded atrypids, Srinocyrtia and other species. The Buffalo Creek pyritic beds (unit 8) are well exposed in the floor of the creek upstream and here contain Devonochonestes coronatus and are Pseudoatrypa in addition to pyritic tubes and nautiloids characteristic of the bed farther west. The uppermost beds of the Windom include a band of argillaceous limestone followed by shale and irregular large septarian concretions. These units comprise the C and D limestone beds respectively. The upper E unit as well as the Penn Dixie beds are missing at this locality. In places, the septaria of unit D protrude uoward and deform the basal Penn Yan Shale: lenses of Leicester Pyrite lap directly onto these concretions. Upstream from the Windom/Penn Yan contact a spectacular bed of grotesquely shaped concretions occurs in the upper Penn Yan Shale immediately below thin Genundewa Limestone. Here the Genundewa contains a basal veneer of North Evans lithology, including glauconite and pyrite-coated hiatus concretions. These concretions, characterized by internal lamination, have been completely disinterred from the Penn Yan and rolled into new orientations. This pre-Genundewa disconformity is believed to correlate westward with the North Evans limestone.

STOP 5A Cayuga Creek, Upper Windom Section.
Turn left into driveway just before intersection with Eastwood Road on right. Park at end of the drive and proceed on foot to lower section of Cayuga Creek. Walk back upstream toward Clinton Road bridge.
(1/2 hour): The upper 3.5-4 m (11-13 ft) of the-Windom Shale are exposed beneath the bridge. There are two zones of elliosoidal calcareous concretions, separated by about 2 m (6.5 ft) of nearly barren pyritic fissile dark gray shale. The lower concretion band is well exposed in the creek floor north of Clinton Road; surroundinq shales contain abundant small brachiopods and a pyritic fauna with large masses of pyrite. This interval resembles superficially the Buffalo Creek pyritic bed (unit 8) but is apparently coextensive with lower barren shales of unit 4 seen farther west.
An upper concretionary band occurs 15-30 cm (6-12 in) below the upper contact of the Windom. Shales immediately above this concretion level are highly fossiliferous and contain abundant chonetids, Mediospirifer, Spinocyrtia, Athyris and Pseudoatrypa. This band appears to be coextensive with the Big Tree bed (unit 5) and it may also represent a western remnant of the Fall Brook Coral bed seen in Genesee County and farther east.
The upper contact of the Windom is sharply defined and exhibits local truncation; the Big Tree bed is observed to approach the contact as it is traced northward along this section of Cayuga Creek. The Windom is abruptly overlain by black fissile shale (possible westward limit of the Renwick Member); it contains oriented Styliolina and patches of chonetid brachiopods. Large lenses of rusty-weathered Leicester pyrite occur at the contact near the Clinton Road bridge. These have yielded well-preserved pyritized wood, fish bones, and other fossils.

STOP 5B. Cayuga Creek, Lower Genesee Section.
Turn riqht into driveway on east side of bridge and park at end of drive. Walk to falls and remains of concrete dam across Cayuga Creek.
(1/4 hour): This section has been thoroughly described in previous field trip guidebooks (see Kirchgasser and Brett, 1981, p. 18). The Genesee Formation here includes 1.3 m (4.3 ft) of black and dark gray (Renwick?) Shale, followed by 1.8 m (6 ft) of gray, concretionary Penn Yan Shale. A prominent line of concretions occurs near the top of the section and is probably correlative with that seen in Little Buffalo Creek. A ledge of Genundewa Limestone about 20 cm (8 in) thick caps a low waterfall near the remains of an old concrete dam. The base of this ledge, again, contains encrinite and black hiatus concretions indicating an eastward extension of the North Evans type lithology associated with a pre-Genundewa erosional unconformity.

A2: CARBONATE FACIES OF THE ONONDAGA AND BOIS BLANC FORMATIONS NIAGARA PENINSULA, ONTARIO
Mary Rose Cassa
Gulf Research and Development Company
Pittsburgh, Pennsylvania
Don L. Kissling
ERCO Petroleum Services, Inc.
Houston, Texas
Devonian bioherms of the northern Appalachian Basin have been an important source of hydrocarbons since the 1967 discovery of gas from an Onondaga pinnacle reef in Steuben County, New York. Onondaga bioherms are represented in the outcrop belt by small organic buildups which have been studied for at least three-quarters of a century (Grabau, 1903; Stauffer, 1913,1915). More recent studies of these buildups and their components enable us to better understand the paleogeographic distribution of the buildups, their internal facies structure, and their importance in hydrocarbon exploration.

A2: CARBONATE FACIES OF THE ONONDAGA AND BOIS BLANC FORMATIONS NIAGARA PENINSULA, ONTARIO

Tonowanda Channel of Niagara River on right.
Grand Island is visible across the river, behind us. At the south end of Grand Island, the Tonowanda and Chippewa Channels join and Fort Erie, Ontario can be seen across the river.

Lock in Black Rock Canal on right.

STOP 1. Ridgemount Quarry
Hard hats must be worn. Please exercise caution near quarry walls; watch for overhangs and loose rock.
An excellent exposure of the Silurian-Devonian unconformity is found in the north wall of this quarry. Several small bioherms are exposed in the northern part of the quarry and in an "embayment" a few hundred feet west of the entrance. The mounds are characterized by abrupt thickening of lower Edgecliff strata which contain abundant solitary and colonial rugose corals, tabulate corals, and crinoid material (Figure 9). Dominant coral genera include Acinophyllum, Cladopora, Heliophyllum, Cystiphylloides, Syringopora, and Emmonsia. Internal structure is stratified; facies are represented as successive layers which pinch out laterally and drape over one another to give the characteristic mounded appearance. Stratified structure and absence of rigid framework indicate that turbulence was low during deposition. Biohermal strata contrast markedly with laterally equivalent and onlapping crinoidal packstone and wackestone beds of non-biohermal Edgecliff.
Sub-biohermal Strata
Mottled olive-gray Bertie Dolomite is unconformably overlain by 0.4 m of yellowish-gray conglomeratic Springvale Sandstone, containing large, flat dolomite clasts. The Bois Blanc consists of 3.2 m of light olive-gray, cherty, fine-grained limestone, containing trilobites, bryozoans, and abundant brachiopods. The mounds are separated from the Bois Blanc Limestone by a thin, shaly zone.
Biohermal Strata
The base of the larger mound sags markedly into underlying strata. Basal beds of the two mounds are similar, consisting of 0.2 to 0.5 m of yellowish-gray, crinoid packstone. Abundant in-place Syringopora and other corals are found in the basal beds of the smaller mound.
The overlying facies, 1.0 to 1.5 m of crystalline coral-crinoid packstone, can be traced between mounds. It contains Acinophyllum, Syringopora, Cladopora, Heliophyllum, and Cystiphylloides, as well as large crinoids whose columnals measure up to 2 cm in diameter. The smaller mound is capped by coral-crinoid packstone-grainstone, containing abundant Acinophyllum, common Heliophyllum, and sparse Cystiphylloides.
In the larger mound, the coral-crinoid packstone is overlain by 0.5 m of coral-dominated wackestone, which, in turn, is overlain by 0.5 m of packstone containing Acinophyllum and branching tabulate corals, Cladopora and Aulopora. Above that, Acinophyllum, Heliophyllum, and Cystiphylloides are found in coral-crinoid grainstone or packstone matrix. This facies is porous, with bitumen-lined interparticle and intraskeletal pores. The mound is capped by up to 0.5 m of crinoid-stylioline wackestone-packstone, containing few corals. Rare chert nodules in biohermal beds are light-colored and highly irregular in shape. Overlying the mounds are olive-gray, argillaceous crinoid-stylioline wackestone and mudstone, containing abundant dark chert nodules and many rugose and tabulate corals.
Non-Biohermal Strata
The overthickened, richly fossiliferous strata of the bioherms grade laterally into somewhat thinner, non-biohermal beds of the lower Edgecliff which consist of medium-grained crinoid grainstone and packstone containing few corals. This facies, approximately 0.8 m thick, is overlain by 7.6 m of crinoid packstone and grainstone which contain many Heliophyllum and Acinophyllum colonies. In his description of this locality, Oliver (1976) assigned these beds to the Clarence Member, perhaps based on the presence of chert nodules or on the darker, more argillaceous nature of laterally equivalent beds which overlie the mounds. Although the exposure could represent a local, fossiliferous facies of the Clarence, Oliver's (1976) suggestion that the Edgecliff and Clarence interfinger may be borne out here in the occurrence of light gray biostromal beds characteristics of the Edgecliff in association with darker olive gray, argillaceous beds containing fewer corals.

Battlefield and museum on right.
Plaque on museum building reads: "This house stood on the battlefield during the Fenian raid June 2, 1866. John Teal's family cared for the wounded soldier shot near the front verandah." Monument is memorial to "Queen's Own Rifles, 13th Hamilton Battalian Caledonian and York Rifle Companies of Haldimand in defense (sic) of country June 2, 1866."

Port Colborne Quarries, Ltd. to the north.
These quarries are floored in the Silurain Bertie Dolomite.

Robin Hood Flour mill is visible to the northwest.
Port Colborne is the second largest flour milling city in Canada.

Cross Welland Canal - Lock No.8.
The Welland Canal connects Lake Ontario (St. Catherines) with Lake Erie, an elevation difference of 99.5 m (326.5 ft). It was built in the early 1800's and had to be widened, straightened, and deepened several times as ships increased in size and traffic volume grew. This lock, the guard lock, was the longest in the world when it was built in 1933.

R.E. Law Crushed Stone Quarry on right.

STOP 2. Port Colborne West Quarry
Hard hats are optional. Please exercise caution near quarry walls, both from below and from above.
A portion of a broad biohermal bank is particularly well exposed in the east wall of this quarry (Figure 10). Original reconnaissance and detailed study were carried out here and in the R. E. Law quarry, approximately one mile north. The Law quarry is floored in Silurian dolomite and exposes Springvale and Bois Blanc strata, including greenish, Acinophyllum-rich beds of the upper Bois Blanc and lower Edgecliff, which represent initial stages of bioherm development. This southern quarry is floored in the upper Bois Blanc (Oliver, 1976). Lower Edgecliff strata are characterized by a coral assemblage which includes Cystiphylloides, Cylindrophyllum, and Heliophyllum. The tabular "core" facies contains a variety of colonial rugose corals and replaces bioclastic beds which are more characteristic of the Edgecliff. Massive favositid tabulate corals are more abundant in the upper, less argillaceous beds.
Glacially scoured surfaces are exposed around the perimeter of the quarry, particularly at the south end. The smoothed surfaces reveal glacial striations and offer spectacular plan-view exposures of the fossil bioherm community.
Sub-Biohermal and Bioherm-Equivalent Strata
Calcareous sandstone and sandy limestone and chert of the Springvale Member unconformably overlie the Bertie Dolomite (exposed in the Law quarry). Glauconite gives the Springvale its characteristic greenish color. Cherty, fossiliferous, fine-grained limestone makes up most of the remaining Bois Blanc, which is characterized by the brachiopod Amphigenia elongate (Telford and Tarrant, 1975; Oliver, 1976), in addition to rugose and tabulate corals, trilobites and bryozoans. The upper part of the Bois Blanc differs in consisting of greenish, shaly limestone which grades upward into overlying Edgecliff beds. Oliver (1976) drew the boundary between the formations based on occurrence of Acinophyllum species. Beds which contain A. stokesi and A. simcoensis are considered Bois Blanc; those containing A. segregatum are Edgecliff. He suggests that these units may represent the missing time interval between Bois Blanc and Edgecliff deposition elsewhere. The lithologic transition suggests that similar depositional conditions prevailed throughout late Bois Blanc and early Edgecliff sedimentation. Acinophyllum biostromes which developed under these conditions represent incipient stages of bioherm development.
Biohermal Strata
Two thin (20 cm) beds of Acinophyllum bafflestone mark the earliest phases of Edgecliff bioherm development. These beds and argillaceous limestone containing diverse coral fauna, including rugose corals, Cystiphylloides, Cylindrophyllum, Heliophyllum, and the tabulate favositid coral Pleurodictyum, are exposed in Law quarry and in the northern part of the inactive (southern) quarry. Total thickness is 4.2 m. Overlying are 0.8 to nearly 2.0 m of massive, light-colored limestone dominated by Acinophyllum in association with rugose corals, Cystiphylloides and Heliophyllum, tabulate corals, Favosites and Emmonsia, and sparse stromatoporoids. Intraskeletal porosity is well-developed; black bitumen stains are common. Matrix consists of crinoid grainstone and packstone and contrasts markedly with that of the underlying, more argillaceous Cystiphylloides and Acinophyllum beds.
The massive-bedded Acinophyllum facies is overlain by 7.6 m of medium-bedded packstone, wackestone and grainstone which contains a varied and abundant fauna, including colonial rugose corals, Acinophyllum and Heliophyllum; solitary rugose corals, Cystiphylloides and Siphonophrentis; massive tabulate corals, Favosites, Lecfedites, and Emmonsia; branching tabulates, Cladopora, Thamnopora, Syringopora, and Aulopora; and laminar stromatoporoids. Crinoid debris is abundant; brachiopods are sparse. Thin sections from the upper 4 m of the buildup reveal abundant fenestrate and encrusting bryozoans, the latter ocurring in association with crinoid holdfasts. Chert is common throughout the section, but is absent from the Acinophyllum and Cystiphylloides beds. The buildup is overlain by argillaceous, sparsely fossiliferous mudstone of the Clarence Member, characterized by abundant dark chert nodules.
Vertical extent of the buildup cannot be determined exactly, but a thickness of about 10 m is estimated. Estimating lateral extent is even more difficult, due mainly to the tabular nature and lack of "typical" biohermal zonation and distinct flank facies. Although the position of the exposure in relation to the buildup as a whole is known, absence of bioherm facies in the Law quarry suggests the buildup is on the order of 1 km broad.

Large, stabilized sand dunes on right.

Dunes migrating over road surface.

Sugarloaf Hill on right.
This dune rises more than 100 ft above lake level and has been a landmark to Lake Erie travellers since the days of the earliest explorers.

Bridge over drainage canal.

View of Port Colborne's harbor and Welland Canal's port of entry.
The park offers a view of Port Colborne's harbor and the Welland Canal's port of entry. Over 6,600 ships and nearly 800 pleasure craft passed through the canal in 1980. Inco Metals' Company nickel refinery is Port Colbornel's largest employer. Canadian nickel, in Inco-developed alloys, was used in the main engines and other components of the space shuttle Columbia.

STOP 3. Port Colborne East Quarry
Rubble pile on right. Park on concrete pad just beyond. Walk SW into abandoned quarry complex.
No detailed studies of this quarry complex have been published since the days of Stauffer (1915). It was once operated by the Canadian Portland Cement Company and included a large plant, of which only the foundations remain. The quarries were developed on a low, ENE-trending anticline. Telford and Tarrant (1975) mapped only Edgecliff at this locality, however, in places, strata have a distinctively Clarence character _ argillaceous, fine-grained, abundant chert - particularly in the north and west walls. This is probably another manifestation of the interfingering nature of Edgecliff and Clarence facies as described at the Ridgemount quarry. Beds at water level are packstone or grainstone; skeletal material decreases and mud increases upward. The "island" in the southern end of the quarry is a bioherm. Large blocks of light-colored Acinophyllum bafflestone are piled to the east of the island, along the roadway which leads southward into the quarry. Near the island, a railroad trestle crosses a cut which connects the northern quarry with a smaller one south of the tracks. In this area are exposed approximately 4 m of massive bedded, light gray, crinoid grainstone and packstone containing abundant large favositids, common Cystiphylloides, and fewer Thamnopora and Syringopora. These strata have all the aspects of proximal flanks observed in the subsurface bioherms. This stop offers excellent fossil-collecting, either from the rubble piled east of the quarry, or from around the quarry itself. As at the western quarry, glacially-smoothed surfaces provide two-dimensional exposures of the fossil bioherm community.

A3: EURYPTERIDS, STRATIGRAPHY, LATE SILURIAN-EARLY DEVONIAN OF WESTERN NEW YORK STATE AND ONTARIO, CANADA
Samuel J. Ciurca, Jr.
Rochester, New York
The eurypterid horizons of the Bertie Group in New York State (Ciurca, 1973, 1978a) continue into adjacent Ontario, Canada bearing their distinctive eurypterid faunas (Ciurca, 1967a,1976). In addition, Helderbergian strata (Clanbrassil Fm.), between Byng and Haggersville, show the presence of post Bertie-Akron strata in this region in a manner analogous to that of the Honeoye Falls Fm. described for similarly positioned strata discovered south of Rochester, New York (Ciurca, 1967b, 1973).
The purpose of this paper is to present a preliminary account of the stratigraphy and paleontology of this interesting eurypterid-bearing sequence of rocks and to stimulate research into the origin and significance of the waterlimes and associated lithologies in which eurypterids are peculiarly characteristic and abundant.
STRATIGRAPHY AND PALEONTOLOGY
Detailed field studies in New York and Ontario, Canada were undertaken with the hope of providing a better framework for understanding the occurrence and distribution of eurypterid faunas and waterlimes in the regions, and to facilitate correlation. In these studies, the waterlime units have been utilized as the basis of a stratigraphic framework. They have been given an importance similar to that given coal beds in cyclothemic sequences and it is hoped that this will help tracing and understanding of the cyclic sequences present in our Late Silurian-Early Devonian rocks. The distribution of the waterlimes of the Bertie Group, and of the new stratigraphically higher waterlimes, is shown in Figure 2. Heretofore, the only well known waterlime was that of the Williamsville from which much of the eurypterid material in collections was knowingly or unknowingly obtained (i.e. Eurypterus remipes lacustris Fauna).

STOP 1. Dunnville Rock Products, Ltd.
Quarry at Byng, Ontario, Canada. This quarry produces "crushed aggregates-concrete stone, Armour rock for shoreline protection, clay fill".

STOP 2. Port Colborne Quarries, ltd.,
Quarry at Port Colborne just north of Route 3

STOP 3. Ellicott Creek
Ellicott Creek at Wiliamsville, just north of NY 5 (called Glen Park).

A4: GLACIAL GEOLOGY OF THE ERIE LOWLAND AND ADJOINING ALLEGHENY PLATEAU, WESTERN NEW YORK

Niagara Falls morainal ridge on right, Lake Tonawanda plain to left.
Cross Hopkins Rd. with slight rise of Niagara Falls morainal ridge on right, Lake Tonawanda plain to left.

Subdued hillocks of Niagara Falls Moraine
Turn right (south) onto Harris Hill Rd. with subdued hillocks of Niagara Falls Moraine partly mantled by Lake Warren silts. Rise up Onondaga Limestone Escarpment.

Sandy soils on Escarpment edge
Sandy soils on Escarpment edge here result from winnowing of older sediments by Lake Dana waters.

Descend Escarpment into river embayment at Clarence Village.
Recent U.S. Geological Survey borings suggest that a large buried (drift-filled) valley connects the embayment southward with the present valley of Ellicott Creek near Stop 1.

Rise south back up Onondaga Escarpment onto gravel plain
Turn right onto Ransom Rd. Rise south back up Onondaga Escarpment onto gravel plain related to Buffalo Moraine and deposited in Lake Warren III. Beaches of lower stage-Lake Grassmere occur along Escarpment crest.

STOP 1. Pine Hill Gravel Pit.
Pit is cut into a portion of the Buffalo Moraine and is just on north margin of present northwest-flowing Ellicott Creek. Borings made for the study of the gravel aquifer (Fig. 6) in this area show two till sheets with sand and gravel between. This and several adjoining excavations expose the thick sand and gravel units deposited in at least 30 m (100 ft) of Lake Warren III or earlier stage. Thin red lake clay partings separate thick rippled sand units (varves?). The overlying till and sand/gravel unit shows evidence of flow and deformation (often irregularly interfingering). The till, laid down by thin, sometimes bouyant ice margin, can be traced at least to the Alden Moraine ~5 mi to the south. Fabrics show moderate NE-SW maxima.

Drive along crest of subdued sandy beach or offshore bar of Lake Warren III.

Bend right on Peters Corners Rd. onto strong Warren III beach ridge.
This strand can be traced intermittently to Syracuse and south and west through Cleveland into Michigan.

Pit on right excavated in beach ridge.
Pit on right excavated in beach ridge. Cross several beach ridges obliquely.

Alden Moraine at left
Cross R.R. bed cut in Alden Moraine at left (source of beach material) and turn right onto North St. following a Warren III beach (moraine on left).

Cross highest beach ridge of several oblique to Sandridge Rd.

Cross several ridges-spits of Warren III.
Turn right (west) at W. Alden onto Broadway (Rt. 20) and cross several ridges-spits of Warren III. This is the area where Warren III beaches split off northward and Warren I and II? terminate south of Alden Moraine.

Turn left onto Four Rod Rd., still crossing Warren ridges.

Descend into floodplain and cross Cayuga Creek.

Rise across washed till (strand of Lake Warren I - highest Warren)
Rise across washed till (strand of Lake Warren I - highest Warren) at white farmhouse (~860 ft [262 m]) and proceed south across Marilla Moraine. Moraine appears unaltered by Lake Whittlesey waters and hence formed before or soon after draining of Whittlesey to Warren I level.

Cross Clinton St. going south, still on Marille Moraine.

STOP 2. Drainageway Marilla-Hamburg Moraines.
View small esker and associated kames to northeast. To west of intersection, Bullis Rd. crosses delta surface formed in Lake Whittlesey and subsequently Lake Warren by water draining along ice margin here.

Cross Hamburg Moraine

Not good till cut at far left along Little Buffalo Creek.

Moulin kame hillock on right behind farm
Moulin kame hillock on right behind farm consists of till and poorly sorted gravel. A few similar forms occur just to east out of sight.

Go west to stop sign (in E-W-oriented meltwater channel).

Cross Meltwater Channel

Cross Buffalo Creek--its post-glacial position?

Many gravel hillocks of moraine have been removed here.

Note deep cut in moraine.

Deep kettle hole and lake on left
Deep kettle hole and lake on left; hummocky ice-contact drift at distal side of Hamburg Moraine.

East Aurora Waterworks.
This is within partly buried valley of Preglacial Cazenovia River which trends northward through the Hamburg Moraine. Valley fill is major water source and buried valley a collector/ conduit of groundwater.

Note postglacial Cazenovia Creek has been deflected to westward path.

Note U-shaped valley cross-section modified by alluvial fans at margins.

STOP 3. Emery Park (Lunch Stop)
The Gowanda Moraine crosses the valley at this point. The park is on the west wall of the partly buried valley (~60-l00 m of drift till) now occupied by East Branch Cazenovia Creek. Ice flow was approximately parallel to this and adjoining valleys. High level deltas graded to proglacial "finger lakes" line the east valley wall in this general area.

Cross East Branch Cazenovia Creek.
Creek is on bedrock at right, deepest part of valley is to left (east) of bridge. Pass through Village of Holland and rise southward onto proximal side of Lake Escarpment Moraine (bedrock actually fills slightly southward).

Turn right onto Hand Rd. at crest of Lake Escarpment Moraine.

Turn around at Chaffee solid waste disposal site (landfill).
Although tills appear quite thick and dense here, the Chaffee Outwash Plain heads at north margin of the current landfill boundary and critically close to leachate drainage.

Note meltwater channels on right
Note meltwater channels on right leading to head of outwash plain within few tenths of a mile.

Cross Grove St., Chaffee, on outwash plain.
Note irregularly south-sloping surface, probably effected by differential settling. A nearby gas well reached bedrock at about 188 m (615 ft) depth (see Calkin and others, 1974).

Nichols Brook site (Calkin and McAndrews, 1980) on left.

Pass out of Preglacial Cazenovia Valley toward Arcade.

STOP 4. Arcade Section.
The stratigraphy at this active cut-bank of Cattaraugus Creek is shown in Figure 4. The locality is south of the Lake Escarpment Moraine. At least three till units are exposed, separated by glacial lake deposits. The upper till is thin and has textural properties strongly influenced by underlying lacustrine deposits and appears to indicate deposition from thin ice. The lower tills are thicker and generally more homogeneous in their properties although the lowest unit carries clasts of red till and clay. The tills are tentatively correlated with Hiram, Lavery, and Kent drifts on the basis of sequence.

Hesitation Stop - Gernatt Gravel Pit
Good exposure (when working) of Chaffee Outwash at Cattaraugus Creek where it overlies till (generally not exposed but just above creek level). Near-horizontally bedded and very well sorted gravel overlies steeply inclined (foreset) units which on one visit appeared to be associated with till units.

Cross bedrock-cored ridge dividing buried valley into two channels.
Deepest channel is on west side and connects valley to south of Cattaraugus Creek with present valley of East Branch Cazenovia Creek Valley (not with Buffalo Creek [Calkin and others, 1974]).

Descend from outwash surface into Cattaraugus Creek Valley.
Bluemont Ski area to south across creek.

Note slumped till of Lavery Till on right
Note slumped till of Lavery Till on right, Lord Hill Section of LaFleur (1979, 1980) on left at Creek. Strong fluvial dissection exposes till and lake sediments in the valley area.

Rise out of postglacial valley onto outwash
Rise out of postglacial valley onto outwash tied to Springville Outwash Plain. Lake Escarpment morainal ridges are to north.

Descend into spillway that drained pro-glacial lake
At hospital, descend into Village of Springville occupying spillway that drained pro-glacial lake in North Branch Eighteenmile Creek and West Branch Cazenovia Creek. This is center of Preglacial Buttermilk Creek heading several miles to south.

Proceed straight (west) on Rt. 39.
(The most scenic route would trend left via Waverly St. and Zoar-Gowanda Rd. but roads are narrow and steep, and bridge weight limits prohibit bus traverse.)

Leave outwash plain crossing onto distal ridge of Lake Escarpment Moraine.

Cross onto outwash plain
Cross onto outwash plain (still on Rt. 39) at head of South Branch Eighteenmile Creek. Formed by meltwater of Lake Escarpment Moraine shed southward into buried Preglacial Connoisarauley River Valley.

Rise off outwash onto Lake Escarpment Moraine as it trendsN-S.

Cross onto gravel valley till
Cross Rt. 75 at Collins Center and onto gravel valley till (underlain by lake clay and till respectively).

Cross Gowanda Moraine.
Stratigraphic sections suggest moraine formed as ice advanced into proglacial lake.

Clear Creek Valley (part of Preglacial Allegheny Valley)
Turn left (south) onto Rt. 62 within Clear Creek Valley (part of Preglacial Allegheny Valley) and park near corner. Reach exposure downstream from highway bridge 0.3 mi south.

STOP 5. Gowanda Hospital Interstadial Site
This site exposes three till units, a buried paleosol and overlying organic horizon. It is briefly described in the text and Figures 3a, b, and c. The right bank section is rarely exposed but the paleosol and wood horizons on the left bank are often clear after minor work. One of the most important aspects of the site is the Gowanda Paleosol, a buried, truncated (of its A horizon) soil whose substantial development and stratigraphic positioning appears to argue for a long mid-Wisconsin nonglacial interval prior to about 50,000 yr BP (Calkin and others, 1982).
One of the many problems of the stratigraphy is the age and correlation of the brown till unit. The till material appears to be derived locally by glacial erosion of the underlying, weathered red "Collins" till and therefore it is difficult to correlate regionally with other till units. Although it displays mudflow-like contacts with the channel gravel, it also shows good glaciotectonic structures including wood sheared from underlying deposits. The age of the wood suggests a mid-Wisconsin ice advance; however, there is some question whether the ice sheet reached past this area to Titusville, Pennsylvania, in Middle Wisconsin interval as suggested by current correlations (Figs. 2 and 3b).

Rising onto Fairchild's (1932) Asylum Terrace
Turn left (west) onto Richardson Rd. rising onto Fairchild's (1932) Asylum (Gowanda State Hospital) Terrace graded to a local proglacial lake in the Cattaraugus Creek (Preglacial Allegheny) embayment of the Erie Basin. This surface is an extension of top gravel unit (8) at Gowanda Hospital site.

View at left of Fourmile Level, a delta surface
View at left of Fourmile Level, a delta surface (on Cattaraugus Indian Reservation) formed in Lake Whittlesey and later Lake Warren.

Gravel pit at right displays large foreset bedding
Gravel pit at right displays large foreset bedding units in thickened section of Asylum Terrace seen at the Gowanda Hospital site (Fig. 3a, unit 8).

Proceed north with Gowanda Moraine parallel to right.

Zone of weak strand lines
Rt. 62 follows along zone of weak strand lines of Lake Whittlesey and Lake Warren I. Lowland on left is an old buried tributary valley of Allegheny River.

Cross Winter Gulf and organic site on left
Cross Winter Gulf (unofficial name) and organic site on left (Schwert and Morgan, 1980; Calkin and McAndrews, 1981). The section here is diagramed in Figure 5.

Cross gravelly ridges (before low point)
Turn left onto Milestrip Rd. (just south of a "Friends" cemetery built on a delta of Lake Whittlesey). Cross gravelly ridges (before low point) intermediate between Whittlesey and Warren (possibly Arkona?). Note ridge-spit extending from west (on right) graded first to Lake Whittlesey and later modified by Lake Warren waters.

Spit extending eastward is tied to Whittlesey beach
Spit visible (again) extending eastward is tied to well-developed Whittlesey beach (visible on left) which completely encloses bedrock-based high area here (plateau outlier).

Cemetery at intersection spans a Warren ridge.

STOP 6. North Collins, Whittlesey Beach Exposure
The Glacial Lake Whittlesey beach with crest at 850 ft (260 m) here is almost totally composed of shale, eroded from the local bedrock (Calkin, 1970, Fig. 2). The good development of the ridge on this narrow-embayment-side of the island in Lake Whittlesey is of interest. Lake Whittlesey extended southwest beyond Toldeo and into the Huron Basin. Several ridges of Lake Warren occur below the Whittlesey ridge; many have been destroyed by years of farming or construction.

Proceed east (off Whittlesey island)

Rt. 62 follows along Lake Warren beach ridge.
Turn left (north) at Rt. 62 (intersection at North Collins is on delta deposits of Lake Whittlesey). Rt. 62 follows along Lake Warren beach ridge. Lake Whittlesey beach is visible intermittently on incline to right (east), lower Warren ridges to left with deeper water silts and clays.

Whittlesey beach and wave-cut cliff exhumed in old gravel pit at right.

Lake Warren beach ridges exposed in gardens on either side of road.

Cross South Branch Eighteenmile Creek.
This and similar cuts are apparently post-glacial gorges.

View to right (northeast) of wave-cut beach and bluff of Lake Whittlesey.

Cemetery on right and road itself still on Lake Warren beach.

Onondaga Escarpment
Pass under Rt. 5 and through Onondaga Escarpment. Note south dip of strata. This was formerly a prize fossil collecting quarry.

B1: STRATIGRAPHY AND FACIES VARIATION OF THE ROCHESTER SHALE (SILURIAN: CLINTON GROUP) ALONG NIAGARA GORGE
Carlton E. Brett
University of Rochester, Rochester, NY 14627
The linear, east-west configuration of Paleozoic outcrop belts in western New York and Ontario imposes a strong two-dimensionality on our knowledge of the stratigraphy and facies relationships of these rocks. It is frequently assumed that the outcrop sections provide a reasonable transect from near shore clastic-dominated facies in the east to offshore carbonates and marine muds in the west. This view is overly simplistic and it ignores the fact that the Paleozoic epeiric seas had a northern as well as an eastern shoreline (directions based on modern geography). Furthermore, the idea of a simple east-west transect is contradicted by detailed examination of stratigraphy in western New York. Stratigraphic sequences such as the Silurian Clinton, Lockport, or Salina Groups exhibit vertical facies changes, manifest in the gradational contacts between beds, members, or formations. Walther's law predicts that such vertical sequences of litho- and biofacies should mirror arrays of laterally adjacent, contemporaneous facies belts. However, lateral gradation of lithologies is rarely observed along the outcrop belt of western New York. Rather, one observes that thin stratigraphic units representing distinctive facies, are traceable along the strike of the outcrop belt for tens to hundreds of miles (see, for example, Belak, 1980).
This "layer cake" aspect of New York stratigraphy has facilitated local correlation. However, it has also led to a common impression that the strata represent vertical stacking of time parallel facies units in a three dimensional sense, implying basinwide environmental changes. This non-Waltherian view of western New York stratigraphy is probably erroneous and it has greatly hampered attempts to decipher facies relationships and depositional environments. I contend that it is largely an artifact resulting from the east-west trend of the modern outcrop belts.

B1: STRATIGRAPHY AND FACIES VARIATION OF THE ROCHESTER SHALE (SILURIAN: CLINTON GROUP) ALONG NIAGARA GORGE

Begin road cut in Lockport and Rochester formations.

STOP 1. Lockport Junction Roadcut.
Exposure of upper Rochester/DeCew Dolostone contact. Pull vehicles off in parking area on left side of road.
The first two stops of this trip provide an overview of the Rochester Shale in eastern Niagara County, for comparison with Niagara Gorge sections farther west. This exposure illustrates the gradational upper contact of the Rochester Shale with the overlying DeCew dolostone. The upper 3-4 m of the Burleigh Hill Member of the Rochester Shale are exposed at the base of this cut. Nearly barren, friable, calcareous shale grades upward into a 1-2 m interval of interbedded dolomitic shale and buff weathering, burrow-mottled layers of argillaceous laminated calcisiltite. These beds appear to be gradational into the overlying DeCew Dolostone. This transitional upper Rochester unit thickens eastward to form the Gates Member which is recognized near the type section at Rochester, New York. The upper portion of the roadcut exposes an excellent section of the Gasport Formation (Lockport Group) and the sharp contact between the DeCew dolostone and the cross-bedded, crinoidal biosparites of the Gasport.
The uppermost Rochester and DeCew are interpreted as rapidly-deposited carbonate silt and clay sediments, winnowed from Gasport crinoidal shoals which lay nearby to the northwest. Cross lamination and abundant soft sediment deformation in the OeCew suggest rapid influx of sediment followed by dewatering. Body fossils are exceedingly rare in the upper Rochester and the DeCew, but burrows, including Chondrites, Planolites and Teichichnus are abundant. This may,again,reflect high turbidity.

Small exposure of Gasport Limestone.

STOP 2. Thrall Roadcut, Cambria, New York.
High cutbank in Rochester Shale and Lockport Group, in pasture along south side of Thrall Road. Park vehicles on right hand side of road, in front of driveway to farm.
Although somewhat weathered,this exposure provides a good reference section for the middle Rochester Shale in eastern Niagara County. Here the upper 4 or 5 m of the Lewiston Member, and its sharp contact with the overlying Burleigh Hill are exposed. Although largely covered by slumped talus, limestone ledges of Lewiston submember E ("bryozoa beds" of Grabau, 1901) protrude from the bank in several locations. This is an excellent locality for collecting the diverse fauna of middle Rochester beds. Weathered talus at the base of the slope has yielded over 20 species of brachiopods. corals, gastropods and complete thecae and crowns of Stephanocrinus, Caryocrinites, and various crinoids. Weathered slabs of limestone replete with ramos and fenestrate bryozoans are abundant here. Note the sharp contrast with the overlying barren mudstone of the Burleigh Hill Member. Thin calcisiltites comprise the only interbeds in this upper portion of the Rochester. Weathered slabs from the upper bank have yielded abundant trilobite remains (Dalmanites, Trimerus), ostracodes, Tentaculites and crinoid columnals. However, the bulk of the interbedded shale is very sparsely fossiliferous, in marked contrast to the underlying Lewiston beds. The top of this section is again capped by buff weathering DeCew Dolostone and Gasport Limestone.

We are now riding along the base of Niagara Escarpment.

Proceed up low ridge on Irondequoit Limestone
Proceed up low ridge formed by lower platform of Niagara Escarpment on Irondequoit Limestone.

STOP 3. Baer Roadcut.
Roadcut in Rockway and Irondequoit Limestones. Park near south end of cut.
There are very few outcrops in Niagara County where the basal beds of the Rochester Shale can be examined. This will be a brief stop to observe the uppermost Irondequoit Limestone which immediately underlies the Lewiston Member. Here the Irondequoit is a crinoidal biosparite, similar to the Gasport Limestone. Well-preserved fossils occur sparingly in the upper Irondequoit, including thecae of Stephanocrinus, Caryocrinites and other echinoderms. Small, white-weathering bioherms composed of fistuliporoid bryozoans and bound biomicrite occur near the top of this exposure. Such small bioherms occasionally protrude upward into the basal beds of the Rochester Shale.
Continue southward along Baer Road crossing the small plateau on Irondequoit Limestone and then up the main Niagara Escarpment.

Small exposure of Gasport Limestone at turn in road.

The classic Pekin roadcut through a Gasport bioherm
The classic Pekin roadcut through a Gasport bioherm is exposed along 429 immediately below Upper Mountain Road at this locality.

Excellent view off Niagara Escarpment onto Ontario Lowlands Plain.
On clear days this affords a view of Lake Ontario.

View to right out to Ontario Lowlands Plain and Lake Ontario.

Reservoir for Robert Moses Hydroelectric Plant appears as bank on left.

STOP 4. North End, Niagara Gorge Near Lewiston, New York.
Pull off on broad shoulder of Robert Moses Parkway and park at 55 mph sign. Passengers will disembark here, proceed over guard rail and down a slope, bearing to the right or north to cliffs along Niagara Gorge (see Fig. 7 point A).
Cliffs along the east face of Niagara Gorge between Lewiston Queenston Bridge and the Robert Moses Power Plant provide an excellent section of the entire Irondequoit, Rochester, and lower Lockport units. Here the Rochester Shale is approximately 17 m thick; the lower half comprises the Lewiston Member which consists of about 8.7 m (28.6 ft) of medium to brownish gray calcareous shaley mudstone with interbedded thin carbonates. The member exhibits a gradational lower contact with Irondequoit Limestone, but is sharply differentiated from the overlying Burleigh Hill Member at the top of a 1-2 m interval of bryozoan rich limestones (unit E). As at most localities in western New York and adjacent Ontario the Lewiston Member can be subdivided into six informal units or submembers designated by letters A-E. All of these beds are readily accessible in this cliff section and will be described as follows:
A) The basal transition zone of the Lewiston is up to 1 m thick and consists of dark-brownish to ashy-gray, silty, very calcareous and fossiliferous mudstone with interbeds of argillaceous limestone (biomicrite and/or biosparite). Brachiopods are very abundant and may be packed into layers; characteristic species include: Atrypa reticularis, large Leptaena rhomboidalis, Whitfieldella oblata and Plectodonta transversalisalis. Bryozoans are less common than in overlying beds, but laminar fistuliporoids are not uncommon. Echinodenn debris is abundant in the lower shales and unit A has yielded certain unique forms including a high, narrow morph of Stephanocrinus anulatus, large Eudalyptocrinites and the very rare crinoid Paracolocrinus (Brett, 1978).
Locally, small bioherms 1-5 m across and up to 2 m high protrude upward from the Irondequoit Limestone into the base of the Rochester shale (Sarle, 1901). These mounds are composed of whitish to massive micritic limestone with abundant laminar fistuliporoid bryozoans. A particularly good example of one of these mounds, now inaccessible, but readily visible, occurs along the high wall of Irondequoit Limestone immediately south of this Rochester Shale outcrop. This mound appears to interfinger laterally with shales of unit A; however, it al so contains pockets filled with a greenish clay shale, unlike the basal Rochester. Bioherms such as this have yielded a number of unique fossils not seen elsewhere in the Rochester Shale. Large Bumastus and Calymene trilobites, sometimes as coquinites of cephalic and pygidial shields occur in shaley pockets within the biohenns. Unit A clearly exhibits features transitional between typical Irondequoit Limestone and Rochester Shale.
B) The lower beds of the Rochester Shale grade upward into a 2.5 - 3m interval of softer, less calcareous, medium to brownish-gray mudstone with numerous lenticular beds of bryozoan rich biomicrites. As a whole, this interval is richly fossiliferus; although some mudstone beds are nearly barren. Ramose bryozoans are particularly characteristic and they frequently occur in clusters packed in a mudstone matrix. Assocciated with these clusters are abundant brachiopods such as Atrypa reticularis, small Leptaena, and Whitfieldella. This interval is particularly notable for the abundance of ecinoderm remains including thecae of the blastoid-like pelmatozoan Stephanocrinus angulatus, and the rhombiferan cystoid Caryocrinites ornatus, both of which are typiclly associated with bryozoan-rich patches. Holdfasts of Caryocrinites are commonly found cemented to brozoans. Gastropods, the trilobites Bumastus, Arctinurus, Dalmanites and others are also abundant in these beds. Certain limestone lenses in unit B appear to represent starved ripples of storm-concentrated, skeletal debris. rotated geopetal structures and infillings of brachiopod shells with matrix identical to that of the underlying beds suggest derivation of these fossils by reworking during storms.
C) Near the north end of Niagara Gorge the middle interval of the Lewiston Member consists of about 3-4 m of sparsely fossiliferous gray shales and interbedded dark-gray, burrowed, laminated calcisiltites (pelmicrites). Bryozoan clusters and biomicritic limestones are absent from this interval. These shales exhlblt a low diversity fauna dominated by the brachiopods Striispirifer, Strophonella and Parmorthis and the trilobites Dalmanites, Trimerus and Arctinurus. Near the base of unit C occur thin horizons which locally contain exceptionally well-preserved fossils. These layers, in all about 10-20 cm thick, were designated the Homocrinus band at Lockport, New York (Ringueberg, 1888); they contain the characteristic minute inadunate crinoid Homocrinus parvus, as well as completely articulated specimens of Asaphocrinus and Macrostylocrinus, the cystoid Caryocrinites, edrioasteroids and rare starfish. These fossils are associated with dense bedding plane assemblages of Striispirifer and other brachiopods. Such assemblages suggest rapid smothering of the sea floor by muds, producing catastrophic (live) burial of benthic communities by storm-generated mud layers (Brett, 1978; 1980)
Homocrinus-bearing layers have been recognized at Niagara Gorge about 4.6 m (15 ft) above the base of the Lewiston Member. However, no large assemblages have as yet been obtained from this locality. Calcisiltites of Lewiston C also appear to record a type of storm-generated layer. These units form thin (1-2 cm) persistent bands. Weathered surfaces reveal fine plana- and hummocky- cross lamination, often in alternating sets. Their upper surfaces may be rippled and basal contacts are invariably sharp. The undersurfaces of some calcisiltites yield abundant sole marks including flute and groove molds which suggest current scouring of cohesive muds; occasionally, well-preserved fossils may also occur on the undersides of these beds. Most calcisiltites are barren of body fossils, but they contain abundant trace fossils including large vertical shafts - possibly escape burrows - and post-depositional mining structures such as Chondrites and Planolites.
Rochester calcisiltites closely resemble storm silt layers described by Reineck and Singh (1972), from the modern North Sea and by Kreisa (1981) from the Ordovician Martinsburg Formation. They are interpreted as deposits from storm-generated density currents which transported carbonate silts from shallow platform areas into the Rochester depositional basin.
D) Overlying unit C is an interval, up to 2 m thick, of fossiliferous mudstone with biomicrites which closely resemble unit B, both in lithology and fauna. Again, clusters of ramose bryozoan are abundant and exhibit virtually all of the associated fauna found within the lower unit B. These beds, again, yield abundant atrypids and Whitfieldella, Striispirifer, Leptaena, Bumastus trilobites, dendroid graptolites and the pelmatozoans Stephanocrinus angulatus and Caryocrinites. Lenticular calcarenites resembllng those in unit B become increasingly abundant upward in unit D whereas barren calcisiltites are less frequent than in unit c.
E) "Bryozoa beds." The top of the Lewiston Member is marked by a series of thin lenticular limestones (biomicrites and biosparites) interbedded with soft, gray, fossiliferous shale. Grabau (1901) termed this unit the "bryozoa beds," because of the great abundance of ramose and fenestrate bryozoans which constitute a bulk of the thin limestones. Brachiopods and echinoderms are also abundant in these beds although typically disarticulated and fragmented. Notable is the reappearance of a large, slender morphotype of Stephanocrinus seen also in unit A at the base of the Rochester Shale.
The uppermost bed of unit E is generally somewhat thicker and more continuous than the underlying layers and may be richer in brachiopod valves and crinoidal debris, resembling the uppermost layers of the Irondequoit Limestone. This unit marks the top of the Lewiston Member in nearly all localities. Locally, this topmost limestone bed is glauconitic and contains shale intraclasts, evidently derived by erosion from the underlying beds.
At this locality, as in most areas of western new York, the Lewiston Member is abruptly overlain by medium to dark gray platey and calcareous shale of the Burleigh Hill Member, named for exposures along Burleigh Hill Drive in St. Catharines, Ontario (Brett, in press). In the north end of Niagara Gorge the Burleigh Hill is about 10 m thick. However, as will be noted, this unit thins rapidly southward along Niagara Gorge. The basal 4-5 m of the member are sparsely fossiliferus to nearly barren, laminated and platey shales which weather into elongate slabs. Lithologically and faunally this portion of the Burleigh Hill Member most closely resembles unit C of the Lewiston Member, and, as with the latter unit, these shales contain occasional thin, laminated calcisiltites which increase in frequency upward. No bryozoan biomicrites have been observed in the Burleigh Hill Memeber at any locality in western New York and bryozoans are generally absent. Near the base of the Burleigh Hill are a few thin shell layers composed chiefly of the brachipods Fardenia, Parmorthis, and Strophonella as well as trilobite fragments.
The upper half of the Burleigh Hill Member is gradational into the overlying DeCew Dolostone. Bands of calcisiltite become more closely spaced and eventually merge into a silty dolomitic shale near the top. A few thin layers near the top of the Burleigh Hill have yielded local patches of well-preserved crinoids including Dimerocrinities and Dendrocrinus as well as brachiopods and other fossils. Burleigh Hill dolomitic shales appear to pass upward gradationally into the overlying DeCew Dolostone Formation. Unlike the Lewiston member, which appears to represent a subsymmetrical cycle, Burleigh Hll reflects a shallowing-upward hemicycle.

Route Revision
2011: The Robert Moses Parkway has been interrupted and modified, so the route in the Guidebook is no longer possible. However, it is now possible to make left turns off of the Parkway... OHM

Goat Island Dolostone
Small exposures of Goat Island Dolostone of the Lockport Group in the roadcut.

STOP 5. Niagara Sewage Pumping Station.
Proceed on foot down old access road to Niagara sewage pumping station in the Gorge. Note well-exposed bioherm in the Gasport Limestone along roadcut.
This stop illustrates the contrast between northern and southern sections of Rochester Shale in the Niagara Gorge. A large artificial cut behind the new sewage pumping building exposes the upper portion of the Lewiston and the entire Burleigh Hill Members of the Rochester Shale. At this location in the gorge the Lewiston Member is approximately 12.5 m (41 ft) thick; the majority of this thickness consists of unfossiliferous shales of a greatly thickened submember C9 here about 11 m (36 ft) thick in contrast to 3.6 to 4 m (11-14 ft) at Stop 4. The upper portion of this unit, visible at the base of the cut, consists of nearly barren, silty shale with one or two thin calcisiltite bands. The fossil-rich submember D is not recognizable at this locality; its position appears to be occupied by a section of interbedded shales and thin (5-10 cm) calcisiltite bands. Four or five prominent ledge-forming dolomitic calcisiltites occur near the center of the outcrop, apparently representing the lateral equivalent of "bryozoa beds" (submember E). These bands exhibit sedimentary structures including hummocky cross lamination, rippled upper surfaces, and sharp, scoured basal surfaces, suggestive of current deposition of fine carbonate silt. The beds are interpreted as layers derived from winnowing of bryozoan-crinoid shoals which existed to the north (e.g. at the northern of Niagara Gorge). Ripple- and cross-bed orientation suggest southerly current transport of sediments.
Immediately overlying the highest dolomitic band are 1 or 2 thin layers of coarse, rusty weathering biosparite containing an abundance of brachiopods, pelmatozoans and some bryozoan debris, interbedded with slightly fossiliferous shales. These are essentially the only fossil-rich beds in the entire outcrop and they appear to represent a southern vestige of the topmost bed of unit E in the north. Two km to the north the Whirlpool State Park these bands thicken into a 10-20 cm thick interval of fossil debris and the underlying dolomitic calcisiltites interfinger with typical bryozoan-bearing beds indicating a clearcut transition from typical biosparites of unit E, to the dolostones seen at this locality. The upper bed of fossil debris is followed abruptly by barren shales of the Burleigh Hill Member, which closely resemble those of unit C. The Burleigh Hill is about 6 m thick and displays a sharp, probably erosional, upper contact with the DeCew Dolostone.
This sparsely fossiliferous section stands in striking contrast to sections just a few miles north. It suggests the presence of a fairly abrupt, southward dipping paleoslope.

STOP 6. Ontario Hydro Access Road Cut.
Pass circle at Maid of the Mist information building. Pull off bus along the river road here and park. Proceed on foot to access road for Ontario Hydro Niagara Plant, and Maid of the Mist launch area. Note excellent exposures of Lockport Group beginning at the top of the roadcut with Eramosa Dolostone, followed below by the vuggy stromatolitic and stromatoporoid-bearing Goat Island Dolostone and the dolomitic crinoidal limestone of the Gasport Formation; this unit, in turn, is underlain by buff-weathering, sugary-textured, DeCew Dolostone, exhibiting prominent soft sediment deformation ("enterolithic structure"). The access road forks into two branches, one leading to the straight ahead to the Ontario Hydro Plant, and the other, left hand fork leads to the Maid of the Mist launch area. Near the fork are exposures of the upper part of the Rochester Shale.
This roadcut provides one of the southernmost exposures of the Rochester Shale in New York State. Here the upper contact of the formation is well exposed, just north of the fork in the road. The buff-weathering enterolithic DeCew Dolostone rests with sharp, wavy, and apparently channeled contact on the barren shales of the middle Burleigh Hill Member. No transitional interval is observed at this locality and the Burleigh Hill is only about 4.7 m thick. This situation contrasts with the gradational upper contact of the Rochester Shale observed in most western New York localities. It suggests that the upper Burleigh Hill beds have been removed, possibly by downslope erosional truncation, prior to DeCew carbonate silt deposition. The prominent enterolithic structure of the DeCew Dolostone has long been noted and may have resulted from downslope slumping of rapidly deposited carbonate sediments.

B2: GLACIAL AND ENGINEERING GEOLOGY ASPECTS OF THE NIAGARA FALLS AND GORGE
Parker E. Calkin
Buffalo, NY 14214
Thomas A. Wilkinson
U.S. Army Corps of Engineers
Buffalo District, Buffalo, NY 14207
The Niagara River separating Canada and the United States (Frontispiece II) is unusual as compared to other rivers. for its (a) short length and (b) discharge stability due to the immense storage capacity of its drainage basin. It is largely supplied by the excess discharge brought into Lake Erie from Lakes Superior, Michigan and Huron. In addition to their stabilizing effect, the Great Lakes trap most of the basin sediment so that the river is essentially sedimentfree (Philbrick, 1970). From its mouth at the north end of Lake Erie at 174.4 m (572 ft) the Niagara descends 23.3 m (73 ft) to the brink of the Falls, drops vertically 51 m (167 ft) (Fig. I), and then descends another 22.6 m (74 ft) in gorge to Lake Ontario at 753m (246 ft). The mean natural flow is about 5,721 m3 sec-l (202,000 ft3 sec-1), and can be increased temporarily by as much as 50 percent due to water surface set up during storms along Lake Erie. However, it is otherwise very stable. Since about 1905, the flow over the Falls itself has been markedly limited by water diversion for hydroelectric power generation. Presently it carries 50 percent of the river's natural flow or about 2,800 m3 sec-l (1003000 ft3 sec-1) during tourist hours and only about 25 percent (1,400 m3 sec-l /50,000 ft3 sec-1) at other times. About 92 percent of undiverted flow passes over the Horseshoe Falls, 8 percent over the American Falls, and this percentage may have been the average even under precontrol discharges (American Falls International Board, 1974).
The differences in elevation that cause the Falls is related to the presence of the Niagara cuesta (escarpment) that divides the Erie and Ontario basins (Frontispiece I and II). The canyon (gorge) of the Niagara has been cut southward from this escarpment into a section of jointed, gently south-dipping sedimentary rocks capped by the tough Lockport dolostone. The stratigraphy is considered in detail in a subsequent section of this paper and in Brett (1982, this volume).
The modern Niagara River was initiated as a multi-outlet river-lake system following the last retreat of the Last Winconsin ice sheet; the cutting of its deep incised gorge through time is related in various degrees to the changes in drainage controlled by this ice retreat. The ancestral development culminating with a more detailed chronology for development of the Upper Great Gorge is the initial subject of this paper. The second part considers details of the geology in the present area of the Falls and the geologic processes that control stability as well as retreat of the Falls and Gorge as they are revealed in the context of major engineering projects undertaken principally along the east (American) side of the Niagara Gorge. A third section considers the future of the Falls.

B2: GLACIAL AND ENGINEERING GEOLOGY ASPECTS OF THE NIAGARA FALLS AND GORGE

Travel over glacial Lake Warren plain
Travel over glacial Lake Warren plain with red clay colored by Queenston Shale. We are also at south margin of Lake Tonawanda plain.

Subdued topography
Subdued topography due to subaqueous deposition in Lake Warren and washing by initial stages of Niagara River System.

Note spray of Falls at Left.

Structures at left house gates for water intakes to Robert Moses Niagara Power Plant.

Niagara Falls Sewage Treatment Plant on right
Pass Carborundum Company and Niagara Falls Sewage Treatment Plant on right, Grass Island Pool and control structure (mostly on Canadian side) on distant left.

STOP 1. Goat Island
The Horseshoe Falls is seen between emerged bedrock terraces of the ancestral river. The Niagara Falls Moraine forms the bluff behind the Falls on the Canadian Side. The bedrock slopes which form the Horseshoe and American Rapids are connected beneath Goat Island, at this site, and represent the eastern bank of Spencer's (1907) "pre-glacial Falls-Chippewa Valley." This was believed to trend southward from headwater 2 Km (1.2 mi) to the north (near head of north-trending St. Davids Gorge). Figure 3a shows the surficial deposits on Goat Island.
The stratigraphy, structure, talus accumulation, and general location of previous rockfalls at the American Falls will be observed at this stop.

STOP 2. Schoellkopf Geological Museum
This is the site of the massive rockfall that destroyed the Schoellkopf Powerhouse Stations 3B and 3C and damaged 3A on June 7, 1956. This area of failure will be observed and described.

STOP 3. Whirlpool Park
Descend from the parking lot a series of bedrock or gravel river terraces to Gorge margin and view of Whirlpool. The Whirlpool formed soon after 9800 yr 13P when the retreating Falls intersected the buried St. Davids Gorge (see Figs. 1, 2, 3b). Known since the time of James Holland and Charles Lyell, this gorge is as deep and nearly as wide as the Upper Great Gorge (Hobson and Terasmae, 1969), and extends northward across the Escarpment at the community of St. Davids, Ontario, to the mouth of the Niagara at Niagara-On-The-Lake. Taylor (1933) showed that it probably reached as far south (upstream) as the Railroad Bridge where till was encountered in the Gorge bottom and probably up to the head of the Whirlpool Rapids section (Fig. 1). The age and nature of the drift fill (Fig. 2) suggest cutting occurred during or more probably before Middle Wisconsin time under nonglacial conditions when river discharges and base-level conditions were similar to those of the present.
The Gorge walls expose Lockport Dolostone down through Lower Silurian, Whirlpool Sandstone (type area).

STOP 4. Devils Hole
This is a plunge pool formed by drainage from Lake Tonawanda via a shallow channel east of the main Niagara channel (Fig. 1). The cave has enlarged through solution localized along a master joint. This site is a good one for viewing the stratigraphy and structure of the Lockport Formation.
Bloody Run, the stream now occupying the lower end of this channel, is named after an Indian massacre of settlers which is reported to have occurred here in 1763.

STOP 5. Robert Moses Niagara Power Plant
A brief stop at this plant will be made to observe the limited exposures of rock excavation surface. The Power Vista itself displays models of Niagara Falls and Gorge, the power generating plant setup and in addition, views of the Gorge stratigraphy. Elevator service to the base of the Power Plant Access Road (traversing good exposures of the Queenston through the Lockport formations) may be obtained for geology field trips with special permission.

Cross Barre Moraine at crest of Niagara Escarpment
Cross Barre Moraine at crest of Niagara Escarpment with view of lake Iroquois plain to north.
Descend Escarpment; note meandering lower Niagara River with drop of less than 1 m in 6 mi (9 Km) distance to lake Ontario.

Rt. 104 E here follows crest of wave-cut bluff
Rt. 104 E here follows crest of wave-cut bluff of lake Iroquois with thin lacustrine silts on till. Niagara Escarpment at right.

Rt. 104 starts to follow crest of Lake Iroquois beach ridge.

A second ridge occurs to North
A second ridge occurs to North (North Ridge spit) probably derived from the lockport spillway to the east.

Enter bedrock embayment of lockport spillway system for lake Tonawanda.

Turn left up Escarpment on East Jackson St.
The lockport Wastewater Treatment Plant on right is lockport Gulf site of Calkin and Brett (1978) and Miller and Morgan (1982). Subsurface exposure of the lockport Gulf site have revealed the following stratigraphy:
Top 0.5 m | Fill
2.5 m | Massive silty clay (post glacial)
2.0 m | Gray organic silt, clay, and marl with pollen dominated by spruce; basal wood date of 10,920+ 160 yr BP (1-5841)
3.5 m | Laminated red and gray sand, silt, and clay (Lake Iroquois?)
Base 9.0 m | Red clayey sand and gravel interpreted to be till (only in borings)
East Jackson St. follows one of the three major spillway channels at Lockport.

Kame deposits are related to Albion-Rochester Moraine.

STOP 6. Outwater Park, Lockport
View northward from Lockport Escarpment of Lake Iroquois plain and Lake Ontario (if clear) 11 mi. distant. The Lockport Gulf (W. Jackson St.) spillway circles just below. Good exposures of the bedrock surface and northeast-southwest oriented striations occur in the park dump area to the west of the water tank.

Cross High Street on crest of Barre Moraine ridge.

Another of four Barre Moraine ridges
Cross Summit Street at light, another of four Barre Moraine ridges mapped by Gilbert (Kindle and Taylor, 1913).

You are in middle of the former River -- Lake Tonawanda plain.
You are in middle of the former River -- Lake Tonawanda plain. A few low NE-SW-oriented drumlins can be seen to the northeast.

B3: QUATERNARY STRATIGRAPHY AND BLUFF EROSION WESTERN LAKE ONTARIO, NEW YORK
PARKER E. CALKIN Department of Geological Sciences
Buffalo, New York 14226
ERNEST H. MULLER*
Syracuse University
Syracuse, New York 13210
THOMAS F. DREXHAGE*
Acres American Inc.
Liberty Bank Building
Buffalo, New York 14202
Wave-steepened bluffs along the south coast of Lake Ontario display the most continuous and some of the most interesting exposures of glacial drift in New York. Study of these bluffs provides detail of local and regional Pleistocene history, as well as insight into mechanisms of glacio-lacustrine sedimentation. In addition, knowledge of the composition, structure and correlation of bluff materials is fundamental to interpretation of rates and modes of coastal recession and sediment contribution to the lake basin. Wave and subaerial erosion of these bluffs has been particularly severe because bedrock comprises a very small part of the bluff sections.
Record, or near-record high lake levels between 1972 and 1978 greatly accelerated bluff recession and provided the stimulus for a Sea Grant study at SUNY Buffalo of more than 400 km (250 mi) of Lake Ontario coast in New York (Drexhage and Calkin, 1981).
In this guide book we focus on 1) the geologic setting, composition and stratigraphy of the bluffs west of Rochester (Fig. 1); 2) the historic rates and distribution of bluff recession and sediment loading to the lake along this same reach of coast; and 3) some of the factors that influence local differences in recession rates.
Much of the data on bluff recession in this report is from the comprehensive study of historic recession along the whole coast in New York (Drexhage and Calkin, 1981), as well as more local studies (Fortune and Calkin, 1981; Brennan and Calkin, in press). A comprehensive account of the Lake Ontario bluff stratigraphy in New York will be published elsewhere (P.E.Calkin and E.H.Muller, in prep.), but preliminary accounts have been presented by Calkin and Brennan (1976) and Calkin and others (1978).
Basic field measurements and sampling for the stratigraphic study were undertaken during the summers of 1974 and 1975 when Lake Ontario levels were, at times, as much as 1.5 ft (0.45 m) above the 1OO-year monthly averages which range from 245 to 246.6 ft (74.68 to 74.86 m), respectively. Bluff sections were measured at least every kilometer. Attempts were made to trace stratigraphic units continuously along the coast. In this guide, the same station numbers are used for location on Figures 5 through 25 and are referred to in the text without figure numbers and usually within parentheses.
* Field trip leaders

B3: QUATERNARY STRATIGRAPHY AND BLUFF EROSION WESTERN LAKE ONTARIO, NEW YORK

STOP 1. Terrapin Point, Goat Island, Niagara Falls.
We will take time only for photographs. See Calkin and Wilkinson (this volume, Stop 1) for details.

STOP 2. Whirlpool State Park.
This again is only a photostop. See Calkin and Wilkinson (this volume, Stop 3) for details.

Cross Barre Moraine at crest of Niagara Escarpment
Cross Barre Moraine at Country Club atop the Niagara Escarpment. View north of Lake Ontario (if clear) across Lake Iroquois plain in foreground below Escarpment.

Descend Escarpment.

Proceed north onto Iroquois lake plain
Pass under Route 104 across wave-formed bluff and strand of Lake Iroquois. Proceed north onto Iroquois lake plain on Route 18.

View Lake Ontario and bluff
View Lake Ontario and bluff at 23 (Fig. 7). Nearshore gradient is about 8.6 m/km; both short and long-term recession average under 30 cm/yr. (Drexhage and Calkin, 1981).

STOP 3. Roosevelt Beach.
Park at boat ramp site enclosed by storm fence and gate. You are 100 m east of Station 34.
The bluff stratigraphy as exposed in 1975 was:
Top 0.5 m | Fill
2.5 m | Massive silty clay (post glacial)
2.0 m | Gray organic silt, clay, and marl with pollen dominated by spruce; basal wood date of 10,920+ 160 yr BP (1-5841)
3.5 m | Laminated red and gray sand, silt, and clay (Lake Iroquois?)
Base 9.0 m | Red clayey sand and gravel interpreted to be till (only in borings)
Approximately 1200 m to the west, the lower compact till is separated from the overlying till by a stone pavement. Gilbert (1898) described a well developed stone pavement exposed in shore bluffs for a half mile east of the mouth of Tuscarora Bay. Marked parallelism of striae on the flat upper surface of 10 of these boulders indicated deposition of the upper till to have been by ice flowing S50W. He interpreted the stone pavement as distinguishing two tills. An alternative explanation recognizes the upper till as a subaqueous allo-till facies; the lower till as lodgement facies representing the same glaciation.
The highest bluff recession rates in Niagara County are measured at Roosevelt Beach (Drexhage and Calkin, 1981). Between 1938 and 1951 the bluff receded at an average rate of 2.1 ft/yr. Prior to 1902, Twelvemile Creek entered Lake Ontario through Tuscarora Bay. In 1902, the receding shore bluffs breached the left bank of Twelvemi1e Creek. Subsequent sedimentation has built a barrier across the former channel, isolating the mouth of Twelvemile Creek from that of its East Branch and tying the "Island" east of the State Park to the mainland. (See also Brennan, 1979, Fic. 13, Stn. 11, pp 36-37, and Fortune and Calkin, 1981.)

Note elongate, northeast-trending ridge at right.
Note elongate, northeast-trending ridge at right. This is the general trend of ground moraine ridges in this part of the lake plain. Though very subdued, this grain controls orientation of minor drainage lines. In part, at least, it is considered to reflect fluting of underlying bedrock by glacial erosion.

STOP 4. Olcott Bluffs.
Located between Stations 56 and 57 (Fig. 11). This is the eastern edge of a somewhat uneven silt-topped sand plain that stretches along the coast from Olcott and inland at least one mile to a low ridge, 10 to 20 ft. high and correlable with the Carlton Moraine. Ice-contact features have not been recognized in the thick cross-bedded, subaqueous sands, but their occurrence above abnormally thick clay-silt rhythmites and below fine silt suggests ice marginal oscillation. Figure 26 shows the section as measured 1 km to the west. Seeps near base of the stratified drift induce mass wasting which now largely obscures stratigraphic relationships at this site. Queenston bedrock crops out at bases of bluffs on headlands adjoining this stretch of shoreline. Bluff recession less than 30 cm/yr.

STOP 5. Somerset Bluffs.
Located between Stations 60 and 61. In 1974, the wave-eroded bluffs here recorded two tills, a red stony till overlain by purplish-gray silty till. This section is also revealed in borings for the facility. The following section was measured in 1975:
Top | 0.4 m | Lake clay, silty, oxidized
| 0.55 m | Lake silt, yellow; contains convoluted beds and dropstones.
| 1.1 m | Till, interbedded yellow sand, locally gravelly; subaqueous allo-till (?)
| 2.1 m | Till, purple-red, 10% stones, compact. lodgement and subaqueous till.
| 0.5 m | Queenston bedrock

STOP 6. Thirty Mile Point
This is Station 75 (Fig. 16). Bedrock reaches its greatest elevation above lake level in shorebluff of the south coast of Lake Ontario at Thirty Mile Point. Lake silts and sandy silt till overlie some 3 to 4 m of Queenston bedrock.
Of particular interest is the small, fractured bedrock anticline with northwest-southeast trend paralleling the coastline. As described by Gilbert (1899), the crest was broken by a steeply northeasterly dipping fracture, the northeast side displaced upward 2m with overturning of fold axis to the southwest, enclosing till. Although continuing below lake level, the deformation seems to die out downward. Evidence suggests glaciotectonic thrusting by southwesterly moving ice following initial till deposition (Kindle and Taylor, 1913).
Gilbert wrote "Should this description rouse enough interest to induce others to examine the locality, their visits should not be long delayed. This part of the coast is specially exposed to the attack of storm waves and is rapidly beaten back." Eighty years later, however, the exposure appears much as illustrated by Gilbert with apparent bluff recession of no more than 2-3 m in that interval.

Carlton Moraine trending parallel to route.
Note very gently hummocky topography of Carlton Moraine trending parallel to route.

Orchard Creek has been incised deeply into bedrock
Orchard Creek has been incised deeply into bedrock by early postglacial stream erosion. Like other creeks on this south coast of Lake Ontario, its gradient has been diminished and its debouchment into Lake Ontario drowned by postglacial tilting. Shore bluff retreat partly counters the estuary development that tilting has produced.

STOP 7. Brighton Cliff.
Bouldery to sandy supraglacial drift correlated with ridges of the Carlton Moraine 1 to 2 mi south. Underlying weakly bedded till overlies compact till similar to the main till unit of the Niagara River to Rochester reach of the Ontario coastline. The stratigraphy in the bluff is depicted in Figure 27 from Brennan (1979)."At the top of the till, a deformed boulder layer lies on a distinct erosion surface; above the boulder layer pebbly sand grades upwards to fine sand and silt". (Brennan, 1979, p. 47). Pods of till within the sand and small-scale normal faults further suggest ice contact deposition. Features like the fault in Figure 27b may represent deformation during the Carlton glaciation.

Carlton Moraine
Proceed through type area of Carlton Moraine at the railroad tracks.

Cross Lake Iroquois beach ridge

Pass over Albion Moraine

Cross esker

Note esker ridge angling obliquely toward road.

Bear right at fork onto Kams Road and along esker ridge.

Turn right onto Maple Street across the Burma Woods kames.

STOP 8. Burma Woods Esker/Kame Complex.
The extensive area of glacier disintegration topography traversed for the past three miles developed during wastage of the glacier front from the Barre Moraine, about .5 miles south of this point. The stagnating ice margin apparently fronted on Lake Lundy (Lake Dana (?)) at a stage when it was too shallow to float large ice bergs. The Burma Woods Esker can be readily traced for 4 mi (6.4 km ) and conceivably extends all the way to the Albion Moraine, making it perhaps the longest esker in western New York. It consists of a number of discrete segments, the last to be deposited being at the north end. One of the segments terminates in a kame delta at about 735 ft. suggesting the level of Lake Lundy into which it was deposited. Distinct deltaic foreset bedding can be observed in this pit. See Figure 28 for location.

This is the frontal ridge of the Barre Moraine.
Turn left onto Hemlock Ridge Road. This is the frontal ridge of the Barre Moraine. Proceed east through West Barre on Root Road (continuation of Hemlock Ridge Road) and cross lake flats with several closely spaced drumlin ridges oriented northeast-southwest.

Cross eastern end of Oak Orchard Creek headwaters
Cross eastern end of Oak Orchard Creek headwaters and surrounding swamp, as well as several southwest-oriented drumlins.

Elba -- the "onion capital of N.Y.S."

Cross Onondaga Escarpment
Cross Onondaga Escarpment and rise onto Onondaga Bench. The Batavia Moraine crosses Route 98 at top of the scarp.

Gravel kame topography
Gravel kame topography correlated with the Buffalo Moraine trends northwest away from Thruway on right.

Cross through partly quarried-out kames
Cross through partly quarried-out kames related to the Buffalo Moraine

Pass gravel pits in thick gravel
Pass gravel pits in thick gravel associated with Buffalo Moraine (Calkin, this volume, Figure 2).

Quarry on right next mile in Onondaga Limestone

Cross Onondaga Limestone Escarpment and under Route 5 (Main Street).

B4: SEDIMENTOLOGIC AND GEOMORPHIC PROCESSES AND EVOLUTION OF BUTTERMILK VALLEY, WEST VALLEY, NY
JON C. BOOTHROYD
University of Rhode Island.
Kingston, RI 02881
BARRY S. TIMSON
Earth Surface Research, Inc.
114 State St. Augusta, ME 04330
LORIE A. DUNNE
New York State Geological Survey
Albany, NY 12230
The purpose of this trip is to investigate the sedimentologic and geomorphic processes active in a small non-glacial gravel stream and on adjacent valley walls and tributaries. The work that led to this field trip is part of a larger geologic and hydrologic study by the New York State Geological Survey of the low-level nuclear waste disposal site and other use areas of the West Valley Nuclear Service Center. The geomorphic study is being done to determine, as accurately as possible, the denudation rate in the Buttermilk drainage basin, and to estimate rate and magnitude of morphologic changes to the waste-burial site.
Buttermilk Creek, located in southwestern New York (Fig. 1), has a drainage basin area of 78.4 km2 and is a tributary of Cattaraugus Creek. Figure 2 shows detail of that part of the drainage basin adjacent to the West Valley Nuclear Service Center (WVNSC).
GENERAL GEOLOGY
Surficial Geology
The area of interest is in the Ashford Hollow and West Valley 7 1/2 minute quadrangles. The regional surficial geology has been mapped by Muller (1977) and discussed by Coates (1976). Wisconsinan glacial features and later Holocene modifications of the 2 quadrangles have been mapped in great detail by Lafleur (1979) and discussed by him on the 1980 Friends of the Pleistocene field trip (Lafleur, 1980).
An upper plateau containing the waste-burial trenches, is underlain by till capped in places by a thin layer of fluvial gravel that marks the original fluvial surface immediately following the late Woodfordian deglaciation. Movement of groundwater in the vicinity of the waste-burial trenches has been investigated by Prudic (1979) and Prudic and Randall (1979). Mapping by Boothroyd et al. (1979, 1981) has further refined Lafleur's units in the vicinity of the WVNSC. There are eight till units, identified by age and present steepness of slope, and ten fluvial/alluvial fan systems ranging from the presently-active bar and channel system to late Woodfordian proglacial channels.

B4: SEDIMENTOLOGIC AND GEOMORPHIC PROCESSES AND EVOLUTION OF BUTTERMILK VALLEY, WEST VALLEY, NY

West Valley Nuclear Service Center (WVNSC) entrance.

STOP 1. Overview of the West Valley Nuclear Service Center.
The buildings housing the nuclear fuel reprocessing facility are to the left, waste-burial trenches are to the right. The land and buildings inside the high-security fence are owned presently by the U.S. Dept. of Energy and operated for them by the Westinghouse Corp. Westinghouse is carrying out the West Valley Demonstration Project, a program to solidify the high-level liquid waste stored on site, for later isolation in a still-to-be chosen facility. The NRC-licensed intermediate-level burial trench (left) is also operated by Westinghouse; the low-level trenches (right) are owned by the NYSERDA and are no longer accepting waste material.
The buildings are situated on an early Holocene alluvial fan; the waste-burial trenches are excavated in late Woodfordian Lavery till (Lafleur, 1979). The plateau containing the trenches marks the surface elevation of Buttermilk valley in early post-glacial time. The plateau beyond the trenches is covered by a thin veneer of fluvial gravel deposited in the ancestral late-glacial to early post-glacial Buttermilk Creek. Initial incision and downcutting began sometime before 9900 BP (Fig. 8), and continues to the present. The field trip discussion will focus on the manner and rate of erosion that will, in time, remove the plateau, and with it the waste-burial trenches.

Look for south reservoir in valley on the left.

New York State Plutonium Storage Facility.
End of paved road. STOP. Obtain prior permission to proceed on dirt road. CAUTION. This road is rough and steep. Trucks and/or 4 WD vehicles needed in wet weather. Go downhill and cross B & 0 RR tracks.

STOP 2. Assembly point.
Park vehicles so they do not block the B & 0 work road or access up and down the hill. Old Buttermilk Hill Rd. continues to Buttermilk Creek (100 m), the bridge has been removed. The surveyed section (Buttermilk-Bond reach) begins at the former site of the bridge and extends downstream to the north. Reservoir slug discharge enters from the west just below the bridge site.

Active channel of Buttermilk is undercutting railroad embankment.
View of bar complexes and low terraces.

STOP 3. Gravel-bar complexes, valley-wall landslides, etc.
Gravel-bar complexes, valley-wall landslides and alluvial fans, and Buttermilk fluvial terraces. The tributary stream enters Buttermilk Creek at bar complex 6, opposite the BC-6 landslide (Fig. 7). Extending 250 m upstream, to your left or south, is the BC 4-6 bar complex (Fig. 5). Just upstream of BC 4-6 is the BC-3 alluvial fan, situated on the west wall of the valley (Fig. 6). Fluvial terraces at several levels are preserved on the east side of the valley at the BC-6 tributary and on the west side adjacent to the BC-3 alluvial fan (Fig. 8). We shall discuss each of these features in turn, including gravel movement on the bars (Fig. 12). Please take care not to disturb any of the painted clasts.

B5: DEVONIAN BLACK SHALES OF WESTERN NEW YORK
DOUGLAS G. PATCHEN
KATHARINE LEE AVARY
West Virginia Geological Survey
Morgantown, WV 26507
The road log that follows is essentially a condensed version of the final day of a 5-day trip through the Middle and Upper Devonian clastics of central and western New York (Patchen and Dugo1insky, 1979). That particular trip was organized to give various contractors in DOE's Eastern Gas Shales Project (EGSP) the opportunity to examine, in the field, stratigraphic relations and facies changes hidden deep in the subsurface in the central Appalachian basin. The stops on the fifth day were designed to simulate a 2,200 to 2,500 foot stratigraphic section of "Devonian shale" in a typical "Brown Shale" gas well in West Virginia, Kentucky, or Ohio. The stops on this trip will enable us to visualize what the lowest 1,000-1,100 feet of section in such a well would look like. The main difference will be that the Dunkirk Shale, which is only 40-50 feet thick in this area, thickens westward and merges with the basal black shale of the Huron Shale. In southwestern West Virginia this black shale ranges from 300-400 feet in thickness and serves as both source bed and reservoir in more than 30 gas fields. More recently, prolific oil wells with initial potentials (IP's) ranging from 50 to 1,000 barrels per day have been drilled to this and other shales in the Devonian section in several counties along the Ohio River (Fig. 1). Thus, even though the EGSP is now defunct, interest in the Devonian Shales, both in the surface and subsurface, remains high.
When we agreed, at a rather late date, to organize this trip, we secured from Art VanTyne a promise to submit a companion article for the guidebook discussing surface to subsurface correlations and gas production from Devonian shales in New York. Furthermore, Wallace de Witt informed us that he would present a paper on Devonian shale stratigraphy at the Eastern Section meeting of the American Association of Petroleum Geologists that immediately precedes the NYSGA field trips. Therefore, we refer the readers to their articles and will present only the barest of stratigraphic summaries herein.

B5: DEVONIAN BLACK SHALES OF WESTERN NEW YORK

Exposures of Onondaga Limestone
Exposures of Onondaga Limestone along both sides of the highway. The black Marcellus Shale that overlies the Onondaga cannot be readily observed in the Buffalo area due to the relatively flat topography near Lake Erie.

Rhinestreet Shale with large concretions.
Town of Hamburg water tower. Good exposure of black Rhinestreet Shale with large concretions.

Exposures of the Ledyard and Wanakah Shales
Entrance for Hamburg Park. Exposures of the Ledyard and Wanakah Shales of the Ludlowville Formation can be observed near lake level in the park but not from the highway. Stop 1 of Tesmer (1966); stop 47 of Patchen and Dugolinsky (1979).

STOP 1. Eighteenmile Creek Gorge
Turn left on South Creek Road; park on right side of road. Walk carefully back along the road and over the bridge.
Upstream from the bridge over the main highway are exposures of the Wanakah Shale, Tichenor Limestone, Windom and Penn Yan Shales, Genundewa Limestone, and a few feet of West River Shale. The black shale near the top of the outcrop, which is weathered a reddish color and displays well-developed fractures, is the base of the Middlesex Shale. Notice the weathered pyrite associated with the base of the Tichenor Limestone, along with the abundant fossils, both characteristic of the Tichenor.
It is possible to walk from the exposures on the beach at the mouth of this stream where the Wanakah and Tichenor are present, upstream past the point and see the Middlesex, Cashaqua and Rhinestreet. Thus, continuous exposures from the Ludlowville Formation of the Upper Hamilton Group, through the Moscow Formation, the Genesee and Sonyea Formations, and into the West Falls Formation are present and all visible, representing a large proportion of Middle and Upper Devonian time.

STOP 2. Rt. 5 Bridge Over Eighteenmile Creek
JCT with Rt. 5. Cross and park on right. Descend gorge under the bridge.
The Wanakah Shale is exposed in the stream bed and may be under water, depending on water level. This is followed upward by one or two feet of Tichenor Limestone, about ten feet of Windom and Penn Yan Shale, some thin Genundewa Limestone, about 3 feet of West River Shale, a few feet of dark, platy Middlesex Shale, and the lower few feet of Cashaqua Shale which cap the section. The entire section is perhaps 35 to 40 feet thick and all is accessible.

Railroad Bridge.
Short walk along path to left before RR bridge offers a view of upper Cashaqua and lower Rhinestreet (Stop 3 of Tesmer, 1966).

Excellent, thick exposures of black Rhinestreet Shale
Drive slowly across bridge in right lane; turn around in parking area to right and drive back. Observe excellent, thick exposures of black Rhinestreet Shale in stream banks.

STOP 3: Town Of Evans Nature Park
Exposures of the Rhinestreet may be seen along the road and adjacent to the parking lot by the pedestrian bridge. The base of the Rhinestreet is exposed farther downstream but not here. The shale here is the typical dark, platy shale characteristic of the Rhinestreet, with reddish weathering in places and concretions being very common, although not as evident at this locality as they are in Rhinestreet exposures along I-90 southeast of Hamburg.

Entrance to home of Piarist Fathers
Entrance to home of Piarist Fathers, Stop 48 of Patchen and Dugolinsky (1979); Stop 2 of Tesmer (1966). Exposures of the Wanakah Shale, Tichenor Limestone and Windom Shale are present along the beach. If anyone is interested in examining this site, permission should be obtained from the residents. Also, access to the beach is by way of an old metal stairway. Extreme caution should be used.

Windom Shale to Middlesex Shale interval
Gibra1ter on the Lake (PRIVATE ROAD). Stop 52 of Patchen and Dugolinsky (1979). The Windom Shale to Middlesex Shale interval is exposed along the beach.

Evangola State Park
Turn left at entrance to Evangola State Park. This was Stop 53 of Patchen and Dugolinsky (1979); Stop 5 of Tesmer (1966).

STOP 4: Walnut Creek In Town Of Silver Creek
Park along Parkway near fire hydrant. Walk through small lot to edge of Walnut Creek. Descend into creek bed. Observe Pipe Creek Shale above Angola Shale. Wade under bridge to 60 ft. exposure of Hanover. Dunkirk Shale is exposed 2 miles upstream.
The contacts of the Pipe Creek Shale with the underlying Angola Shale and the overlying Hanover Shale are exposed in the stream bed of Walnut Creek in the Town of Silver Creek. The top 5 feet or so of the Angola is all that is clearly exposed, but the entire Pipe Creek and the lower 60 feet of Hanover are accessible, although wading boots are suggested. Lithologies in the Hanover range from green-gray, thinly bedded shales to silty beds which are more prominent due to higher resistance to weathering.

STOP 5. Point Gratiot, Dunkirk
Turn right (just after paved entrance to power station) into unpaved parking area and park.
The base of the Dunkirk is well exposed on the beach just south of the power plant. The distinct transition zone between the Hanover and the Dunkirk at, and just beneath (but visible in clear water), the water at normal lake level. The greenish-gray beds of the Hanover and the black beds of the Dunkirk are separated by two black and two greenish-gray transition beds. A small exposure may be seen, particularly if the water is calm, by tracing the lighter colored units along the beach and noticing a slight northward dip in this location.
Feeding trails and carbonized plant fragments may be seen on the tops of the beds within the transition zone. Pyrite nodules are common. A freshly broken surface of Dunkirk Shale provides a strong petroleum odor.

New gas wells in vineyards to east.
Along the route notice new gas wells in vineyards to east. These are in the Medina sands (Lower Silurian).

About 55 feet of Dunkirk Shale are exposed in the gully under the bridge.
Cross bridge adjacent to an old bridge on a parallel route to the right (east). This was Stop 55 of Patchen and Dugolinsky (1979). About 55 feet of Dunkirk Shale are exposed in the gully under the bridge. The transitional zone between the Hanover and Dunkirk can be observed in the stream bed.

Observe excellent Hanover-Dunkirk contact on the right.

Cross gorge with fairly poor exposure.

Cross gorge with a good section exposed.

Excellent Rhinestreet exposure
Excellent Rhinestreet exposure along both sides of the thruway near the town of Hamburg water tower. The large concretions are characteristic of the Rhinestreet in this area.

Rhinestreet-Cashaqua contact in the ditch to the east.

FIELD TRIP GUIDEBOOK
State University College
of Arts and Science
Potsdam, New York

1:SEISMOLOGY, TECTONICS AND ENGINEERING GEOLOGY IN THE ST. LAWRENCE VALLEY AND NORTHWEST ADIRONDACKS
Frank A. Revetta, Department of Geology
State University College of Arts and Science
Potsdam, New York 13676
William P. Harrison, Department of Civil and Environmental Engineering
Clarkson College of Technology
Noel Barstow and Ellyn Schlesinger-Miller
Lamont-Doherty Geological Observatory of Columbia University
Palisades, New York 10964
The purpose of this field trip is to develop an understanding of the seismicity and tectonics of the St. Lawrence Valley in Northern New York and the engineering geologic aspects of the St. Lawrence Seaway and Power Authority of New York State. Six stops will be made - one in the vicinity of Norfolk, New York and five in the Massena area. The locations of all stops are shown on Figure 1.
STOP 1 will be near Norfolk, New York (Figure 1) to observe a seismic field station which detects earthquakes that are recorded at Potsdam State College. STOP 2 is at the St. Lawrence Seaway Development Corporation office in Massena, New York (Figure 1) where engineers will discuss the St. Lawrence Seaway System. STOP 3 will be at Massena Center, New York, the epicentral region of the Massena-Cornwall earthquake. At this stop residents who experienced this earthquake will share their recollections of the earthquake with you. STOP 4 will be at the Eisenhower Lock where the engineering aspects of the lock will be discussed. Lunch will be eaten here, and hopefully a ship may be observed passing through the lock. At STOP 5 we will view the Long Sault Dam and observe seismic equipment in operation to detect local earthquakes. STOP 6 will be at Moses-Saunders Power Dam where engineers will discuss the operations and construction of the dam. At this stop there are a number of exhibits and a 30-minute film on the construction of the St. Lawrence Power Project.
All participants will meet in Room 120, Timerman Hall at 8:00 A.M., September 24 to hear a slide-talk on the seismology, tectonics and engineering geology of the St. Lawrence Valley. Frank Revetta will speak on the Massena-Cornwall earthquake of September 5, 1944. Ellyn Schlesinger-Miller and Noel Barstow will discuss the seismology and tectonics of the. Northern New York area. Bill Harrison will discuss the engineering geology of the St. Lawrence Seaway and Power Authority of the St. Lawrence River Valley. Slides will be shown of the stops made on the field trip. Participants will then proceed into the hallway for a brief discussion of the seismicity of Northern New York and the Lamont-Doherty Seismic Network.

Room 120 Timerman Hall
Slide-talk on seismology, tectonics and engineering geology of St. Lawrence Valley

STOP 1. Seismic Field Station
This stop will enable you to observe the operation of a seismic field station (Figure 2). The seismic equipment is contained. in two 55 gallon steel drums. In one drum is a short period (1 second) horizontal geophone, preamplifier-voltage controlled oscillator,and an FM radio transmitter. The geophone is mounted on bedrock which, in this case, is the Ogdensburg dolomite. The geophone detects the ground motion and its voltage output drives the high-gain preamplifier. The amplifier drives a voltage controlled oscillator which is frequency modulated by the geophone signal. This seismic modulated tone is transmitted a distance of 10 miles via an FM transmitter and a high gain directional antenna to Timerman Hall at Potsdam State College. In the second drum are five McGraw Edison 1000 Ampere hour air cells which provide the power for the amplifier, VCO, and radio transmitter for one year.
At the receiver end is another high-gain directional antenna and an FM receiver. The signal, together with the FM carrier wave, is picked up by the receiver and passed into a discriminator where the carrier wave is removed. The signal then passes into the amplifier and into the heliocorder for recording.
2011: Location comes from lat/long of old seismic stations, LDGO website. OHM

STOP 2. St. Lawrence Seaway Development Corporation Operational Building
This stop is at the St. Lawrence Seaway Development Corporation's Administration Building at Massena, New York. At this stop engineers will discuss the construction and operation of the St. Lawrence Seaway. An explanation will be given of a wall display which depicts approximately 2300 miles of waterway from the headwaters of the Great Lakes to the Atlantic Ocean. You will also have the opportunity to view a model of the St. Lawrence Seaway and Power Projects, including the locks, Long Sault Dam, Massena Intake and Village of Massena.

STOP 3. Massena Center
Epicenter Of The Massena-Cornwall Earthquake Of September 5, 1944
Massena Center is the epicenter of the Massena-Cornwall earthquake of September 5, 1944 (Figure 3). The epicenter was located from P-phase arrival times and a least square solution and was found to be at 74° 53.9 W longitude and 44° 58.5' N latitude. The depth of focus of the earthquake was estimated to be 20 miles. The magnitude of the earthquake was 5.9 and a maximum intensity of VIII occurred in the vicinity of Massena Center. The total damage was estimated at $2,000,000.
An interesting fact regarding the damage was in the cemeteries. On the Canadian side of the river the tombstones were generally rotated counterclockwise,and on the United States side they were generally rotated clockwise. It appears that this indicates horizontal displacement along a fault line parallel to the river even though geologists report no surface evidence of any major fault in the immediate area. However, the tombstones and chimney damage indicate an origin somewhere between Cornwall and Massena, which is confirmed from the study of seismograms. The cemeteries are the best evidence of the relative violence of the earthquake in different areas, and they furnish the chief line of division in determining the areas of major damage (Figure 3).
At this stop we will observe tombstones that have been rotated and translated by the Massena-Cornwall earthquake. Also, two Massena Center residents, Messrs. Bob Rickard and James Carton, who experienced the earthquake will discuss their recollections of the event.

Massena Epicenter
2011: The coordinates given in the description of STOP 3 plot up here. OHM

STOP 4. Eisenhower Lock, St. Lawrence Seaway
This structure enables ships traveling the St. Lawrence River to pass around the Moses-Saunders Power Dam and, along with Snell Lock five miles farther east, lowers the ships through a total of 95 feet of elevation. Both locks have dimensions of 850 feet by 80 feet and are of concrete construction. The locks are huge bathtubs, in a sense, with openings along the sides into a passageway (about 13' wide by 15' high) on each side which slopes to the upstream end of the lock. When a ship comes down the St. Lawrence River and through the canal to the lock, the lower lock gates are closed, and the water is at the upper canal elevation. The ship moves slowly into the "bathtub," the upstream gates are closed, and then the water is let out of the locks through the openings in their sides, down the passageway on either side and discharged below the lock. A system of baffles on the downstream end prevents excessive turbulence.
When a ship comes upstream to the lock, the upper gates are closed and the water level is at the same elevation as the water surface downstream from the lock. The ship moves into the lock, the lower gates are closed, and water is introduced into the side passageways from the upstream end of the locks flowing into the lock through the side openings, thus filling the lock and raising the ship to the elevation of the canal on the upstream side. Then the upper gates are opened and the ship moves out of the lock upstream. Recently, some deterioration of the lock concrete has been observed, and an extensive study has been made by the Corps of Engineers, which is resulting in appropriate remedial measures.
At this stop we will visit the Eisenhower Lock Vessel Traffic Control Center to view its functions. Hopefully, we will see a ship pass through the lock. Lunch will be eaten at this stop and a concession stand is available.

STOP 5. Long Sault Dam
The Long Sault Dam is located just below the foot of Long Sault Island, crossing both the main channel of the St. Lawrence River and the smaller channel south of Long Sault Island. It is located four miles north of the Village of Massena, New York and 6.5 miles west of Cornwall, Ontario, Canada (Figure 4). The Long Sault dam serves as a control for the St. Lawrence River, developing approximately 82 feet of drop through the Long Sault Rapids. It is a concrete gravity structure having a maximum height of about 132 feet above foundation. The foundation of the dam is on bedrock (Ogdensburg Dolostone) and the dam is relatively noise free, therefore it is an ideal location for the installation of earthquake detection equipment.
This stop will enable you to observe some seismic equipment installed in the dam by the Lamont-Doherty Geological Observatory and the State University of New York at Binghamton. The dam is an ideal place for the installation of seismic equipment because it is coupled well to the bedrock of the area and is a quiet place. Three instruments may be observed on the lowest level of the dam: a short-period vertical seismometer, strong motion accelerograph (SMA) and a digital cassette accelerograph. The vertical seismometer and the strong motion accelerograph are part of the Lamont-Doherty Seismic Network and the digital event recorder is operated by SUNY at Binghamton.
The short period (1 second) vertical seismometer responds to the ground motion produced by an earthquake. The seismometer drives a high-gain amplifier. The amplifier drives a voltage controlled oscillator (VCO) which is frequency modulated by the seismometer signal. This frequency modulated audio tone is then inserted into a telephone line for transmission to LamontDoherty Geological Observatory. At the L.D.G.O. at Pa1lisades, New York the various tones are distributed to the magnetic tape recorder and to appropriate discriminators. The discriminators separate the seismic data from the telephone line carriers. The data is transferred to develocorders and/or helicorders.
The strong motion accelerograph (SMA) was installed by the Lamont-Doherty Geological Observatory. This instrument contains three accelerometers that record on film the vertical and horitontal accelerations produced by a strong earthquake. The instrument remains in a standby condition until an earthquake triggers it. The "P" wave triggers the instrument which operates till the earthquake is recorded. The. SMA can record a single earthquake or a sequence of earthquakes and aftershocks. The event
indicator shows when an earthquake has been recorded. Before an event it is black, after the event, it is white.
The reason for recording such motions comes from two widely different scientific needs. Such measurements are necessary within man-made structures for engineers to develop structural design criteria in earthquake engineering. There is very little information about the accelerations produced by earthquakes in the eastern United States. Secondly, seismologists studying the details of the earthquake source for information on dimensions, stress drops and time histories of the rupture process need measurements in the near-field of larger earthquakes.
The third instrument is a digital cassette seismograph which belongs to Francis Wu, SUNY at Binghamton, New York. This instrument is triggered by the "P" wave and records the event on cassette tape. A portable playback-plotter accompanies the instrument to provide playback for set-up, testing, maintenance and analysis. The seismic data can be translated from cassettes to any IBM compatible tape and can provide a wide variety of seismological analysis.

STOP 6 Moses-Saunders Power Dam
The location map is shown in Figure 4. This dam provides approximately 912,000 kilowatts of power. The dam has a head of 81 feet, and behind it is Lake St. Lawrence, with its fine marina and Barnhart Island Beach.
A thirty minute film will be shown in the auditorium at the dam, which will illustrate the methods and problems of construction.
A tour of the dam will be made, and from the top of the building Lake St. Lawrence can be clearly seen, with some of the zoned and rip-rapped dikes bounding it composed of compacted glacial till with dry densities on the order of 140 pcf (concrete is 150 pcf).

2: GEOLOGIC TRAVERSE FROM POTSDAM TO THE THOUSAND ISLANDS
Bradford B. VanDiver, S.U.N.Y. Potsdam
The Lowlands Adirondacks, or northwestern part of the Adirondack Mountains Province, contains a record of extremely ancient seas that predate the Grenville Orogeny by hundreds of millions of years, and in which limestones, various detrital sediments, and volcanic materials were deposited. The orogeny, now dated at 1100 m.y. in the Adirondacks, produced severe metamorphism, intense deformation, igneous activity, and a mountain range of Himalayan scale extending for thousands of miles along the eastern side of North America as it existed then. These mountains are referred to as the Ancestral Adirondacks. The Grenville-age rocks
we see today, in the Adirondacks, the Thousand Islands, and in the Grenville Province of Canada, are but remnants of the core of that great mountain range, where orogenic processes were most severe (Fig. lA). There ensued a period of erosion that lasted approximately 600 million years and left a landscape of low relief with karsts developed in the marbles. Flooding by shallow seas that advanced from the east, set the stage for deposition of shelf sediments in late-Cambrian Potsdam time, that continued until the beginning of the Taconic Orogeny in late Ordovician time. This once continuous cover of sedimentary rocks has been largely removed from the Adirondacks and Frontenac Arch in the last few million years by erosion accompanying the still-continuing rapid uplift of those regions (Figs. lB, 2) (Isachsen, 1975).
The principal purpose of this field trip is to examine the Precambrian and lower Paleozoic rocks exposed in a traverse from Potsdam to Alexandria Bay, with special regard for the nature bf the unconformity itself. The trip will be highlighted at midday by a boat trip through the lovely Thousand Islands. The route and stops are shown on Figure 3.

2: GEOLOGIC TRAVERSE FROM POTSDAM TO THE THOUSAND ISLANDS

Dark, migmatitic gneiss
Railroad underpass. Exposures of dark, migmatitic gneiss with pink granitic veining.

Small marble cut
Small marble cut, right, with whitish banded marble below and marble thinly interleaved with rusty calc-silicate rock above. Folding here reflects the ductility contrast between these two rock types that is characteristic of the Adirondack region in general. Flow banding in the marble displays a remarkable fluidity, whereas the calc-silicate, though also intensely folded has been extensively ruptured and displaced. The result is a chaotic "marble stew," which resembles what might be seen if strips of crisp fried bacon were swirled in smooth peanut butter. More of this will be seen at Stop 1.

Low, long roadcut in dark greenish-gray calc-silicate rock
Low, long roadcut in dark greenish-gray calc-silicate rock with subordinate marble interlayers, right side of road. Tight recumbent folding.

STOP 1. The Snake Roadcut
This is the now-famous and graffiti-ed Snake Roadcut; the name for which was first published in the guidebook for the 1971 NYSGA meeting at Potsdam (Fig. 4). The cut is a large and outstanding example of the plastic deformation of the Grenville marbles. The "Snake," itself, is a nearly continuous, thin band of microcline-rich rock on the SE cut (left) that has been sinuously infolded with the marble. Despite its thinness and obvious stretching, the Snake has survived nearly unbroken over much of its length. A good example of a refold can be seen at the NE end, where Fl isoclinal folds have been openly folded around an F2 hinge surface. The deformation shown by the Snake is deceptively simple. Greater complexity, perhaps with as many as four separate folding events, can be observed above the Snake on top of the cut (DANGEROUS!), where thin, infolded layers of rusty calc-silicate rock have been exposed in three dimensions by solution of the enclosing and interleaved marble. A less dramatic, but safer, example can be observed at the right end of the opposite cut, near road level.
In the marble adjacent to the Snake, note the dark green, concentric banding of diopside, the product of metamorphic reaction between the dolomitic marble and siliceous parent rock of the Snake. Diopside concentration diminishes rapidly away from the band. Also found in this reaction zone are fine-grained brown sphene, copper-colored phlogopite, yellowish metallic pyrite, green actinolite, black tourmaline, and very minor quartz.
Carl and Van Diver (1971) proposed a subaqueous ashfall origin for the parent material of the Snake, interrupting a shelf limestone sequence. This is suggested both by the composition, and the thin, blanket shape of the layer. Other snakes of similar material, and some of phlogopite may be seen on the opposite cut.

STOP 2. DeKalb Anticline
DeKalb Anticline, located 100 feet from the right side of the road (Fig. 5). This is an overturned anticline in dark brown garnet biotite schist, with interlayered light greenish gray, calc-silicate rocks, altogether a rather unusual rock for the Lowlands Adirondacks. The fold is interrupted near its hinge surface by a two-foot pinkish pegmatite dike. As at the "Snake," the deformation here appears deceptively simple. Contoured point diagrams of minor fold axes prepared by several generations of Structural Geology students at Potsdam, indicate refolding (this is nearly identical to similar diagrams prepared for the Snake). Furthermore, there are a few puzzling S-shaped folds at the right side of the dike that suggest renewed deformation after pegmatite emplacement. Study the texture of the dike from side to side, and see if you can find evidence for this interpretation.
A small cut directly across the highway displays a rusty basaltic (diabasic?) dike that intrudes the biotite schist, with contacts that zig and zag alternately along schistosity and jointing. At the left end, there is a small xenolith of granitic rock incorporated in the basalt. Diabasic dikes like this are common in the Lowlands Adirondacks. They intrude the Grenville-age rocks but not the Potsdam Sandstone, and are considered to be of late Proterozoic to early Cambrian age.

STOP 3. Red-and-White Roadcuts.
This is one of the most dramatic series of new cuts opened by road construction in 1976-77. The first cut on the right (lowest) exposes highly contorted grayish marble in sharp, irregular, discordant, contact with a chaotic mass of friable pinkish to dark brick red sandstone, sandy intraformational breccia, and conglomerate, with assorted inclusions of marble. A wedge-shaped conglomerate dike is located at the top of the marble just to the right of the sedimentary contact.
All of these features undoubtedly result from the infilling of a sinkhole developed in the marble prior to and possibly continuing during marine transgression in Potsdam time. The contact represents an unconformity spanning about 600 million years. Similar features may be observed at numerous places in the northwestern part of the Lowlands Adirondacks, most notably in the Rock Island Road cut 4 miles north of Gouverneur, (Carl and Van Diver, 1971) .
On a regional scale, remnants or outliers of sandy and conglomeratic sediments like this become smaller and less frequent southeastward from the continuous Paleozoic boundary near the St. Lawrence River, and they are largely confined to areas of marble. Because of their lack of fossils, often chaotic nature, and discoloration, their assignment to the Potsdam Sandstone is uncertain, but many exposures display upward gradation to clean, pinkish to white or brown, orthoquartzitic, wellbedded arenites typical of the Keeseville member of the unit in this region. Such an upward progression may be seen in the second large roadcut on the right, up the hill. The large, reddish-brown cut opposite this consists of well-stratified, quartz pebble conglomerates, with thin orthoquartzitic sandstones on top. A small knob of marble occurs at road level near the lower end of the cut, where clayey sediment has been found (cave floor?).
Studies by the New York State Geological Survey indicate that the Potsdam Sandstone and the overlying Theresa and younger units dip away from and do not pinch out toward the Adirondack Dome. It is assumed; therefore, that these units once formed a continuous blanket over the region, which has been largely denuded during the geologically recent, and continuing doming of the mountains. It is mainly in thick karst fillings like this near the edge of the Precambrian terrain, that the basal Potsdam, or pre-Potsdam, sedimentary rocks have been preserved.

Dark gneiss left.

Dark gneiss, perhaps meta-turbidite
Begin Richville Bypass. Dark gneiss, perhaps meta-turbidite, with apparent preserved small-scale graded bedding.

STOP 4. End of Richville Bypass.
Dark red cut at right is puzzling, and it is hoped discussion will be generated among field trip participants. The material is similar to, but much more hematitic and voluminous than that of the unquestioned sinkhole fillings. More "normal" Potsdam sandstone may be found at the top of the cut. Conglomeratic sandstone dikes in marble may be found at the upper end of the opposite cut. The left half of that cut, however, consists of a whitish feldspathic (metapegmatite) rock outwardly resembling the marble, and containing several thin, diopsidic marble sills or dikes. What do you suppose is the origin of this rock? See if you can find the contact with the marble.

Begin several marble cuts
Begin several marble cuts with abundant small reddish conglomeratic sandstone infillings. From here to Gouverneur the road traverses rolling countryside with predominantly NE-trending ridges underlain by gneiss, and marble valleys.

Enter Gouverneur.
Enter Gouverneur. Note the several buildings in town constructed of Gouverneur marble, essentially the same as the marbles we've been looking at.

Begin several marble cuts.

Potsdam Sandstone cut right, with bowl-shaped structure at top.
These structures are commonly found intermingled with cylindrical structures near the base of the Potsdam over marble. They have long been thought to result from the rearrangement of sand by sifting into underlying small solutional pockets in marble. They are copiously developed along the Cream of the Valley Road north of the Rock Island Road cut.

Begin several marble cuts, some with dark calc-silicate layers.

Sand and gravel quarry in kame
Marion Construction Materials sand and gravel quarry in kame, right. Well rounded cobbles, abundant cross-bedding.

Pinkish Alaskite at x-road, with glacial grooves on top

Optional stop. Begin several cuts of marble
Begin several cuts of marble with infolded and segmented calcsilicate layers, in direct contact with biotite granite gneiss.

Intersection in the Village of Antwerp, cuts in migmatitic gneiss.
Intersection N.Y. 411 in the Village of Antwerp, with cuts in migmatitic gneiss. Pass over Indian River. Turn right to Theresa. The road along the way (about 10 miles) passes by numerous outcrops of gneiss and marble. The gneiss tends to form rounded, elongate, barren knobs, with streamlined, glacially smoothed forms.
2011: On the older maps Route 26 joins at this intersection. Currently, both 411 and 26 join near Philadelphia.

STOP 5. Theresa Reservoir
The cliff on the left side of the road near the reservoir, again, is a reddish conglomerate and breccia similar to those you have seen in sinkhole deposits. Massive and poorly bedded, it is but one of a wide variety of conglomerates and breccias occupying the interval between Proterozoic rocks and "normal" Potsdam Sandstone in the Lowlands Adirondacks. In this one, pebbles are sparse except near the center base of the cliff. Upwards in the section, the rock becomes sandier, better stratified, and cross-bedded. The underlying rocks are concealed by the cliff, but can be seen just below the Niagara Mohawk dam nearby. The rocks are all steeply-inclined gneiss and metaquartzite. The Indian River drops more than 80 feet here. The dam was built in 1929 on the site of the original, 65-foot "High Falls" - almost certainly a fault scarp. Raising the water to its present level eliminated the 15-foot "Upper Falls" that were located a short distance upstream.

Tableland capped by flat-lying, durable Potsdam Sandstone
Theresa lies close to the Paleozoic boundary, and here the road climbs onto an extensive tableland capped by flat-lying, durable Potsdam Sandstone and occasional outliers of Theresa sandy dolostone perched on top of it.

Pass several cuts in Theresa Formation.

STOP 6 at Plessis
The clean surface of the Potsdam Sandstone here offers a remarkable display of well-preserved glacial scour features, including polish, striae, chatter marks, and large grooves. Also visible on the smooth surface are abundant arcuate cross-bed laminae. The gentle undulation of the Potsdam surface seen here is barely concealed beneath thin soil cover between here and Alexandria Bay. Continue north on N.Y. 26 past cuts of light gray, thin-bedded Theresa Formation.

The flatness of the tableland is most evident here
Browns Corners. The flatness of the tableland is most evident here, when viewed across open pastureland with less than 10 feet of relief. Continue left to Alex Bay.

Boat Ride
The purposes of the boat ride are: 1) to give us a welcome relief from bus travel; 2) to allow time to eat lunch; 3) to view some of the magnificant Thousand Islands, and 4) to view, from the boat, exposures of flat-lying Potsdam Sandstone over granitic gneiss at the southern tip of Wellesley Island.
The boat trip will take us first through open water under the beautiful Thousand Islands suspension bridge to the end of Wellesley Island. Then we will wend our leisurely way back through the cluster of scenic islands near the American shore.
It is now believed that the Proterozoic terrain of the Thousand Islands was once blanketed with flat-lying Potsdam Sandstone and younger Paleozoic units, as was that of the Adirondack Mountains. In historical perspective, the Himalayan-sized Ancestral Adirondacks, resulting from the Grenville Orogeny approximately one billion years ago, had by Potsdam time, been worn down to a peneplain, leaving the region vulnerable to marine submergence. Transgression of the so-called "Potsdam Sea" beginning in late Cambrian(?) time (ca. 525 m.y.a.). set the stage for shallow marine deposition of sand, carbonates and clays, the parent materials for the lower Paleozoic units that now rim the Adirondacks and Frontenac Arch. Erosional decimation of these once continuous deposits has been accomplished only in the last 10 million-or-so years as a result of the still-continuing doming of the Adirondacks and concurrent uparching of the Frontenac Arch. Presently, only a few scattered remnants of Potsdam Sandstone remain on the flanks of the Arch in the Thousand Islands region, and on its northwestward and southeastward extensions into Canada and New York, respectively. We will view one of these patches from the boat at the southern tip of Wellesley Island. Farther upstream toward Lake Ontario, a much larger remnant has survived erosion on Howe Island, and still farther, Wolfe Island, the largest of the Thousand Islands, is completely blanketed with limestones belonging in the medial Ordovician Black River and Trenton Groups (the lower Ordovician Theresa and Beekmantown are missing). An exposure of the Proterozoic / Potsdam unconformity that is essentially similar to that of Wellesley Island will be examined at close range at STOPs 7 and 8 later.
The Proterozoic rocks of the Frontenac Arch have also been deeply eroded as a result of the ongoing uplift, leaving only the more resistant knobs projecting as islands or shoals. The islands are generally elongated parallel to their strong northeasterly structural grain, a trend that is even more evident in the marble-gneiss outcrop patterns of the Lowlands Adirondacks. For the most part, the islands are lovely, forested, projections of attractive, pink leucogranitic (alaskitic) Alexandria Bay Gneiss (visible mainly along the shores). Most of them take the form of glacier-polished sheepbacks, with gentle stoss sides facing northeastward and steep cliff sides opposite, indicating a southwestward upvalley ice advance. The islands are largely devoid of glacial debris, except for some minor till hills, and thin ground moraine. This scarcity probably reflects, at least in part, the severe erosion resulting from rapid drainage of Lake Iroquois through the St. Lawrence Valley, after that outlet was opened by recession of the Wisconsin ice sheet.

STOP 7. Alexandria Bay Roadcut
The northeastern (downhill) end of this cut exposes an angular unconformity of profound dimensions, encompassing a time gap of approximately 600 million years between Proterozoic gneisses and basal Potsdam Sandstone. It enables comparison between the contemporaneous erosional surfaces developed on gneisses and those of the marbles seen earlier.
The Proterozoic rocks beneath the unconformity consist of massive, pink, alaskitic gneisses and darke, banded gneisses with steeply dipping foliation. These are extensively weathered, especially in a narrow zone directly beneath the base of the Potsdam. Note, also, that the upturned edges of the gneiss bands are buckled below the contact; This zone may represent a fossil inorganic soil developed on the pre-Potsdam erosional surface, or preferential, post-depositional, groundwater leaching along the contact (which may also explain the extreme friability of the basal sandstone beds). Can you suggest any other possibility?
Features nearly identical to these have been reported on the other side of the Adirondacks near Putnam Center, N.Y. by Van Diver (1980). The pre-Potsdam erosional surface appears to be structurally intact and rises slightly to the northeast (downhill on the road), forming a boss, or knoll preserving the original relief of the depositional surface. Basal sandstone beds drape over the southwestern slope of the knoll, and pinch out against it, while proximal younger beds thin out over the top of it. Upwards in the section, the bedding becomes increasingly horizontal and uniformly thick. Cross-bedding, in general, is poorly developed, but is more prevalent in the upper part of the section.
The basal Potsdam beds at this roadcut have been described by Kirchgasser and Theokritoff (1971), as mature orthoquartzites with scarce clasts of Precambrian rocks, suggesting an origin by reworking of fluvial sands by an encroaching sea. On a regional scale, marine transgression set the stage for leveling of the irregular Proterozoic surface by filling in all of the karst depressions like those seen earlier, and covering over projections in gneisses such as that of the Alex Bay Cut.

Cross-bedded Potsdam Sandstone cut.

STOP 8. Proterozoic/Potsdam unconformity.
This cut shows features similar to the Alex Bay cut, but here the basal sandstones display better-developed, low-angle~ crossbedding. The purpose of this stop is to allow comparisons between these two exposures of the unconformity, as developed on gneiss. From here, we will proceed directly to Ogdensburg, and then to Potsdam.

Begin several excellent exposures of gneiss.

Cuts in lower potsdam Sandstone with distinct lower and upper lithofacies (see Selleck, this volume).
Continuing northeastward, the cuts along the highway expose progressively higher stratigraphic sections of the Potsdam and Theresa Formations. Contact between the two units is exposed at Chippewa Bay (Selleck, STOP 3, this volume; Kirchgasser and Theokritoff, 1971).

A good overlook to view the river is located a at Cedar Point.

3: SELECTED MINERAL OCCURRENCES IN ST. LAWRENCE AND JEFFERSON COUNTIES, NY
George W. Robinson
National Museums of Canada
Mineral Sciences Division, NMNS
Ottawa, Ontario, Canada K1A OM8
Probably no other region in the State of New York is better known for its wealth of mineral occurrences than at St. Lawrence, Jefferson, and Lewis Counties. Indeed, many are among North America's most famous and classic localities (Beck, 1842; Dana, 1877; Kunz, 1892; Jensen, 1978; Robinson and Chamberlain, 1981). The vast majority of these occurrences are found within the Grenville metasediments, which are geologically complex and host a wide variety of mineral assemblages. It is the intent of this trip to acquaint the participant with a selection of localities that provide a variety of geological environments, are of mineralogical and historical interest, and will hopefully afford good collecting opportunities. For additional information, the reader may wish to consult some of the available collecting guides (Agar, 1921,& 1923; Robinson, 1971; Robinson and Alverson, 1971; Van Diver, 1976).

3: SELECTED MINERAL OCCURRENCES IN ST. LAWRENCE AND JEFFERSON COUNTIES, NY

STOP 1: The Powers Farm at Pierrepont
Many of the most interesting localities in Northwestern New York and Southeastern Ontario are in contact zones between various Precambrian rocks and Grenville marble, and particularly in their associated calcite vein-dikes (Robinson, 1982; Moyd, 1972). Such contacts are often of a local nature, and host a wide variety of complex skarn-like mineral assemblages. The Powers Farm has one such occurrence.where a quartz-tourmaline-biotite pegmatite (?) is in contact with coarsely crystallized calcite.

STOP 2. The McLear Mine at Dekalb Junction
Continue to the first road to the right and park. The McLear Mine is immediately to the southeast of this intersection.
The McLear pegmatite was discovered in 1907 by J.H. McLear, on the Kilburn Farm, 3.9 miles southwest of Dekalb Junction (Cushing and Newland, 1925; Shaub, 1929). The ore consisted of pure, white microcline perthite, which was hand cobbed and shipped to Rochester and Trenton for use in the pottery industry. By 1929 the Green Hill Mining Company had developed both open cut and underground workings, and shipped over 120,000 tons of pottery grade feldspar (Shaub, 1929). By 1938 mining ceased (Tan, 1966).
The main pegmatite is a lens shaped body 850xl15x60 feet with a spacial orientation generally paralleling the regional NE-SW structural trend of the enclosing Grenville metasediments. Radiometric age determination from uraninite indicates the pegmatite was emplaced in the middle Precambrian at 1094 m.y. (Shaub, 1940). The mineralogy of the pegmatite is unique, and suggests a complex origin by successive replacement of the host crystalline limestone by magmatic solutions probably emanating from nearby granites (Shaub, 1929). Based on mineralogic and textural zonation the apparent paragenetic sequence is diopside + tremolite + quartz + feldspar + quartz, giving rise to a gradational contact between the pegmatite and wall rock. Later hydrothermal alteration caused slight sericitization of the feldspars and serpentinization of the diopside and tremolite.
Minerals that may be collected relatively easily include: diopside, microcline, mica, quartz, titanite and tremolite. Allanite, apatite, calcite, chlorite, goethite, hematite, kaolinite, magnetite, molybdenite, pyrite, pyrrhotite, rutile, serpentine, talc, thorite, thucholite, tourmaline, uraninite, and zircon occur more sparingly.

STOP 3. The Gem Diopside Mine at Dekalb
From the McLear Mine proceed south (right) on the road to Bigelow for 1 mile and park. The locality for gem diopside is on the ridge across the field, east (left) of the road. This locality is on private land, and is NOT regularly open for collecting!
This locality has produced some of the finest crystals of gem diopside known. Early specimen labels may give the locality as the Mitchell Farm, as Calvin Mitchell was probably the first person to find and distribute specimens in the 1880's. By 1889 the famous mineral dealer George L. English acquired the mining rights, and by 1892 George F. Kunz had described crystals over 3 inches long that would yield gems up to 30 carats. For unknown reasons the deposit was not worked again until 1967 (Szenics, 1968), and intermittently thereafter (Robinson, 1973).
The mine is situated in a northeasterly trending ridge of diopside-tremolite-quartz schist, approximately 4 miles northeast of the Village of Richville. The relative proportions of diopside, quartz and tremolite vary considerably, and the quartz locally forms tightly folded bands. The gem pockets tend to form within the diopside rich layers and along tremolite veins 'which follow joints perpendicular to the strike. The pockets are often filled with a compact gray talc and acicular tremolite. The apparent paragenetic sequence is diopside + tremolite + talc + quartz ± calcite. Other species that occur less commonly are pyrite, plagioclase, and datolite (reported but unconfirmed). The diopside invariably occurs as euhedral prismatic crystals with well developed forms {100}, {110}, {001}, {l01}, and several {Okl} and {hkl} prisms (Figure 1) .

STOP 4: The Coal Hill Vein at Rossie
The Rossie Lead Mines are one of the oldest and most famous North American mineral localities. The large crystals of calcite and galena these veins once produced are indeed classics. The Coal Hill Vein is perhaps the best known and is probably a relatively low temperature hydrothermal calcite-galena vein that intruded Precambrian granite in post-Ordovician time.
Park in the field to the right at the Coal Hill Vein.
Mining first commenced at the Coal Hill Vein in the winter of 1836, and continued throughout the Civil War. The vein was excavated over a length of 600 feet and to a depth of 200 feet. By 1868 operations ceased, after producing over 1625 tons of lead (Cushing and Newland, 1925). During this period many fine, large crystals of galena and calcite were recovered, and soon became the object of much discussion (Beck, 1842; Emmons, 1842; Dana 1877). Fortunately a number of excellent specimens found their way into prominent collections and may still be seen today at the American Museum of Natural History, Harvard University, Hamilton College, and the New York State Museum. The complexity of forms on some of the calcite, pyrite, and fluorite crystals is nearly unrivalled (Figures 3-5).
The vein consists primarily of calcite with disseminated galena, and occupies a nearly vertical, east-west fault in the enclosing Precambrian granite. Inclusions of partially altered wall rock form a brecciated zone near the contact. By comparison to nearby veins and similar deposits in Ontario, emplacement is thought to be post-Ordovician (Beck, 1842; Smyth 1903; Wilson, 1924). Whether the mineralizing solutions originated from below as relatively cool, chemically inactive fluids, descended from above through meteoric concentration from the overlying Paleozoic rocks, or were perhaps derived from both meteoric and magmatic waters remains an unanswered dilemma (Smyth, 1903; Buddington, 1934; Wilson, 1924; Uglow, 1916).
Recent SEM studies have unveiled the presence of an unusual assemblage of anatase, albite, synchysite, and cerian epidote occurring in micro cavities and fissures in both the vein material and altered wall rock. Hopefully, a continuing investigation will help clarify the origin and paragenesis of these veins (Robinson and Chamberlain, in prep.).
Nearly all the following species may still be collected from the dumps, but not in the quality that was produced when the mine was operating: albite, anatase, anglesite (?), calcite, celestine, cerussite, chalcopyrite, fluorite, galena, microcline, quartz, sphalerite, stilbite (?), and synchysite.

STOP 5. The Sterling Mine at Antwerp
Stop at the Villeneuve Farm on the right side of U.S. 11 to obtain permission to enter the Sterling Mine property.
Continue north on U.S. 11 to the Sterling Rock Shop and mine road entrance on the right. Park here and walk down the old mine lane approximately 350 yards to the mine.
The Sterling Mine was the first U.S. locality for millerite, and is often regarded as having produced some of the world's best specimens of that species. The mine lies near the middle of a group of hematite deposits known as the Antwerp-Keene belt (Buddington, 1934). Mining first began in 1836 and continued until 1910, creating an open pit 500 feet long, 175 feet wide and 115 feet deep, that produced hundreds of thousands of tons of ore (Smock, 1889).
The geology of this deposit is complex, and a detailed mineralogical study is currently in progress (Robinson and Chamberlain, in press). The mine is situated along a marble-gneiss contact, and the ore is intimately associated with a heavily slickensided quartz-chlorite rock which is thought to have formed by the replacement of the gneiss by corrosive, iron-rich solutions derived from the decomposition of underlying pyritic schist (Smyth, 1894; Buddington, 1934; Prucha, 1957). Both the chloritic rock and marble appear to have been replaced by hematite resulting in a gossan-like structure which was then preserved by a capping of Potsdam sandstone. Open spaces were filled with hematite and quartz, and possibly other species not preserved. Subsequent recrystallization of the quartz and hematite at relatively low pressure and temperature is suggested by the presence of Fe-talc and stilpnomelane, and is supported by fluid inclusion studies (Robinson and Chamberlain, in press). Further changes in the composition, eH and probably pH of the mineralizing solutions are evident from the presence of magnetite pseudomorphs after hematite, both Fe(II) and Fe(III) rich stilpnomelanes, Fe-talc and various sulfide and carbonate phases.
Minerals that can readily be collected are hematite, magnetite pseudomorphs after hematite, quartz, stilpnomelane ("chalcodite"), Fe-talc, siderite, goethite, calcite, ferroan dolomite, and more rarely millerite and jamborite (?), all of which occur as well formed crystals in vugs in the crystalline hematite-quartz ore. Early reports of cacoxenite and ankerite can not be confirmed, and likely resulted from the misidentification of stilpnomelane and siderite (Robinson and Chamberlain, in press).

4: STRATIGRAPHY, STRUCTURE, AND GEOCHEMISTRY OF GRENVILLIAN ROCKS IN NORTHERN NY
James D. Carl
S.U.N.Y. Potsdam
William F. deLorraine
St. Joe Resources Company
The geology of the northwest Adirondack lowlands is characterized by northeast-trending belts of highly deformed rocks, chiefly marbles and gneisses, all metamorphosed to upper amphibolite facies grade during the Grenvillian Orogeny. A clear picture of the structure and stratigraphy of this region has proven elusive due to effects of recrystallization, multiple folding, anatexis and magmatism during metamorphism.
Several different structural and stratigraphic models have been proposed which illustrate the diversity of opinion surrounding these rocks. Engel and Engel (1953) believed the stratigraphy to be part of the overturned, southeastern limb of a regional anticlinorium whose upright limb lay to the northwest in Canada. They recognized five major stratigraphic units which, from NW to SE in order of decreasing age, include the following:
1) Black Lake metasedimentary belt; 2) Gouverneur, or Lower Marble; 3) Major Gneiss belt; 4) Balmat-Edwardst or Upper Marble; and 5) Harrisville-Russell belt (see map, Figure 1 and cross-section, Figure 2).
A model by Lewis (1969) included two major marble units, separated by the Major Gneiss, which were continuous across the northwest Adirondacks but repeated in linear, northeasterly belts by tight, upright folds. More recently Foose (1974) and Wiener (1981) postulate that there is but one carbonate horizon repeated by multiply-refolded nappes.
There seems to be agreement that alaskitic gneisses (leucogneisses) which core domical structures in the northwest Adirondacks constitute a basal horizon over which marble and gneiss precursors were deposited. Geochemical data and recent field mapping reveal a relict stratigraphy consistent with an ash flow tuff origin. Geochemical data from the Major Gneiss are consistent with an origin as slightly reworked, dacitic tuff. Results of mapping by St. Joe Resources Company geologists (including deLorraine) are best interpreted as two distinct carbonate units separated by the Major Gneiss. The basal marble, here termed the Gouverneur marble type, directly overlies the leucogneisses and comprises the Engels' Black Lake, Gouverneur (Lower Marble), and Harrisville-Pitcarin marble (part of the Balmat-Edwards, or Upper Marble of the Engels). Major Gneiss overlies this marble and, in turn, is overlain by an upper marble, hereby called the Balmat-Edwards marble type. This model is similar in some respects to that of Lewis (1969).
The purpose of this field trip is to investigate regional stratigraphy and structure from the perspective given here. We will point out numerous areas where further investigation is needed, particularly with regard to the role of magmatism during (before?) metamorphism. We will also discuss the origin of some of the gneissic rocks in view of recent geochemical data.

STOP 1. New roadcut on Route 812 north of Harrisville near bridge over Oswegatchie
We start our trip in the Harrisville-Pitcarin marble belt adjacent to the Highlands - Lowlands boundary which lies just to the southeast. Marbles here belong to the Lower marble belt (Gouveneur marble type) and overlie the Clark Pond leucogneiss body which lies to the southwest. Formerly, this belt was included in the Upper or Balmat-Edwards marble belt of the Engels. These marbles consist of coarse-grained, light gray and white, banded, graphitic-calcitic marbles with accessory brown tourmaline, local chondrodite and diopside. A thin layer of Major Gneiss between Geer's Corners and Pitcairn separates the Lower (calcitic) marble from the Upper (silicated-dolomitic) marble to the north toward Fullerville and Balmat. Note the lobate form of the intrusive body of quartz-syenite exposed on the right-hand side of the outcrop.

STOP 2. Zinc and Talc mines
STOP No. 2A. St. Joe Resources Co. #2 Mine area at entrance to Balmat #2 mine, Route 812, Gouverneur quadrangle.
Exposed here in the core of the Balmat syncline is unit 14, one of 15 carbonate units comprising the stratigraphic section at Balmat. Overall plunge of the syncline (overturned) is NNW. Note the profusion of isoclinal folds, rootless fold hinges, transposed layering, and fragmented silicate layers in marble. Look for bladed tremolite clusters, diopside, quartz, serpentine, and dolomitic and calcitic marbles. Contrast the composition of this marble with that at STOP 1. Nearby is the old #2 mine-mill complex, now unused because milling operations have shifted to the new #4 mine area. However, #2 shaft still serves as an access and escape route for the #2 mining area. This is the site of original mining in the Balmat district, having begun in 1930, although sphalerite showings were reported as early as 1838 by Ebenezer Emmons.
STOP No. 2B. Area to right of gate at entrance to #2 mine area; old American Talc shaft.
Exposed here is Unit 13, a talc-tremolite-anthophyllite schist. Suggested by Engel (1962) as a shear zone metasomatically enriched in Mg, it more likely is a siliceous meta-evaporite unit. Its distinctive appearance, composition, and continuity make it an excellent marker for use in unravelling the structure and stratigraphy of the Balmat district (deLorraine, 1979). This rock is mined for use primarily as paint filler and for use in ceramics.

STOP 3. Pump house road, Sylvia Lake
Entrance at Gouverneur Talc Co. parking lot. Proceed down road almost to lake; park near dirt road with gate on right.
Units 11 and 12 are exposed here. Unit 12 is a relatively pure dolomite marble. Unit 11 is representative of most of the silicated dolomitic marble units in the district and is composed of well-layered quartz-diopside (est. 50-65%) and dolomite with minor interlayers of calcitic marble. In a nutshell, Balmat stratigraphy is characterized by alternating pure dolomites (such as Unit 12) and silicated dolomitic marbles (such as Unit 11) for a total of 15 carbonate units. Anhydrite is also important; a large body underlies Sylvia Lake

STOP No.4. Popple (Poplar) Hill migmatite
Best exposure of major gneiss in the northwest Adirondacks. A good introduction to problems of origin for migmatite and for the protolith of a widespread rock type in the Canadian Shield. This oligoclase-K-feldspar-quartz-biotite, sometimes sillimanite-garnet gneiss lies between the carbonate units and is traceable for more than 70 km from Philadelphia, New York to Colton. It is consistently gray and fine-grained except where strewn with convolute quartzo-feldspathic veins, boudins, K-feldspar porphyroblasts, amphibolites and thick sill-like bodies of leucogneiss, all of which are visible at this outcrop.
Carl (1981) believes that much leucosome is locally derived and not introduced from outside sources. He disagrees with conclusions reached by Engel and Engel (1960 a,b) that the effects of metasomatism are increasingly pronounced to the northeast where metamorphic grade approaches granulite conditions (Stoddard, 1981). Changes in rock chemistry occur over short distances as is illustrated at this outcrop. It is not easy to demonstrate changes of a more gradual nature over great distances.
We will point out disruptive contacts between banded gneiss and massive, subporphyroblastic rock that contains angular fragments (xenoliths?) of darker rock like that found in Hermon gneiss (see our "optional stop"). deLorraine first recognized this rock last summer, which illustrates either 1) that the second decade of examining the same rock outcrop is most informative, or 2) that the rest of us are essentially blind. This massive rock is more mafic, less potassic and is enriched in Sr, Yt Ba, and Th relative to banded gneiss (Table 1). Rb content is about the same. Note that the high Ba and Sr content of massive rock is also a characteristic of its K2O-enriched leucosome.
Amphibolites are generally conformable and in sharp contact with banded gneiss. They contain biotite-selvaged leucosome that resembles its host in plagioclase content and low Ba and Rb.
Leucosome in banded gneiss is of granitic composition with K-feldspar dominant over plagioclase and 25-35% modal quartz. Like the host gneiss, leucosome is enriched in Ba, Rb and Sr. Textures range from xenomorphic granular to strongly flaser and cataclastic. Porphyroclasts are surrounded by wreaths of mortar similar to that surrounding K-feldspar augen in the Hermon gneiss. A possible mode of origin is that of partial melting along shear zones at some early stage of metamorphism and folding.
What was the protolith of the major gneiss? Perhaps dacite volcanics that were slightly weathered and reworked as proposed for paragneiss in NW Ontario by van de Kamp and Beakhouse (1978). There is at least one locality where cross bedding seems preserved. Sillimanite content is variable and may occur as thin lenses or in thin sections, but Al2O3is generally low for a shale. Harker diagrams show igneous trends (except for Na and K) and the rock lacks enough CaO, Cr and Ni to represent the composition of many graywackes. An Na/K ratio of 1.0 is obtained instead of 1.2-1.4 characteristic of graywackes when leucosome is included in an assessment of average outcrop composition (Carl, 1981). The massive rock at the Popple Hill outcrop with its more mafic chemistry may represent a volcanic feeder for material now incorporated in the adjacent banded gneiss.

STOP 5A. Small outcrop on north side of road, "Steer's Head"
Gouverneur marble and gray, granitic intrusive rocks exposed here. Note the light gray inclusion of marble (shaped like a steer's head) in the darker gray granitic rocks. Similar gray granitic rocks are well exposed along Route 11 as far south as Antwerp; this string of granitic bodies extends as far northward as Moss Ridge on the Bigelo quadrangle. North of Battle Hill at the south end of Moss Ridge (Gouverneur quadrangle), the gray gneiss undergoes a transition from gray to splotchy gray and red, to pink/red granite. Its red coloration north of Battle Hill causes the unit to resemble the basal leucogneisses. We suggest that Moss Ridge is the northerly extension of the granite intrusive belt and probably constitutes a sill-like body within Gouverneur-type marbles. As such, it is unrelated to the basal leucogneisses as was proposed by Foose (1974). Moss Ridge also lacks a pronounced positive magnetic anomaly that is common to other leucogneiss bodies.

STOP 5B. "Train wreck" Outcrop - Fragments of "basaltic" rock in Gouverneur marble.
Clustering of blocks and their rectangular outline suggests disruption of a basaltic dike during folding. Mineralogy of the dike, however, is adjusted to metamorphic conditions. Plagioclase is absent in contact zones in the dike rock which contains meionite scapolite, diopside, microcline, sphene, tremolite, biotite, quartz, tourmaline and apatite. This roadcut also contains a basalt dike that is not disrupted.

STOP 6. Hyde School leucogneiss and amphibolite at the southwest end
STOPs No.6 and 7. The Hyde School "alaskite" body: leucogneiss and amphibolite at the southwest end, and tonalite at the northern edge along the Hyde road, Pope Mills quadrangle.
The Hyde School is the best exposed of several domical leucogneiss occurrences in the Northwest Adirondacks. Many years ago A. F. Buddington proposed that the gneisses represent granitic intrusions into anticlinal crests (phacoliths) during Grenville folding and metamorphism. The Hyde School body, however, is anything but a simple dome. Isoclinally folded and refolded amphibolite layers are shown to mimic the larger structures, and there is evidence that all "domes" are protruberances of a single, multiply-folded, lower stratigraphic unit present throughout the lowlands. The Hyde School body has been recently mapped by Erv Brown.
The blunt, southwesterly-plunging end of the Hyde body overlooks a solution valley in the surrounding Lower Marble unit. Amphibolites interlayered with leucogneiss (alaskite) are virtually undisturbed at this locality. Some are broken with coarse-grained quartz and feldspar occupying the break. Extension in the direction of plunge or laterally in the plane of foliation produced tension within these relatively competent layers.
Carl and Van Diver (1975) recognized a stratigraphy of sorts within the leucogneiss and made comparisons of major element chemistry with ash flow tuffs. The presence of dark tonalite-trondhjemite gneiss units within a dominantly granitic gneiss sequence was compared to the capping of ash flow tuff sequences by later, more fluid, plagioclase-rich extrusives. The lower parts of ash flow sequences have rhyolitic tuffs derived from the uppermost, most differentiated portion of the underlying magma chamber. The plagioclase cap rock represents a later outpouring of more fluid magma at greater depth. The stratigraphic sequence on the surface, thus, represents an inversion of the zonation that existed in the underlying magma chamber (Figure 3).

STOP 7. The Hyde School tonalite at the northern edge
Units of tonalite-troudhjemite occur along the western margin of the Hyde School exposure and in the center of the southern dome. If these are truly the cap rock of ash flow tuffs, then a walk northwardly along the Hyde road is upward in the stratigraphic sequence. It is also a look deeper into the magma chamber that gave rise to that sequence.
Support for an ash flow tuff origin has recently come from geochronology studies of Bob Lepak (1983) and Tom Maher (1981), students of Norman Grant at Miami University of Ohio. They find a crystallization age for precursors of the leucogneiss at 1263 + 25 Ma and an initial 87Sr/86S ratio of 0.7033 + 0.4. Samples with high Rb/Sr ratios give evidence for open system behavior of Sr that is proposed (by other workers) to have occurred in silicic volcanics. This Sr loss is attributed to factors such as the reordering of K-feldspar structural state during cooling of the tuffs, or by Sr loss in fluids prior to or during metamorphism.
Carl has analyzed rock samples taken along the Hyde road from granitic leucogneiss into the tonalite-trondhjemite unit. Chemistry is given with respect to lithology in Figure 2. Note the change from siliceous to more mafic chemistry toward the plagioclase unit and an "upward" increase in MgO, CaO, Na2O, TiO2, Ni, Cu, Sr, and Ba. There is a decrease in SiO2, K2O, Rb, Y, Zr, Nb, Pb, and Th. Analyses by Calvin Pride, University of Ottawa, show less total rare earth element content (and no negative Eu anomaly) in the caprock than in the underlying leucogneiss. The caprock is slightly enriched in light REE relative to heavy REE than is the underlying leucogneiss (La/Yb ratios of 9.7 vs. 8.0).
These trends are remarkably similar to those recorded in a vertical sequence of the Bishop Tuff in California by Wes Hildreth (1979). The lower, siliceous part of that sequence is enriched in the small, highly charged cations Y, Nb, Th, and La. It is also enriched in Rb and has a strong negative Eu anomaly. Ba and Sr enrichment occurs in the more mafic caprock. In contrast to the leucogneiss sequence, however, Hildreth reports the caprock enriched in K over Na (odd!) and in Zr content.
Large portions of the leucogneiss sequence must have been rapidly extruded and deposited as is the case for individual flows in a tuff sequence. Deposition of other portions, however, must have occurred intermittantly and in water because of interlayering with numerous thin amphibolites (mafic tuffs?), calc-silicates and garnet-sillimanite gneiss. Extensive compaction, recrystallization and folding evidently obliterated all textural evidence of the precursors.

5: THE TRENTON GROUP OF THE BLACK RIVER VALLEY
Robert Titus
Hartwick College

5: THE TRENTON GROUP OF THE BLACK RIVER VALLEY

STOP 1. Park beyond bridge which crosses Mill Creek.
About 90 m of the Trenton Group are exposed at this location. The 16 m of strata below the bridge display the upper Kings Falls Limestone and all of the Sugar River Limestone. Upstream there is a complete exposure of the Denley Limestone. There is only one short break in the section. Finally, the entire Steuben Limestone can be seen along the upper reaches of Mill Creek. The Steuben Limestone begins just below the quarry. Thus, most of the lower Trentonian transgression and all of the middle Trentonian regression are represented at this location.

STOP 2. Park beyond the bridge which crosses the Deer River.
About 17 m of the uppermost Trenton Group Hillier Limestone is exposed here. This may be the most complete section of the Hillier Limestone. The rocks become progressively more micritic towards the top reflecting deepening seas. The outcrop thus records the upper Trentonian transgression.

6: A FEW OF THE BEST OUTCROPS IN THE NORTH COUNTRY
BY
James D. Carl, S.U.N.Y. Potsdam

STOP 1. Trinity Episcopal Church, and a walk into the Potsdam business district.
Our tour will begin with Fall Island and Trinity Church and will include a short walk downtown. The community has recently been chosen for a Main Street award for its Market Street renovation project. A number of buildings have been restored or built for compatibility with the architecture of the late 1800s, the period of greatest construction in the village. This two-block section of Market Street and a portion of Raymond Street were placed on the National Register of Historic Places in 1979. Here are sandstone and brick buildings (some marble trim) of Italianate and Greek revival and other styles including the simple slab construction of the earliest commercial sandstone building (1821) that houses Eugene Earle, Jeweler. Note also, the slab and binder construction (1840) of Page One Bookstore.
Background
Little was known about the northern Adirondack region at the close of the Revolutionary War. Carlton Island and Fort Oswegatchie (Ogdensburg) were still occupied by the British, and the north shore of the St. Lawrence River was dotted with settlements of Tory refugees and their families. According to Marguerite Chapman (1969), downstate New Yorkers felt the need to establish a buffer region between English Canada and the Mohawk Valley. Settlements south of the St. Lawrence River would act as a deterrent and give warning of potential invasion from the north.
The state legislature acted to provide for the sale of wilderness land and to appoint land commissioners for its disposal. Townships of 100 square miles were created instead of the 36 square mile block adopted by the Federal government in 1785 as the fundamental surveying unit for western lands. Evidently the state government was reluctant to set up the administrative machinery necessary to sell the land in small parcels. An act of May 25, 1787, established five townships along the south shore of the St. Lawrence River and five to the south of these. Following good advertising procedures the land commissioners named some of the towns after old world cities: Louisville, Stockholm, Potsdam, Madrid, Lisbon, Canton, DeKalb, Oswegatchie, Hague (Morristown), Cambray (Gouverneur).
Public notification of the forthcoming land sale was notoriously and perhaps deliberately hurried. The announcement first appeared in the Albany Gazette on June 7, 1787, for a sale which was to be held on the 10th of July in New York City. Millions of acres were sold for a fraction of their value with a Detroit fur trader-turned-land speculator, Alexander Macomb, buying the lion's share of the pot (3,670,715 acres). Surveying, division and sale of Macomb's purchases began immediately, but evidently did not offset other financial problems because Macomb was imprisoned for debts in the 1790's. Among those solicited for land purchases were the royalty and wealthy of France. The Revolution in America was over. Northern New York promised beaver, wild grapes, maple syrup and even friends of like mind (?) and language in Montreal, a "short" boatride down the St. Lawrence River. Winters were not discussed in detail.
The town of Potsdam was eventually sold to Garrit Van Horne, David M. Clarkson and their associates on November 18, 1802. The saga of the Clarkson family from Bradford County, York, England, begins in the North Country along with the Episcopal heritage represented by this church.
Trinity Church
In early years of the Village, a small frame building on Union Street served as a school during the week and as a community church on Sunday. By the l820s and early 30s Potsdam was a thriving community with buildings lining both sides of Market Street and stately sandstone houses along Main and Elm. Common worship of the early settlers had given way to organization and construction of churches such as that of Baptists, Methodists, Presbyterians and Universalists. Episcopalians were meeting at the St. Lawrence Academy, a three-story structure, 68 by 36 feet, built in 1825 of Potsdam sandstone and located on the site of the north end of Snell Hall on the downtown campus of Clarkson College.
Although the first Episcopalian priest is said to have visited the county in 1816, the first resident priest was called in 1834 with at least three members of the Clarkson family pledging funds for his support. The Reverend Richard Bury arrived from Ogdensburg, and the parish was formally organized under the name of Trinity Church on March 23, 1835.
The site chosen for construction of a church was Fall Island adjacent to and on the south side of the Parishville Turnpike Road. Thomas Clarkson offered stone from his quarry, free of charge, for the "neat gothic edifice of stone 44 by 64 feet." The original design for the building and name for the parish was taken from Trinity Church constructed in 1788 in New York City. The name also emphasized, for good measure, a theological distinction between Episcopalians and local Universalists. The building was completed and consecrated on a warm July afternoon in 1836. A procession that began at the Academy Was concluded with a sermon by Rev. Bury on Fall Island. An engraving of the church as it appeared in 1836 (Figure 1) shows that the church lacked the tall steeple possessed by its namesake in New York. Windows were plain glass, and the high-backed, rented pews were complete with doors. Colorfull upholstering was installeded by pew renters accustomed to long services, ana several pews were reserved for "strangers."
The side walls are about all that remain of the original structure. These walls consist of horizontal layers that alternate rows of flat-faced sandstone blocks (slabs) whose bedding is laid horizontally with rows of blocks (binders) whose bedding is laid vertically. This layer by layer alternation added style and texture to a smooth wall and was said to give added strength. Compare the slab and binder construction with that of strictly flat slabs in the Earle Jewelers building on Market Street.
The simplicity of architectural style of this early church was not acceptable in the second half of the 19th century. Victorian tastes in these parts leaned toward "roughened" (ashlar) stone construction whereby soaring walls of massive stone could be topped or garnished by highly carved stone or wrought iron decoration. The ashlar stone fence in front of the church (1867) was a prelude of changes to come. An ashlar chapel was added in 1885 and the present facade was finished in 1886. The towers capped with ornamental stone are a tribute to the skills of quarrymen and stone cutters as well as to the faithful who paid the bills. A new spirit seems to have prevailed in the church. In 1886 the pews were declared free of rent.
Windows were installed and dedicated as donations became available in the l890s. Created by Louis Tiffany and Company of New York, the windows depict the designs of notable paintings such as Holman Hunt's "Christ the Light of the World." The beauty of these windows, accentuated by dark ash ceilings, is most striking from the inside on a sunny day. The present rector of the parish, the Rev. Canon James Pennock, is also mayor of the Village of Potsdam.

STOP 2. No. 1 Quarry of the Potsdam Red Sandstone Company
Much sandstone in buildings throughout the area was taken from quarries that were strung along both sides of the Raquette River south of Potsdam Village. Several sandstone houses (about the size of large log cabins) were built between 1309 and 1820 along the Back Hannawa Road. Much stone was hauled along this road in later years to construct the homes and businesses of Potsdam.
The qualities of Potsdam sandstone were highly praised in the 1850s. The stone was cheap, available and of pleasing red coloration. Elsewhere it may be white or gray. It was also durable and not as susceptable to spalling in case of fire as was granite building stone. Iron furnaces in Ontario and New York State had sandstone lining. Note, say various appraisers, the sharpness of outline in natural exposures that has lasted "several centuries." The stone occurs in even-bedded strata and cleaves into slabs with flat faces and straight edges. There is nothing in the rock to "nourish parasitical mosses." Walls made from this siliceous stone do not become moldy and decaying as is the case with walls of limestone in damp climates. This stone keeps its color, and the claim was made that exposure to air actually hardens it. Perhaps this is over zealous advertising; it may refer to the tight silica cementation that naturally existed once broken and loosened quartz grains were brushed away. This old quarry site is now the property of Niagara-Mohawk Power Co., but sandstone is still taken on occasion for patio or building trim.
Geologic Setting
The Cambrian Potsdam sandstone has been stripped from the Adirondack dome northward to the vicinity of Potsdam Village. Present distribution of that sandstone, however, is uneven. The small park on Fall Island across from the church is underlain by Precambrian amphibolite whereas the Cambrian Potsdam sandstone of No. 1 Quarry is located to the south near the border with the Adirondack highlands.
The Potsdam sandstone is of variable thickness. It was deposited upon an irregular surface of low hills and ridges of resistant Precambrian gneisses or as filling in sinkholes where bedrock consisted of marble. Erosion nearly to the level of that surface has left many sandstone outliers scattered here and there in the Potsdam area and in Precambrian portions of the northwest Adirondacks.
The Raquette River at the quarry site has cut a channel into glacial and deltaic sediment now exposed in the bluffs of Figure 4. The quarry is located within the sandstone outlier that was buried by till deposits during glacial advance and by outwash during glacial retreat. These sediments, in turn, were covered with a layer of magnetite-bearing quartz sand that, in the vicinity of Hannawa Falls, forms a large fan-shaped delta that opens to the north. These sands probably were deposited by the Raquette River when it entered a pro-glacial lake impounded between the highlands to the south and the ice front to the north. Retreat of the glaciers was accompanied by lowering of the lake level, by entrenchment of the Raquette River into the underlying sediments, and by exposure of the sandstone outlier at this quarry. The river at Hannawa Falls, thus, has a relatively steep-walled channel. To the north, however, the braided and meandering channel seems deliberately to avoid disturbing a topography of glacially-deposited hills that consist of ribbed moraine in varying stages of drumlinoid molding (Carl, 1978).

STOP 3. Sand terrace overlooking the St. Lawrence Valley
The transition from Adirondack lowlands to highlands occurs between Hannawa Falls and Colton. Our stop marks the southern boundary of the glacially deposited and overridden hills of the lowlands. Presumably (?) it also marks the southern extent of Fort Covington glaciation. We will walk under the power lines toward the edge of the terrace. Ottawa, the Gatineau hills and the other side of the Valley are out there but too far away to be seen. In language understood by corporate executives, the view from the top is superior, even if incomplete.
This area of transition is also the site of at least three sand terraces, the uppermost here at 800 feet elevation which includes the continuous but slightly higher surfaces (up to 900 ft.) along the Colton-Parishville road to the east. Compare terrace elevations here with those of other St. Lawrence Valley terraces as given in MacClintock and Steward (1965, p. 42). A second terrace remnant is preserved 200 feet below this level along highway 56 near Brown's Bridge road. The third or lowermost terrace begins at 580 feet and slopes northward in true deltaic fashion at Hannawa Falls. The delta ends abruptly at Sweeney Road, Potsdam quadrangle, in a northeast-trending, nearly undissected slope. This slope may represent middleset beds draped over the northeasterly end of a till hill. The contact between deltaic sands and underlying till or kame material is observed in gravel pits throughout the area.
Terrace sands consist of moderately well-sorted, angular, magnetite-bearing quartz sands that include heavy minerals derived from mountains to the south. The sands show cross bedding, channeling, climbing ripples and occasional boulders and gravel lenses. Similar sands underlie flat surfaces at lower elevations to the north including that at a recent housing development in Raymondville. Sand grains here are more rounded and contain less magnetite than at Colton. They were evidently recycled in the Champlain Sea. The uppermost terraces at Colton, Parishville and elsewhere along the Adirondack highland-lowland boundary represent the ancient shorelines of pro-glacial lakes that were impounded by retreating ice to the north. Imagine the view from this terrace at Colton roughly 10,000 years ago.

STOP 4. Gouverneur-type marble about 4 miles west of Canton on highway 11.
Recumbant folding of marble and a thin layer of silicate minerals within that marble. This is th e "snake" outcrop described in Brad Van Diver's book, Rocks and Routes of the North Country, and in field trip 2 of this guidebook. If the spray-paint antics of anguished lovers, religious zealots and fraternity pledges permit, we will observe a diopsidic reaction rim between the marble and the layer whose mineralogy includes quartz, microcline, sphene, phlogopite, pyrite, actinolite and tourmaline. The layer may have originated as air-born volcanic ash.

STOP 5. "Train wreck" outcrop. Fragments of "basaltic" rock in marble.
An outcrop eminently suited for black and white photography. Clustering of blocks and their rectangular outline suggests disruption of a basaltic dike during folding. Mineralogy of the dike, however, is adjusted to metamorphic conditions. Plagioclase is absent in contact zones in the dike rock which contains meionite scapolite, diopside, microcline, sphene, tremolite, biotite, quartz, tourmaline, and apatite. This lengthy roadcut also contains a basaltic dike that is not disrupted.

STOP 6. Popple (Poplar) Hill migmatite
Best exposure of Major Gneiss ih the northwest Adirondacks. A good introduction to problems of origin for migmatite and for the protolith of a widespread rock type in the Canadian Shield. This oligoclase-K-feldspar-quartz-biotite, sometimes sillimanite-garnet gneiss lies between the carbonate units and is traceable for more than 70 km from Philadelphia, New York, to Colton. It is consistently gray and fine-grained except where strewn with convolute quartzo-feldspathic veins, boudins, K-feldspar porphyroblasts, amphibolites and thick sill-like bodies of leucogneiss, all of which are visible at this outcrop. See the discussion for stop number 4 in Field Trip number 4, this guidebook. <br

7: GENERAL GEOLOGY OF THE ADIRONDACKS
Bradford B. VanDiver
S.U.N.Y. Potsdam

STOP 1. Fort Jackson gorge
For about a mile before Hopkinton on 11B, there are open views to the St. Lawrence Lowlands, that give the distinct impression of looking out to the sea over a gently sloping coastal plain. Here, at Fort Jackson, are some clues as to why. The well-bedded and strongly cross-bedded (Keeseville member?) Potsdam Sandstone dips gently northward away from the Adirondack Dome, presumably as a consequence of its geologically recent and ongoing uplift. The gentle slope "to the sea" apparently is the dip slope developed on the resistant Potsdam Sandstone. A few miles upstream in the Nicholville Gorge, the Nicholville Conglomerate rests directly on Precambrian gneisses, and represents either basal Potsdam or a sub-Potsdam unit.

STOP 2. Parking area 8 miles southeast of Santa Clara.
The bedrock cuts here are dark green, massive, syenitic, or mangeritic (pyroxene syenitic) gneiss, like those seen in passing Santa Clara and several more cuts to here. This peculiar rock-type is widely distributed in the Adirondacks, in association with anorthosite, charnockite (hypersthene granite) and various other members of the anorthosite clan. The large erratic boulders placed along the edge of the parking area display some of the other major rock types of the Adirondacks.
This is also a good place to view the low, knobby, glacially-scoured landscape of the foothills country. Extensive glacial polish and striae are visible in exposures about a quarter mile back from the parking area.

STOP 3. Gabriels, scenic camera stop.

STOP 4. High Falls Gorge.
This is a commercial tourist attraction located at the northeast end of Wilmington Notch, where the West Branch Ausable River drops over 100 feet. The river follows the Wilmington Notch fault zone and cascades over a resistant mass of granite (Figure 1). Numerous fractures in the gorge are intruded by diabase dikes that weather in recess. Dikes like these (and sills) are extremely common in the Adirondacks. Sixty-one "were recorded by W.J. Miller in his geologic study of the Lake Placid quadrangle (1919). Though definitely post-Grenville, their ages probably vary widely. Here, for example, they intrude fractures presumably related to the late Ordovician Taconic Orogeny. Elsewhere, as in the Lowlands Adirondacks, many are pre-Potsdam.
The rushing water has produced numerous potholes in the hard bedrock of the streambed, some of very large size.
Similar features may also be seen in the Flume and adjacent roadcut about 2 miles farther east, where N.Y. 86 crosses over the river.

STOP 5. Whiteface summit
The rock of the summit is Whiteface-type metanorthosite. The Adirondack metanorthosite is a large, massif-type, anorthosite body of thick slab-like form that underlies most of the High Peaks region. Its igneous emplacement predates the Grenville Orogeny, and thus, it has been metamorphosed along with nearly all of the other Adirondack lithologies. Most of this large mass consists of a coarse-grained, porphyroclastic facies, called Marcy-type, in which plagioclase porphyroclasts commonly measure several inches in length, and rarely more than a foot. Whiteface lies near the northern border of the mass where, presumably, the shear and chill effects associated with emplacement are responsible for the finer grain size, more gneissic texture, and more gabbroic composition of the Whiteface-type (Figure 2). The structural and petrologic picture, however, maybe considerably more complex, as indicated by Crosby (1968), who considers the rocks here to be part of the Jay-Whiteface Nappe, and who has mapped complex interstratification of Marcy- and Whiteface-types with charnockite, mangerite, other gneisses below the summit. Figure 1 gives a highly generalized picture of the distribution of the major rock types around the mountain.
The effects of alpine glaciation are well represented on Whiteface by several aretes, cirques, and U-shaped valleys downslope from them (Figure 3). In historical perspective, Wisconsin glaciation at climax about 20,000 years ago, covered the Adirondack peaks with a thick blanket of ice. The ice thinned during glacial recession until the higher peaks projected through, but residual ice masses remained in the existing mountain valleys. The resulting alpine glaciers persisted for long enough to carve the distinctive features noted here and present throughout the High Peaks region. In the Catskill Mountains glacial cirques formed contemporaneously are much better developed, owing to the lesser resistance of the sedimentary rocks there, and to their nearly horizontal stratification.
The peculiar, ladder-shape of Lake Placid, and in fact, its very presence, demand further explanation. The lake occupies a system of crossvalleys developed first by stream erosion of fault zones, and then later deepened and widened by ice advance. It is now dammed at its southwestern end around Lake Placid village by moraine.
The role played by Wilmington Notch in pro-glacial lake development can best be appreciated in the view from the summit, From here, it is seen as a very narrow constriction between two large moderately-level lake plains. Figure 4 shows three stages of deglaciation in this region, with ice first blocking drainage through the Notch, and later melting away to permit convergence of the impounded waters on either side of it.
Other features to note from the summit are:
1) Lake Champlain in the distance opposite to the Lake Placid direction.
2) The profile of the High Peaks region in a sweep from southwest (across Lake Placid) to southeast (ca. 900 to left of Lake Placid).
3) Northeast-trending notches and valleys other than Wilmington Notch.
4) Slide stripes on steep, smooth cirque walls, on Whiteface, and on some of the other peaks.
5) Sheeting of the summit rocks.
6) Representative rock types in the retaining wall near the "Castle."

STOP 6. Glacial drift bank on Whiteface highway
This is a bouldery, sandy, well-washed deposit probably best described as a kame, but lacking visible stratification (concealed by slopewash?). Pick around among the fragments to see if you can find some Potsdam Sandstone. What would its presence mean in terms of glacial history?

8: GLACIAL GEOLOGY AND SOILS OF THE ST. LAWRENCE-ADIRONDACK LOWLANDS AND THE ADIRONDACK HIGHLANDS
Michael Kudish

8: GLACIAL GEOLOGY AND SOILS OF THE ST. LAWRENCE-ADIRONDACK LOWLANDS AND THE ADIRONDACK HIGHLANDS

Delta of the West Branch St. Regis River
Delta of the West Branch St. Regis River into Lake Iroquois at the 900-foot level. View of Parishville Desert (STOP 1) to the north (left) across the River.

STOP 1. PARISHVILLE DESERT
According to Van DIver (1976), this is a delta built into Postglacial Lake Iroquois by the West Branch St. Regis River at the 900- foot level. The delta is now deeply dissected, the Desert only a remnant. Much of the material (mostly fine sand) of the delta was probably carried south of Parishville by the ice sheet and then returned north by the River. Sand-blasted ventifact cobbles and boulders are Potsdam Sandstone, Adirondack Highlands gneisses, Canadian gneisses, and Bucks Bridge limestone (a dirty-brown, strongly-weathered part of the Theresa Formation).
Van Diver's hypothesis that upper soil layers have been removed by wind erosion is verified by digging a soil pit: the B2ir horizon is directly under the surface in places, the upper A horizons being absent.
A plantation of Scots (and a few Jack) Plnes has provided the seed source for naturalized reproduction of these species. Other pioneers on the droughty, infertile soil are Gray and Paper Birches, Trembling aspen, White pine, Red maple, Fire cherry, Bracken fern, and Pilose Hair-cap moss.

Note the change in land use
Note the change in land use from existing farms to abandoned farms to forest in only several miles as we cllmb from the St. Lawrence Valley Lowlands to the Adirondack Highlands. The contact between the Potsdam sandstone and the Highlands gneisses is about two miles south of this intersection but concealed by thick glacial drift. Note also the pioneer vegetation on the abandoned farms. Aspens, Balsam poplar, Paper and Gray birches, Red cherry, Serviceberry, Meadowsweet, and White pine. Elevation 800 ft.

Cut in glacial outwash on left (northeast).

First cut in Adirondack Highlands rock.
The 1970 Geologic Map of New York identifies it as "amg," interlayered amphibolite and granitic, charnockitic, mangeritic or syenitic gneisses. Elevation 1060 feet.

Gravel pit in glacial till on left (north) and another pit 0.3 mile further.

Basswood trees in this area.
For this Adirondack rarity, see Figure 1. Basswood indicates rich, fertile soil in the Highlands. Elevation 1300 ft.

The falls are over "amg" just out of sight to the left (northwest).

amg rockcut on south (right). Elev. 1580 ft.

Gravel pit in till on left {north). Another pit at 32.8 miles total.

Several rock cuts in "phgs
Several rock cuts in "phgs" symbol on 1970 Geologic Map of New York. These are charnockitic, granitic, and quartz syenitic gneisses (see also Buddington, 1937).

Rock cut in phgs.
Shallow soils surround outcrops in the Highlands and often Red spruce and Hemlock predominate. On the deeper, well-drained till soils we have Northern Hardwoods (Beech, Yellow birch, Sugar maple).

A Balsam swamp.
Poorly-drained areas lacking Peat moss are dominated often by Fir.

Rock cut in phgs and a till cut at Mileage 36.0. Elevation 1650 feet.

Parking area. Note Northern Hardwoods.

Deep cut in glacial outwash.
At Total Mileage 39.9, the Town of Santa Clara is using another outwash mass for sanding roads in winter.

STOP 2. Black Spruce Bog
Elevation 1450ft. This extensive bog extends to Total Mileage 40.9; stop anywhere along its half-mile length. Note the resemblance to northern Canadian or Alaskan muskeg. Poorly-drained soils are classifled by the U.S. Soil Conservation Servlce as Histosols where at least 51 inches (1.3 m) of organic matter overlies the glacial drift or bedrock. All living plants and trees are fully rooted in the organic matter; no roots penetrate the mineral substrate. The dominant ground cover plants are the Peat mosses (Sphagnum spp.); when these mosses die, they accumulate, decay only partially, become compressed, and create extremely acid (pH 3 to 4) peaty soils. Most mineral nutrients are in limited supply so that the plants which grow here must survive on very low concentrations. A few of the plants have adapted to this environment by capturing insects as a nitrogen supplement (Sundews and Pitcher plants), while most others use mycorrhizal fungi to greatly extend the root absorption surface. Among the spruces in more open areas are Cranberries, Labrador Tea, Bog Laurel, Bog Rosemary, Leatherleaf, and Cottonfrass sedge. See Figure 2 •

First of a series of rock cuts extending for 0.6 miles.
The westerly cuts are in phgs but the easterly are in "hbg", biotite and/or hornblende granitic gneiss (Buddington, 1937).

Rock cut in phgs. Elevation 1645 feet.
From here for the next 4.7 miles, N.Y. 30 crosses a large, rolling outwash plain with numerous cuts and fills across kames, kettles, and crevasse fillings. Much of this area, called McColloms, was burned over in 1903 and earlier, and has been covered with pine plantations.

Rock cut in "a", Marcy Metanorthosite
Rock cut in "a", Marcy Metanorthosite (Buddington, 1953; Davis, 1971). Mountain Pond on the left (northeast) is bounded on the west by an esker and on the east by bedrock. Mountain Pond elevation 1634 ft.

Barnum Pond on the right (west).
Barnum Pond on the right (west). View of Jenkins and St. Regis Mountains beyond, the northwesternmost outposts of the Metanorthosite in the Adirondacks.

STOP 3A. Glacial Till
This cut is in glacial till with a loamy sand texture (average 88,% sand, 10,% silt, 2% clay), consisting mostly of crushed Metanorthosite, gneisses, and Potsdam Sandstone. It is often quite hard and dense, with silt grains cementing the sand and angular gravel fragments into a fragipan. The vegetation above this cut had been cleared for farmland and then was reforested both naturally and by people. The trees and plants you see here are pioneers: we must go to STOP 3B to see natural vegetation on a well-drained till site.

STOP 3B. Northern Hardwoods on Till
This road cut shows a typical soil profile developed in the upper 30 or so inches (0.75m) of well-drained glacial till. Soil can be defined as the zone of interaction between parent material (here till) and forest; it is only about 30 in. thick in most places as few roots penetrate deeper. Because of the sandy nature of the till, the soil which develops in it is characterized by rapid leaching (removal of organic matter and mineral material) from the upper or A horizons and deposition in the lower or B horizons. Such soil profiles developed in sands are very colorfully banded although infertile and are called Spodosols (formerly Podzols). The soil series here is Becket, a Typic Fragiorthod, family coarse-loamy, mixed, frigid. The C horizon is unaltered till in its original state, underlies the soil rather than is a part of it, and is not visible here without further excavation.
The forest which develops on well-drained tills such as Becket soils is a Northern Hardwoods Forest with Beech, Yellow Birch, and Sugar maple dominant. Walk up the old log road to the left (north) of the cut for a quarter of a mile or so to see this forest. Other trees are Striped maple, Hemlock, Red spruce, and perhaps Black cherry. See Figure 3.,
The elevation at the road cut is 1680 reet. Marcy Metanorthosite outcrops on the summit of 1863-foot nearby Beech Hill.
Common ground cover plants are Spinulose woodfern, Wood sorrel, Clinton's lily, Canada mayflower, Starflower, Wild sarsaparilla, and Purple trillium. Humus pH averages 4.5 to 4.,7 under Sugar maple.

STOP 4. Glacial Outwash
Park on the shoulder at the intersection of Route 30 and the Keese Mills Road which diverges to the right (west). Paul Smith's College Campus and Route 30's junction with Route 192 are adjacent. More extensive cuts in glacial outwash are present on campus and we can observe them if time permits. Elevation of junction of Routes 30 and 192 is 1658 feet. See Figure 4.
This cut is in glacial outwash with a sand texture averaging 96% sand, 3% silt and 1% clay. The deposit, made by a meltwater stream flowing to the southwest, consists of the same kinds of crushed rock as are found in the area tills, but with most of the silt and clay carried away in suspension. Due to the inadequate quantity of silt, sand and rounded gravel particles are not cemented together into a fragipan. Our Campus is built upon a series of kames as part of a valley train. Numerous dry kettles and kettle ponds are found locally. The thickness of the outwash valley train, as determined by water well data, ranges from zero at out- crops to over 165 feet (50.3 m): the average thickness on Campus is 60 to 100 feet (18.3 to 30.5 m). The valley train extends for 23.5 miles (38 km) southwest from Loon Lake to Fish Creek Ponds, with Paul Smiths about midway. The highest elevation of these sands at the College is between 1680 and 1700 feet so that any higher hills project above this sea of outwash as rock islands mantled with till. Taking isostatic rebound into effect, the original southwest slope of the train seems to have averaged about 5.8 feet per mile (Kudish,. 1975,1981).
The soil profile which develops on well-drained outwash sands is also a Spodosol. Because of the still coarser texture, the rate of leaching from the A horizons and the rate of accumulation in the B horizons are greater than in the tills. These out-wash soils, with less silt and clay, are even more infertile than their till counterparts. Drainage on the kames and other valley train features can be excessive and plants can wilt during long summer droughts. The sand grains of the B2ir horizon are often cemented by iron and aluminum sesquioxides (Fe2O3 and Al2O3},leached down from the gray A2 horizon above, creating a dense red-brown hard layer called an Ortstein. Just as fragipans occur locally only in tills, Ortsteins occur only locally on outwash. The critical concentration of silt appears to be about 6%.
The soil series here are Wallace (with Ortstein) and Adams (without); they are Typical Haplorthods, family sandy, mixed, frigid.
Climax vegetation on outwash consists of trees which can survive on nutrient-poor, drought-prone sands; the forest type is a mixed woods (mixed broadleaf and evergreen species) dominated by Red spruce, Yellow birch, Balsam fir, Red maple, and Hemlock. White pine follows disturbances and Red pine occurs on sites where wind exposure prevents other trees from surviving. Ground cover is very much like that on till soils, but humus pH is even more acid-- pH 4.0 commonly. Under the more open Red pine stands, commonly on the east shores of lakes, less shade-tolerant species occur: Blueberries, Huckleberry, Wintergreen, Trailing arbutus, Serviceberry, Sheep laurel and Bracken fern.

9: LOWER ORDOVICIAN STRATIGRAPHY AND SEDIMENTOLOGY, SOUTHWESTERN ST. LAWRENCE LOWLANDS
Bruce W. Selleck
Dept. of Geology, Colgate University, Hamilton, NY 13346
The Potsdam Sandstone and overlying Theresa Formation of the southwestern St. Lawrence Lowlands record the initial transgression of marine waters into the region during latest Cambrian to early Ordovician time (Fisher, 1977). The Potsdam Sandstone is widespread throughout the peripheral Adirondack region of northern and eastern New York, but is highly variable in thickness, composition and environments of deposition. In the area of this fie1dtrip (Figure 1), the Potsdam Sandstone (In this region, all of the Potsdam is referable to the Keeseville Member of the Potsdam Sandstone, Fisher, 1968, 1977.) can be subdivided into a lower and upper facies. The lower Potsdam consists dominately of flat-bedded medium- to fine-grained quartz arenites with occasional cross-stratified units of varying scales. The lower facies lacks both body and trace fossils. A variety of red-pink coloration patterns are common in the lower Potsdam, making it a desirable building stone in northern New York. The lower Potsdam in this region is dominately shallow marine in origin, but locally aeolian dune, beach and braided fluvial facies are present.
The upper portion of the Potsdam Sandstone consists of alternating burrowed and flat-bedded slightly calcareous sandstones deposited in a shallow subtidal to low tidal flat setting.
The overlying Theresa Formation consists of three informal subdivisions: lower Theresa thin-bedded calcareous siltstones of intrashelf lagoon origin; middle Theresa interbedded bioturbated dolomitic sandstones and cross-laminated quartz sandstones deposited in a shallow subtidal to low tidal flat environment; and upper Theresa sandy dolostones, dolomitic sandstones and calcareous siltstones of high tidal flat origin.
Biostratigraphically diagnostic macrofossils are absent throughout both formations in this area, although late Tremadocian conodonts have been reported from the Theresa-correlative March Formation in Ontario (Greggs and Bond, 1971). The extremely low faunal abundance and diversity may indicate that high and/or fluctuating salinities were prevalent in these shallow marine peritidal environments.
In the course of the trip, we will cross the so-called "Frontenac Axis", a region where Proterozoic rocks outcrop in a northwest-southeast trending belt, providing a connection in surface exposure between the Adirondack Lowlands and the Grenvillian Canadian Shield to the northwest. We will view the stratigraphic section in descending order as we drive southwest from Morristown to Alexandria Bay, New York, paralleling the St. Lawrence River. The Thousand Islands of this section of the St. Lawrence River are largely held up by Proterozoic gneisses and quartzites, although the larger islands (Wellsley, Grindstone) expose the mantling Potsdam Sandstone.

9: LOWER ORDOVICIAN STRATIGRAPHY AND SEDIMENTOLOGY, SOUTHWESTERN ST. LAWRENCE LOWLANDS

STOP 1. Roadcuts on both sides of Rt. 37
Roadcuts on both sides of Rt. 37 expose the high tidal flat facies of the upper Theresa Formation. The basal beds at this exposure consist of vuggy, sandy dolostones deposited as upper intertidal mudflats. A thin unit of laminated calcareous siltstone of tidal pond origin overlies the vuggy dolostone. The remainder of the section consists of dolomitic sandstones with abundant vertical and U-shaped burrows alternating with less bioturbated cross-laminated sandstones. These facies represent middle to high tidal flat sands. Quartz- and calcite-infilled voids in the sandy dolostone unit may document the former presence of evaporite (gypsum/anhydrite) nodules.

STOP 2. Middle portion of Theresa Formation
The rhythmic interbedding of yellow-white cross-laminated quartz sandstones and darker, bioturbated dolomitic sandstones is typical of this portion of the Theresa Formation. Rare mudcracks are present within the yellow-white sandstones. The dolomitic sandstones represent shallow subtidal to lower inter-tidal muddy sand flats that supported an abundant infauna. The yellow-white cross-laminated sandstones were deposited as slightly topographically higher mid-tidal flat sand bodies, upon which benthic fauna could not persist due to active current reworking and/or subaerial exposure to the substrate.
The sharp basal contacts of the bioturbated facies with underlying cross-laminated sandstones may indicate that the rhythmic alternation is due to a series of successive slight relative sea level rises of 2-3 meters. Thus, each bioturbated dolomitic sandstone-cross-laminated sandstone pair can be interpreted as a single shallowing upward sequence.
A peculiar "wavy-bedded" unit near the northeast end of the outcrops appears to have resulted from intraformational soft-sediment deformation. Note the general low-amplitude folding and small high-angle fault in the exposure.

Lower Theresa Formation and upper Potsdam Sandstone
Long roadcut exposing lower Theresa Formation and upper Potsdam Sandstone near Oak Point, New York.

STOP 3. Basal Theresa Formation and Uppermost Potsdam Sandstone.
The contact between the Potsdam Sandstone and lower Theresa Formation is prominently displayed at this stop and is marked by a color change (Potsdam = grey-white-yellow; Theresa = grey-brown), an abrupt increase in carbonate content in the basal Theresa, and changes in bedding style. The lower Theresa in this area consists of 2- 10 cm beds of plane-laminated or low angle cross-laminated calcareous fine sandstones/siltstones regularly interbedded with bioturbated calcareous fine sandstones/siltstones. Subvertical escape (?) burrows commonly traverse the plane-laminated beds and record attempts by deposit-feeding fauna to return to the sediment surface following a sudden influx of sediment. The environment of deposition of this basal Theresa facies is interpreted as a subtidal protected intrashelf lagoon characterized by sporadic periods of sediment influx (plane-laminated beds) followed by periods of quiescence of the substrate, allowing colonization by deposit feeders (bioturbated beds). This facies is limited in extent in the region, apparently because of the distribution of basement ridges of Proterozoic quartzite which acted as wave and current barriers. To the south and west of this area, coarser, bioturbated sandstones resembling those seen at STOP #2 occupy the basal Theresa Formation.
The upper Potsdam Sandstone at this top consists of a series of units of bioturbated calcareous medium-grained sandstones and plane-laminated to small-scale cross-laminated calcareous medium sandstones interbedded on a scale and style resembling the middle portion of the Theresa Formation seen at STOP #2. Alternating shallow subtidal (bioturbated sandstones) and low intertidal (plane-laminated to small-scale cross-laminated sandstones) environments are similarly inferred.
The interesting trace fossil Diplocraterion yoyo is ubiquitous in the Potsdam Sandstone here. The forms are generally indicative of a response to growth and/or erosion of the sediment surface. The generally vertical orientation of these and other burrows is typical of burrows found in modern settings where organisms live within the sediment for purposes of protection from wave and current violence or dessication. This burrow style contrasts strongly with the generally horizontal traces seen in the basal Theresa Formation. Fragments of the inarticulate brachiopod Lingulpis accuminata are common in both the upper Potsdam Sandstone and lower Theresa Formation at this stop.

STOP 4. Contact between the lower Potsdam and upper Potsdam
The contact between the lower Potsdam and upper Potsdam lithofacies is exposed at this road cut on the southwest side of Rt. 12. The lower portion of the outcrop consists of pink-yellow plane-bedded and crossbedded medium-fine sandstones typical of the lower Potsdam. The upper, massive calcareous sandstone bed is riddled with burrows, including Diplocraterion yoyo, and resembles some beds of the uppermost Potsdam seen at STOP 3. The bioturbated upper Potsdam is again interpreted as a shallow subtidal to low intertidal sand flat environment. The lower Potsdam here is likely a subtidal shelf sand, but the lack of burrows and other diagnostic primary structures preclude a definitive paleoenvironmental reconstruction.
Interestingly, the contact between these two lithofacies at this stop (and throughout this area) appears to represent a period of widespread emergence as documented by shrinkage cracks in the sandstones immediateLy below the contact and lenses of brecciated sandstones that are interpreted to result from breakup of a silcrete-like cemented soil horizon.
Glacially striated and chattermarked surfaces are observable on the northwest side of the road.

Beginning of series of excellent exposures of Proterozoic gneisses.

STOP 5. Proterozoic / Potsdam unconformity
The unconformity between the basal Potsdam Sandstone and underlying Proterozoic basement gneisses is exposed in this roadcut on the southeast side of Route 12. This contact represents a time interval of some 600 million years. The basal sandstones here exhibit large-scale low angle planar-tabular cross bedding, and are devoid of trace and body fossils. The depositional setting for this facies is problematic, although shallow marine tidal inlet, beach or aeolian dune environments are potentially workable facies models.
Considerable variation in color pattern is evident in the Potsdam Sandstone, with the basal 0.5-1.0 meters white to light grey in color, whereas the upper portion of the outcrop exhibits the pink, red, orange and salmon colors often seen in the Potsdam Sandstone used as a building stone. In this section, the deeply colored beds contain abundant tiny (2-50 micron) disseminated hematite and leucoxene crystals with these pigments both surrounding detrital quartz grains and imbedded in later authigenic silica cement. Highly corroded grains of detrital magnetite and ilmenite in the colored sandstones appear to have been the source of iron and titanium which subsequently precipitated as hematite (probably with a goethite precursor) and leucoxene under oxidizing diagenetic conditions. The white sandstones immediately above the unconformity contain no hematite or leucoxene, although limonite-goethite halos of relatively recent origin are locally developed around magnetite grains. The pristine condition of the majority of magnetite and ilmenite grains indicates that these basal sands never suffered a persistent oxidizing diagenetic history. The proximity of these unoxidized grains to the underlying pyritic gneisses suggests that the pore waters near the contact were "Eh-buffered" by the alteration of pyrite and Fe-silicates in the gneisses, thus preventing breakdown of the magnetite and ilmenite, and the subsequent precipitation of pigmenting agents.
Note that the sole surface of the lowermost sandstone bed mimics the shape of the underlying (now weathered) basement erosional surface.

STOP 6. Typical Lower Potsdam Sandstone
The roadcut on the southwest side of Route 12 exposes typical lower Potsdam Sandstone. Flat-bedded medium- to fine-grained sandstones underlie and overlie a 1 meter thick bed of tangentially cross-stratified medium sandstones. The dominant cross-bed dip direction is nearly due south. Immediately above the thick cross-stratified unit smaller-scale cross-beds dip to the north.
As with many exposures of the lower Potsdam Sandstone, assignment of an environment of deposition is difficult here. Although the flat-bedded sandstones lack trace or body fossils, a shallow marine subtidal environment is suggested by the continuity of individual beds, the lack of upward fining or coarsening trends and the lack of obvious channel form geometry. However, definitive diagnostic primary structures are absent. The large cross-stratified unit, produced by a bed form of at least 2-3 meters in amplitude (stoss-side erosion beveled the upper portion of the structure as it migrated, leaving behind a scoured lag deposit of granules at the updip termination of the cross-strata), could have been deposited by a large subtidal sand wave, or an aeolian dune during a period of emergence.

STOP 7. Angular Proterozoic / basal Potsdam unconformity
STOP '7. The angular unconformity between the basal Potsdam Sandstone and Proterozoic gneisses is again exposed in these large roadcuts on both sides of N.Y.S. Route 12. The dominant facies present here is typical of the lower portion of the Potsdam throughout the southwestern St. Lawrence Lowlands. Flat-bedded medium- to fine-grained quartz arenites are occasionally interrupted by 0.2 to 1.0 meter sets of cross-strata. The lack of diagnostic trace and body fossils is a nettling problem if we assign a shallow marine environment of deposition to this facies.
Note the "weathered zone" at the unconformity. Does this represent a "regolith" or buried soil horizon: or is another explanation more viable? Note also the general absence of clasts of the underlying gneiss in the basal Potsdam Sandstone.

FIELD TRIP GUIDEBOOK
Donald B. Potter, Editor
Hamilton College
Clinton, New York 13323
Printed at Hamilton College for the New York State Geological Association. Additional copies may be obtained from the permanent Executive Secretary, Fred Wolff, Department of Geology, Hofstra University, Hempstead, NY 11550

AB2a: CROSS SECTION OF THE LOON POND SYNCLINE, TUPPER LAKE QUADRANGLE, NEW YORK
D. B. Potter, Jr.
Department of Forestry and Geology
University of the South
Sewanee, TN
This field trip crosses the Loon Pond Syncline, an area mapped during the summers of 1978, 1979, and 1980 under the direction of Leo Hall at the University of Massachusetts. The syncline, a northeast-trending elongate basin, was named and first mapped by Buddington and Leonard (1962) as the northeast part of the Bog River Synclinorium (Figure 1).
The syncline occupies most of the southern half of the fifteen minute upper Lake Quadrangle, which lies in the central Adirondacks within the Adirondack Highlands region. The Arab Mt. Anticline, composed of charnockitic gneisses, lies to the north, and the Salmon Lake Anticline lies to the south (Figure 1).
The stratigraphy of the syncline is distinctive. In contrast to most of the Adirondack Highland rocks which are chiefly orthogneisses and anorthosite, a great deal of quartzite, marble, and calc-silicate rock as well as quartzo-feldspathic gneisses constitute the rocks here. In this respect the rocks of the Loon Pond area are similar to those of the Northwest Lowlands (Figure 1). Erosion of the multiply deformed rocks has exposed a structural basin which shows some similarity to the Darning Needle Syncline in the Cranberry Lake Quadrangle (Leavell, 1977).
Access: Route 10, linked to Route 30 by Route IDA, extends west across the field area to the old Sabattis Railroad station and provides the primary access to the sparsely populated region (Figure 2). With the exception of a clear area south of Sabattis that burned in 1903, the region is heavily wooded. Topographic relief is about 800 feet.

AB2: CROSS SECTION OF THE LOON POND SYNCLINE, TUPPER LAKE QUADRANGLE, NEW YORK

View of Loon Pond Mountain to the northwest.

Small outcrops of East Charley Pond Gneiss on both sides the road.

Cross bridge at the head of Little Tupper Lake.

STOP 1. Otter Pond Dioritic Gneiss
Otter Pond Dioritic Gneiss is exposed along the north side of the road. Near the east end of the outcrop, a late 1 meter-thick vertical dike cuts the foliated gneiss. Discontinuous quartz veins help define the edges of the northtrending dioritic dike.
Estimated modes from thin sections of the foliated gneiss at this outcrop (646) and one .3 miles east (647) follow:
| 646 | 647
Quartz | 1 | 12
Plagioclase | 71 | 43
Biotite | - | 1
Augite | 13 | -
Hornblende | 10 | 36
Apatite | tr. | tr.
Zircon | 1 | tr.
Magnetite and Ilmentite | 4 | 8
Foliation is N84W,24SW and parallels foliation in basement rocks to the south. The outcrop was mapped by Buddington and Leonard (1962) as a diorite gneiss, but they did not consider the unit to be as widespread as is shown in Figure 2.

STOP 2. Sabattis Road Member of the Lost Pond Marble
The Sabattis Road Member of the Lost Pond Marble is exposed on the north side of the road. Most of the outcrop consists of brown-to gray-weathering marble beds up to 2 m thick. A few layers of quartzite, .5 m thick, are also present. The graphitic marble includes quartz, microcline, pale green diopside, phlogopite, calcite, sphene, and scapolite. The quartz and diopside stand out as small knobs and clusters on the weathered surface.
F2 fold axes plunge S45W at about 10 degrees, and minor undulations in bedding define a pronounced lineation in places.

STOP 3. Bear Pond Gneiss
The Bear Pond Gneiss is exposed along the northwest shore of Bear Pond. Layering and foliation strike northeast, parallel to the trend of the pond, and dip southeast beneath the Lost Pond Marble of STOP 2. Grain size in the magnetitebiotite-quartz-microcline gneiss varies from fine to pegmatitic.
A biotite-rich unit of the Bear Pond Gneiss lies on the north side of the road .1 mile west of Bear Pond. The gneiss is cut by a coarse microcline pegmatite body that is roughly concordant to foliation.
Near the crest of the hill .2 miles west of Bear Pond a third example of the Bear Pond Gneiss is exposed. The rock is a gneiss. Locally, both sillimanite and coarse garnet constitute more than 10% of the rock. A strong F2 sillimanite lineation plunges S46W at 4 degrees. Garnet distribution in this "chicken pox" rock is locally random, but in some places the garnet is concentrated in layers parallel to foliation.

Swamp to north is underlain by Lost Pond Marble.

Bear Pond Gneiss exposed on left side of road.

STOP 4. Bear Pond Gneiss
This area is not generally accessible to the public. Beginning at the southwest corner of the log landing, walk 400 yards at S40W across uneven terrain to the outlet of a small pond. Here the Bear Pond Gneiss is exposed in the axial region of a map-scale F2 syncline. Both limbs strike NE and dip SE. Many minor structures exposed along the outlet illustrate the second phase of deformation. Fold axes and mineral lineations form a tight southwest-plunging concentration on an equal area net. If water levels permit, a faint F3 magnetite lineation will be seen.
The Loon Pond Dioritic Gneiss is exposed on the other side of the outlet .1 mile southwest along the edge of the pond.

Bear Pond Gneiss on south side of road.

Abandoned Sabattis Railroad Station.
Turn around and return to Little Tupper Lake.

STOP 5. Overgrown quarry on west side of road.
The old quarry is in the Bog River Member of the Lost Pond Marble and contains graphite, calcite, sphere, phlogopite, quartz, calcite, and diopside. Diopside varies in color from pale to dark green and locally forms more than 50% of the rock. The rock is moderately well to poorly foliated, and grain size varies from medium to coarse. There is great variation in the relative proportions of calcite and quartz in the rock. Rocks at this location bear a strong resemblance to the diopsidic marbles of the Sabattis Road Member of the Lost Pond Marble (Stop 2).

AB2b: BEDROCK GEOLOGY OF THE GRAMPUS LAKE AREA, LONG LAKE QUADRANGLE, NEW YORK
Page Fallon
Department of Geology and Geography
University of Massachusetts
Amherst, MA
What follows is a brief description of the geology of the Grampus Lake area. These are the preliminary results of a study conducted under the guidance of Professor Leo M. Hall at the University of Massachusetts. The map area lies in the southwest part of the Long Lake quadrangle and includes a portion of the southeast corner of the Tupper Lake quadrangle (see Figure 1). Previous work in the area was done by Cushing (1907) in the Long Lake quadrangle and Buddington and Leonard (1962) in the Tupper Lake quadrangle.

AB2b: BEDROCK GEOLOGY OF THE GRAMPUS LAKE AREA, LONG LAKE QUADRANGLE, NEW YORK

STOP 1. Buck Mountain Fold Complex
This stop offers the opportunity to see the diopside augen quartz gneiss and other quartz rich gneisses and well exposed examples of second and third phase folds.
Road Cuts: Glassy quartzites and diopside augen quartz gneiss with small sparse diopside augen are exposed on the western side of Route 30. The small outcrop on the eastern side of the highway contains a few large dark green diopside porphyroblasts.
1-A.) Buck Mountain Syncline. Walk east from the highway 600 feet down the logging road. Bear left at a small cabin onto an overgrown skidder trail. Walk 1000 feet approximately N45E along a contour. The outcrop on the steep slope to the southeast exposes the hinge of the Buck Mountain Syncline, a large third phase fold, (see figs. 8 and 9). This is a tight fold which plunges moderately to the southeast on a northwest trending, steeply south dipping axial surface.
I-B.) Proceed west from the highway on an overgrown trail from the south end of the western road cut for about 1000 feet. Turn north and climb the hill to a large pavement outcrop.
The rock is typical diopside augen quartz gneiss. The augen which have weathered out, giving the rock this distinctive texture, are large single crystals or aggregates of smaller grains of green to white diopside. Scapolite is common. Minor K-feldspar, and traces of calcite, sphene, and zoisite are present.
A second phase isoclinal fold, outlined by a thin amphibolite, is refolded by a tight third phase fold, forming a hook interference pattern. Note the lack of an axial plane foliation in the hinge of the second phase fold. A more prominent axial plane feature is present in the hinges of third phase folds. Other folds, and a nice view to the south, are visible higher on the hill.

STOP 2. Rock Pond Syncline
The low outcrop to the left is a buff weathering diopside granulite which contains, in addition to diopside, calcite, plagioclase, and minor microperthite and quartz. Sulfides are present and graphite is abundant.
The structure of this area is poorly understood. The Rock Pond syncline closes around the calcsilicate gneisses just to the northwest. Refolding in the third phase produced north-side up folds (see fig. 4, Section E-F). The inappropriate rotation sense of the third phase fold is attributed to original curvature of the hinge line of the Rock Pond Syncline. Late folding about northwest trending axial surfaces causes local changes in the direction of plunge of the third phase fold.

AB2c: A TRAVERSE ACROSS THE SOUTHERN CONTACT OF THE MARCY ANORTHOSITE MASSIF, SANTANONI QUADRANGLE, NEW YORK
Paul Ollila
Vassar College
Poughkeepsie, NY 12601
The 15' Santanoni quadrangle is located between 44°00' and 44°15' north latitude and 74°00' and 74°15' west longitude in what is known as the High Peaks region of the Adirondack Mountains of New York State (Figure 1). The nearest towns of any size are Lake Placid, which is northeast of the quadrangle, and Saranac Lake, which is north of the quadrangle (Figure 2).
Approximately 80% of the quadrangle is underlain by anorthosite or anorthosite-related rocks. The remainder of the area is underlain by pyroxene syenite gneisses (commonly ascribed to a mangerite-charnockite series), amphibolites, granitic, pelitic and calc-silicate gneisses, marbles and quartzites. All of these rocks have been affected by the approximately one billion year old Grenville metamorphism and form the southeastern part of the Grenville province of the Canadian shield. Bedrock geologic mapping of the Santanoni quadrangle at a scale of 1:62 500 was carried out between 1978 and 1982 under the direction of Howard Jaffe from the University of Massachusetts.
AB-2

AB2c: A TRAVERSE ACROSS THE SOUTHERN CONTACT OF THE MARCY ANORTHOSITE MASSIF, SANTANONI QUADRANGLE, NEW YORK

STOP 1 Gooseberry Mountain Gneiss
The Gooseberry Mountain Gneiss consists of pink-weathering, medium-grained granitic gneiss, black-and white-weathering amphibolites that average 1 m in thickness and gray-weathering layers 1 to 3 mm thick rich in sillimanite, biotite and quartz. Sillimanite gneisses are the key to identifying the Gooseberry Mountain gneiss. Other rocks included within this unit are quite similar to rocks included in the Moose Mountain Gneiss.
Sillimanite gneisses form only a small part of the unit but have been found on the north side of Gooseberry Mountain, on the southern end of a hill just east of Deer Pond, and on the southwestern side of Gooseberry Mountain in the Long Lake quadrangle.
North of Gooseberry Mountain, zones characterized by abundant sillimanite rich layers occur within pink granite gneiss. Within these zones, sillimanite-rich layers are separated by 1 to 2 cm layers of quartz and pink microperthite augen. Granitic gneiss within the Gooseberry Mountain gneiss is typically composed of anhedral quartz, and microperthite, brown biotite, magnetite, and may contain green hornblende and orthopyroxene. Sample 17-1 (Table 1) is fairly representative except that the granitic gneisses commonly contain higher modal proportions of magnetite. Average grain size is 1 to 2 mm and foliation is defined by oriented biotite. Sillimanite rich layers and amphibolite layers parallel foliation. Both weathered and broken surfaces of granitic gneiss are pink to brown. Locally the granite gneiss is garnetiferous and garnetiferous granitic pegmatites are fairly abundant on the southwest side of Gooseberry Mountain.
Amphibolite layers are abundant at low elevations on the northern side of Gooseberry Mountain and also north of Deer Pond in the Long Lake quadrangle. The amphibolites are medium-grained but range in texture from well-foliated to granular. They are black-and white-weathering and typically have a color index near 50. Hornblende and plagioclase are the dominant minerals but amphibolites also contain brown biotite, orthopyroxene and oxides. Both garnetiferous and non-garnetiferous varieties have been observed. At location 17-22, granitic gneiss and amphibolite layers average 1 m in thickness and granitic gneiss forms about 60% of the outcrop. Going south from this location, the amount of amphibolite decreases, until near the summit of Gooseberry Mountain, the rock is almost entirely granitic gneiss. This sequence is reversed down the south side of Gooseberry Mountain. This repetition, and the occurrence of sillimanite gneisses on the north and south side of Gooseberry Mountain, suggest that this unit has been doubled by folding.

STOP 2 Moose Pond Formation-Ymp
The Moose Pond formation is extremely poorly exposed. One probably loose block of coarse-grained calcite marble (sample 17-6, Table 2) is located at the south end of Moose Pond. A mixture of rusty-brown medium-to-fine-grained diopside-quartz-microperthite granulites (17-7, Table 2) and fine-grained biotite-quartz-microperthite gneisses crops out along the western shore of Moose Pond at location 17-7. Although there is abundant quartzite and diopsidic quartzite float northwest of Shaw Pond a nearby outcrop northwest of Shaw Pond contains only a few thin diopside-rich layers. Most of the rock at this location is a medium-to fine-grained brown augite-biotite-quartz-plagioclase-microperthite gneiss.
No outcrops were observed in the region between Gooseberry Mountain and Wolf Pond Mountain. The Moose Pond marble is inferred to go through this region on the basis of topography and the geometry of folds in the Moose Mountain gneiss and the Gooseberry Mountain Gneiss. The aeromagnetic map (1978) shows a magnetic low east of Gooseberry Mountain which is consistent with the presence of marble in this valley. Mineral assemblages in rocks from the Moose Pond marble are listed in Table 2.

STOP 3 Calcareous Quartzites of the Moose Pond Formation.
These rocks contain quartz, diopside, calcite, sphene, microcline and scapolite. The scapolite is partially altered to prehnite.
The dominant foliation in these rocks trends 276°, 26 S and a strong lineation defined by trains of diopside trends 213°, 20°.
The rotation sense of minor folds at this outcrop indicates south side down movement.

STOP 4. Mylonitic pyroxene quartz syenite gneiss.
This rock is more intensely foliated and finer grained than normal for pyroxene quartz syenite gneiss. Foliation trends 90°, 35 S and locally a strong lineation defined by quartz ribbons trends 222°, 25°. A few asymmetric augen and what are possibly S and C foliations (Berthe et al. 1979, Simpson and Schmid, 1984) suggest south side down movement.
The mineralogy of pyroxene quartz syenite gneiss along Ermine Brook is typical of pyroxene quartz syenite gneiss found elsewhere in the quadrangle. Modes of typical pyroxene quartz syenite gneisses are listed in Table 3.

STOP 5 Gabbroic Anorthosite Gneiss (Ygag)
The gabbroic anorthosite, gneiss map unit trends NW-SE in a zone across the southwestern corner of the quadrangle (Figure 3). It lies between metamorphosed sedimentary and igneous rocks to the southwest and anorthosite to the northeast. The dominant rock type within the unit has a color index (C.I.) equivalent to gabbroic anorthosite but minor amounts of gneissic anorthosite, noritic anorthosite, gabbro, and syenite are included as well. Forty-four samples from the gabbroic anorthosite gneiss map unit were examined in index of refraction oils or in thin-section. Of these 27 have a C. I. equivalent to gabbroic anorthosite, 7 are monzonites, 5 are anorthosites, 2 are gabbros, 1 is noritic anorthosite and 1 is a quartz syenite. The syenitic rocks and the gabbros generally occur as concordant layers or sills. Most of the rock in the unit has a composition similar to gabbroic anorthosite except that it contains more garnet, hornblende, alkali feldspar and quartz. Modes of four samples of gabbroic anorthosite gneiss (Table 4) are representative of the amount of hornblende, garnet, K-feldspar, and quartz typically found in these rocks. Orthopyroxene, although present in all four modes, is not commonly present in anorthosite gneiss. At this locality pyroxene is commonly rimmed by hornblende which locally defines a strong lineation that trends 225°, 24°.
Rock at this locality is heterogeneous, consisting of gabbroic anorthosite gneiss with lesser amounts of gabbro, anorthosite, and syenitic gneiss. This is a good area to look at both intrusive relationships between the different rock types and the intense deformation typical of gabbroic anorthosite gneiss. Note also the different response of the various rock types to deformation.

STOP 6 Anorthosite.
This anorthosite is typical of anorthosite in much of the interior of massif. This rock is probably part of a layer or large xenolith of anorthosite in the gabbroic anorthosite gneiss map unit. More gabbroic anorthosite gneiss crops out to the north along the other branch of Ermine Brook and on Little Santanoni Mountain.

BC3: FORELAND BASIN SEDIMENTATION IN THE TRENTON GROUP OF CENTRAL NEW YORK
C. J. Mehrtens
Burlington, Vt. 05405
Purpose
The purpose of this field trip is to re-examine several of the well-known exposures of the Trenton Group in the Mohawk Valley. This re-examination is necessary due to the recent reinterpretations of the depo-tectonic setting and sedimentology of these units. Specifically, the Trenton Group in central New York has been redefined as a foreland basin and a tectonically active shelf edge/trench slope environment (Cisne, et al., 1982). The sedimentology of the Trenton Group has been shown (Mehrtens, in review) to evolve from in situ carbonates to dominantly turbiditic in nature. This field trip will visit several localities where participants will be able to view: (1) variations in the thickness of units over short lateral distances; (2) rapid facies changes within individiual stratigraphic sequences; (3) syn-depositional slump fold horizons; (4) internal structures within limestone beds, identifiable as Bouma sequences. These features are all characteristic of sedimentation in the tectonically active foreland basin. The text for this field trip will review the stratigraphic model presented by Cisne and Rabe (1978) and Cisne, et al (1982). Evidence for the interpretation of the limestone and shale couplets of the Denley Limestone and Dolgeville Facies as bioclastic turbidites will also be reviewed. Previous interpretations of the Trenton Group depo-tectonic setting will be presented and compared to the foreland basin model. It is hoped that this field trip will demonstrate, if nothing else, the strong role that a model or paradigm can play in the interpertation of stratigraphic sequences.

BC3: FORELAND BASIN SEDIMENTATION IN THE TRENTON GROUP OF CENTRAL NEW YORK

Pass lower portion of City Brook on right.

STOP 1. Buttermilk Creek
Park immediately beyond the bridge and descend to Buttermilk Creek. The section downstream of the bridge is part of the Black River Group (Gull River), consisting of calcareous limestone. Underneath the bridge and a short distance upstream are ledges of coarsely crystalline limestone alternating with massive calcareous sandstone beds. These are the lagoonal sediments of the Napanee and Selby Limestones. These rocks have been described by Titus and Cameron (1976) and are characterized by their aphanitic texture, birdseye structures, massive bedding, and disseminated quartz sand. This facies continues in a series of benches going upstream. The contact of the Napanee and Selby with the Kings Falls occurs immediately above the pool below the first waterfall. The Kings Falls is differentiated from the underlying facies by the first appearance of fossiliferous calcarenites that are thinner bedded and exhibit lateral thickening and thinning of individual beds. The Kings Falls continues upstream to the larger waterfall, consisting of beds of calcarenite and bioturbated calcilutite. The lateral lensing of the beds, so characteristic of the Kings Falls is readily visible.
While at this stop you should: (1) examine the Napanee and Selby (lagoonal) facies as this is the only stop where they will be seen on this trip; (2) examine the Kings Falls, noting in particular the features which may suggest that it accumulated near wave base. Are there any internal structures within the limestone beds? How much shale, if any, is present? Are the beds laterally continuous? How frequent was bioturbation? Where are the fossils within limestone beds or on bedding planes?

STOP 2 City Brook
After disembarking from the cars, descend to City Brook upstream of the bridge. The section downstream is one of the most beautiful exposures of the Black River, Selby, Napanee and Kings Falls Limestones in the Mohawk Valley but is off limits. Under the bridge, and continuing up section, are small benches of the Sugar River Limestone. These bedding planes are distinguished by their abundant Prasopora colonies, along with the typical Sugar River benthic fauna described in Titus and Cameron (1976). Compare the Sugar River Limestone to the Kings Falls Limestone seen at STOP 1. How does it differ? What is the evidence that it might have accumulated at slightly deeper depths? How laterally continuous are these beds? Do they exhibit the same degree of lateral lensing? Is there a change in the relative percentage of calcarenite versus calcilutite beds? The contact of the Sugar River and the Denley Limestones occurs in the small waterfall. The basal Denley seen here is similar to the basal Denley seen at the next stop (Shedd Brook) but is very different than the basal Denley at Trenton Falls Gorge.
Here the Denley is much less fossiliferous and much finer-grained. Note the nodular limestone bedding. Bedding planes are not littered with fauna, except for an occasional trilobite and cephalopod. Continuing up the stepped benches note the abundance of calcilutite, mostly all barren. The dominant two lithologies of the Denley here are: (1) a barren calcilutite with planar bottoms and reworked (bioturbated) tops and (2) a nodular, more argillaceous calcilutite. These lithologies continue upstream until the waterfall is reached. Here, on the cliffs above the stream, the contact with the overlying Dolgeville Facies is seen. The Dolgeville is characterized by the interbedded planar calcilutite with thick interbeds of shale (see Figure 15). This City Brook section is interesting because it records a very rapid, nongradational facies change in the Sugar River/Denley contact. It also is unusual in that the Denley here is such a deep water deposit. Examination of the limestone beds reveals a dominance of planar laminations interpreted as Td and structureless, bioturbated micrite interpreted as Td'. While at this stop you should ponder the nature of the facies change from the Sugar River to Denley. Do you think it's the result of lateral facies mosaicing accompanying gradual transgression, or, could it be the result of a rapid drop of the fault block, drowning the shelf?

STOP 3. Shedd Brook
After parking at the top of the hill, cross the road and descend to the stream bed. Walk down to the base of the section. Exposed at the base of Shedd Brook is the upper Kings Falls Limestone. It should look similar to the upper part of the section at Buttermilk Creek, that is, coarse calcarenite to calcirudite beds which exhibit lensing. All of the Sugar River Limestone is exposed in this stream cut, and comparisons can be made between the Kings Falls and Sugar River. Study the Sugar River lithologies and bedding styles to draw some conclusion about environment of deposition relative to wave base. This is an important point because the Sugar River is interpreted to represent "normal" carbonate accumulation below wave base. If this is what "normal" below-wave base sedimentation looks like, what interpretations can be made about the overlying Denley Limestone? The contact of the Sugar River and the Denley Limestone occurs at the top of the waterfall. Examine the upper horizons of the Sugar River. Note the abundance of relatively unfossiliferous calcilutite beds with shale interbeds. How gradational are the Kings Falls to lower Sugar River to uppermost Sugar River facies? The top of the waterfall represents the last of the fossiliferous calcilutite and calcarenite beds in this section. The percentage of interbedded shale is also increasing. A bentonite horizon is present in the bushes on the left side of the stream. There is a long bench in the stream bed of the nodular barren calcilutite beds with thick shale interbeds of the Denley Limestone. This should look similar to the Denley seen at the previous stop. Up stream at the bend in the brook, Dolgeville beds of planar calcilutite and shale are seen. Passing under the road you continue to walk on nodular bedded, calcilutite horizons of the Denley Limestone. About 50 feet above the road on the right side of the stream, there is a small exposure of interbedded nodular calcilutite and planar calcilutite beds with bioturbated tops, also of the Denley Limestone. Two more bentonite horizons are located in this small cliff. The stratigraphic section seen along Shedd Brook is very similar to that in City Brook but it is worth walking this section to demonstrate: (1) the gradational Kings Falls to Sugar River section; (2) interbedded bentonite horizons.

West Canada Creek on right, access to Trenton Falls Gorge is ahead.

STOP 4. Prospect
(needs special permission from Niagara Mohawk Power Corp.)
After parking the cars across the bridge, descend the cliff to West Canada Creek carefully. Standing on the bedding plane above the creek, turn around and examine the cliff face. A prominent slump fold horizon is visible (Figure 16). Note that the slump fold can be traced laterally to an undisrupted horizon of calcarenite. The nose of the fold is characterized by brecciated clasts of limestone so the sediment was fairly lithified at the time of emplacement. Paleoslope measurements on this and other slope indicators (aligned fossils) indicate a paleoslope of S80E (Cisne and Rabe, 1978). Note the sediment in which the slumping occured. This is the Denley Limestone, but a very different Denley than what has been seen at Stops 2 and 3. Note how fossiliferous some of the calcarenite and calcirudite beds are. The strophomenid Rafinesquina is especially abundant, as is Prasopora. Interbedded with this fossiliferous facies of the Denley are lithologies we have already seen: nodular, bioturbated calcilutite and calcilutite with planar bases and bioturbated tops (Td'). Also present are beds of graded skeletal debris (Ta), and horizontally laminated skeletal debris (Tb). Looking upstream a wide waterfall can be seen and individual beds can be traced across this exposure. Beds which exhibit this degree of lateral continuity, with negligible change in thickness could not have accumulated near wave base.

STOP 5. Dolgeville
This stop along East Canada Creek in Dolgeville is made for examination of the basinal shales. Parking on the hill and descending to the stream below the dam, the calcareous turbidites and interbedded shale horizons of the Utica shale are exposed. The calcareous turbidites are identifiable by their buff yellow weathering. Tc and Td horizons are the only Bouma Units present. The thick shale interbeds contain numerous good graptolites. Based on the Bouma Units present within the turbidite horizons and the thickness of the inter-turbidite deposits, it is possible to interpret this section as representing a distal turbidite facies. The source of the calcareous horizons is the foundered shelf (Dolgeville Facies) inter-tonguing with the basinal terrigenous muds. Continuing down to the pool at the base of the waterfall, drag folds associated with the Little Falls Fault are visible.

STOP 6. Canajoharie Creek
Descend to the creek from the parking lot. The creek bed is Chuctanunda Creek Dolostone of Lower Ordovician age. The lower cliff face contains the unconformity between this dolostone and the interbedded limestone and shales of the Kings Falls Limestone. Looking up the cliff the Kings Falls is overlain by the Canajoharie Shale (Figure 15). In other words, all of the Lower Trenton is missing, with the exception of a thin section (15 feet) of Kings Falls, and all of the upper Trenton is missing. Cameron (1971) described this section of limestone as Sugar River, but noted that it represents a shallower water environment than the Sugar River seen to the northwest (Stops 2 and 3). This unit can be better described not by the fossil assemblage it contains, but by the lithofacies present. The bedding style is identical to that of the Kings Falls seen earlier: laterally discontinuous beds exhibiting lensing and cross laminations. Looking at this section you can ask yourself: How can wave-reworked limestones and basinal shales be juxtaposed with no intervening deeper water limestones? Why are there no lower Trenton units between the Kings Falls and the Lower Ordovician dolomites? Do these abrupt facies changes represent lateral mosaicing produced by sea level changes or does it seem more probable that movement on a syndepositional block fault could generate this type of sequence?

STOP 7. Caroga Creek
After parking, descend to the creek below the bridge under Route 5. The section below the bridge and downstream are undifferentiated Black River deposits. Depending on the height of the stream, variable amounts of rock are exposed here. At low stage, aphanitic dolostones with birdseye structures are visible. The section between the two bridges has many covered intervals but ledges of coarsely crystalline limestone outcrop and are interpreted as Kings Falls. Under the second bridge ledges of laminated calcarenites outcrop, exhibiting planar tops and bottoms and lacking fossils. Upstream of these are beds of the bioturbated, barren calcilutites,. These last two lithologies are characteristic of the Denley Limestone as seen on City and Shedd Brooks.
A covered interval occurs above this and below the cliff with Utica Shale. This section then, is another thinned section of Trenton. Both the lower Trenton and upper Trenton units are missing or greatly reduced in thickness. Because the quality of this exposure is not equal to that at Canajoharie Creek, it is not as spectacular, but the significance of the facies changes is equally important. Note that as one progressed east for the last two outcrops, the magnitude of the variation in stratigraphic sections became more significant. This is in keeping with our moving further into the foreland basin from the stable shelf represented in the earlier outcrops.

BC4: ANIMAL-SEDIMENT RELATIONSHIPS IN MIDDLE ORDOVICIAN HABITATS
David W. Larson
Hamilton College
Clinton, New York 13323
In recent years a number of workers have presented arguments to suggest that utilization of infaunal life strategies by marine organisms has varied through the Paleozoic. Evidence for a progressive "infaunalization" of Paleozoic communities comes from functional analysis of trace fossils (Seilacher, 1977), patterns of taxonomic richness of skeletonized bioturbating organisms (Thayer 1979, 1983), and the sedimentary record of the effects of burrowing organisms (Garrett, 1970; Sepkoski, 1982; Larson and Rhoads, 1983). Between the Middle Ordovician and Early Devonian, it seems that the depth of biogenic reworking of sediment in marine shelf settings increased from essentially zero to over 5 cm. Exploitation of buried food resources by deposit-feeders propels this infaunal invasion (Larson and Rhoads, 1983). Miller and Byers (1984) present an opposing view, that infauna are abundant and diverse throughout the early Paleozoic. At present, there is no consensus as to the style and degree of biogenic reworking in the early Paleozoic.
This field trip is meant to provide an opportunity to examine some of the evidence that has convinced me that biogenic reworking in Ordovician sedimentary environments was much reduced in comparison to recent counterparts. We will visit a series of four outcrops of Middle Ordovician carbonate rocks in the Black River Valley of northwestern New York (Figure 1). Our trip will take us on a transect of facies from the intertidal carbonates of the Black River Group through a range of shallow to deep shelf and basinal environments in the Trenton Group. The goal is to examine Ordovician animal-sediment relationships and their sedimentologic and paleoecologic implications.

BC4: ANIMAL-SEDIMENT RELATIONSHIPS IN MIDDLE ORDOVICIAN HABITATS

Bridge across Sugar River.
Upstream is an excellent exposure of the limestones in the lower portion of the Trenton Group. The quarry on the right side of the highway is in the Black River Group. Downstream, solution cavities and channels in the Black River Group cause subsurface drainage of Sugar River. At low discharge all of Sugar River disappears into the stream bed.

STOP 1. Road cuts in the Black River Group
Road cuts in the Black River Group on north and south side of Turin Road.
The Black River Group is a well documented example of tidally influenced carbonate deposition. This discussion of the stratigraphy and sedimentology of the Black River Group is largely drawn from Walker (1973) and Walker and Laporte (1970).
Here the Black River Group is divided into three formations:
Chaumont Formation: burrowed, fossiliferous wackestone.
Lowville Formation: fenestral, laminated mudstone, wackestone, and packstone.
Pamelia Formation: dolostone and dolomitic sandstone.
The sequence Pamelia/Lowville/Chaumont is interpreted by Walker (1973) to record the progressive transgression of the Middle Ordovician sea onto an eroded Grenville terrane. From base to top the Black River Group records the transition from supratidal to intertidal to shallow subtidal conditions.
The Lowville Formation includes a number of sedimentologic features indicative of an intertidal origin: mudcracks, fenestral fabric, and algal laminations. In addition, oolites, intraformational conglomerates, and fragmented mounds of Tetradium indicate vigorous stirring of the bottom.
The Chaumont Formation contains fewer sedimentologic criteria on which to base an environmental interpretation. Walker (1973) bases his assignment of the Chaumont to the shallow subtidal on the presence of brachiopods and bryozoa in the Chaumont and the interbedding of Lowville and Chaumont lithologies.
A striking feature of the outcrop is the contrast in sedimentary fabrics between the Lowville and Chaumont Formations. Burrows are rare in the Lowville. The sedimentary structures that permit such a straight-forward facies assignment are barely altered by biogenic reworking. Chaumont sedimentary fabrics on the other hand are dominated by burrows. In many cases the outlines of individual burrows are distinct; in others, the burrow outlines are diffuse. Importantly, other than laterally discontinuous bedding units, the biogenic structures have very nearly obliterated the depositional features. This style of bioturbation is characteristic of deposit-feeding communities (Rhoads and Young, 1970; also Rhoads and Boyer, 1982).
Here then we are able to see that for these Ordovician habitats, like their recent counterparts, the effects of bioturbation increase in an offshore direction. A deposit-feeding community was clearly active in this shallow subtidal setting.

STOP 2. Steuben Limestone of the Trenton Group.
Abandoned railroad cut through the Steuben Limestone of the Trenton Group. From this vantage point you can see the Tug Hill Plateau, underlain by the Utica Shale and Lorraine Group, to the west. To the east across the Black River Valley are Grenville rocks of the Adirondacks.
At this exposure we will examine a ten meter section of the Steuben Limestone (Figure 6). About 40 cm of Hillier Limestone is exposed at the top of this cut. We will see a much thicker section of the Hillier at Stop 4.
The Steuben Limestone is generally a thickly bedded fossiliferous packstone with some important variations in lithology. Near the base of the exposure, fossiliferous mudstones and wackestones are interbedded with centimeter thick argillaceous mudstones. Both grainsize and bed thickness increases upward through the Steuben. Midway through the section are cross-laminated grainstones and packstones, some with mega-rippled upper bedding surfaces. There are shaly partings near the top of the Steuben, but no interbedded lime or argillaceous mudstones. The upper portions of the Steuben accumulated in more turbulent, more frequently agitated waters than the sediments at the base of the exposure. On the onshore-offshore gradient, I assign the Steuben to an open marine shelf subject to occasional stirring by currents or waves (Figure 3). Certainly the Steuben was deposited in a more exposed environment than the Chaumont of Stop 1.
Trace fossils are prominent throughout the Steuben. Near the base of the exposure are examples of Palaeophycus, Planolites, and Chondrites. These burrows are confined to bedding surfaces or generally penetrate the sediment only several cm. Monocraterion, a vertical sediment filled tube one cm in diameter and up to 8 cm long, is common in the crinoidal packstones near the top of the Steuben.
The style of bioturbation also varies vertically in the Steuben. Although nowhere is the Steuben completely burrow reworked, it seems that the greatest degree of biogenic alteration of the sedimentary fabric occurs in the upper Steuben with Monocraterion. This trend runs counter what we would expect from the modern: rather than finding the greatest degree of biogenic reworking in fine-grained sediments at depth, here the coarser-grained, shallow-water environments are more reworked. Consequently, at this point Figure 3 shows the divergence in bioturbation trends for the Recent and Ordovician.

STOP 3. Whittaker Falls Park.
Nearly all of the Trenton and Black River Groups are exposed along Roaring Brook. In a combination of rapids, falls, and level stretches, the rocks are exposed in both vertical section and on bedding planes. A long, nearly continuous exposure of the Denley Limestone is the focus of our attention.
On the basis of smaller grain size and fewer indications of turbulent conditions, I have assigned the Denley to a position further offshore than the overlying Steuben Limestone. The upper 50 m of the Denley contains mega-rippled and cross-stratified grainstones interbedded with finer-grained lithologies. This portion of the Denley was deposited within the reach of storm wave base. Because the basal 9 m of the Denley lack these grainstones, this portion of the formation appears to have accumulated below storm wave base.
The Denley Limestone contains a diverse fauna including brachiopods, bryozoa, crinoids, and trilobites. Many of the body fossils apparent on outcrop here are fragmented, abraded, and occur in grainstone or packstone units. Overturned heads of the bryozoan Prasopora attest to disturbance and relocation of many of the fossils. Figure 7 is an illustration of the role of turbulent events, major storms, in producing both the sedimentary structures and the fossil assemblages in the Denley.
Not all of the fossils are reworked, however. Adhering to the tops of limestone beds, or entombed within centimeter thick shaly partings are some fossil assemblages that indicate in place accumulation. Evidence for in place accumulation includes lack of abrasion and fragmentation and the co-occurrence of fossils ranging in size from .1 to 1.5 cm. In addition, several specimens of juvenile crinoids, complete with holdfast, suggest in place burial rather than transportation before burial.
Trace fossils are abundant here. Palaeophycus and Chondrites are the most conspicuous. Again, despite the presence of burrows, the sedimentary fabrics of the Denley retain their original features. Maximum depth of burrowing is about 3 cm.

Crummy roadcut on left is Steuben Limestone.

Excellent exposures of Trenton Group.

We are climbing to the top of the Tug Hill Plateau.

STOP 4. Bridge over Gulf Stream
Park off of road on left-hand side.
Cut along Gulf Stream where we can examine the contact between the Utica Shale and the underlying Hillier Limestone of the Trenton Group.
Watch out! Poison ivy is abundant and lush here, especially on the Utica Shale.
This is a 13 m section that records the transition from wave influenced shelf to deep, anaerobic basin (Figure 8). Illustrating this trend through the Hillier Limestone is a decrease in grainsize, loss of mega-rippled and cross-laminated beds, and an increase in number and thickness of shaly partings in the limestone.
Here the transition to deeper water is marked by an increase in burrowing. Palaeophycus, Planolites, and Chondrites are present, but evidence of a bioturbating, deposit-feeding community is absent. Here, too, the conspicuous body fossils are brachiopods, bryozoa, and crinoids although the gastropod Liospira is locally abundant.
The uppermost Hillier is an interesting lithology with lumpy nodular bedding. The fauna here includes mostly phosphatic forms: trilobites, conularids, and lingulids with setae preserved around the margin of the valves.
The Utica Shale is a black, fissile, argillaceous mudstone. Careful collecting can turn up cephalopods, graptolites, and the trilobite Triarthrus.

BC5: SEDIMENTARY STRUCTURES AND PALEOENVIRONMENTAL ANALYSIS OF THE BERTIE FORMATION (UPPER SILURIAN, CAYUGAN SERIES) OF CENTRAL NY
Victor P. Tollerton, Jr. and Herman S. Muskatt
Utica College of Syracuse University
Utica, N.Y.
The Bertie Formation (Upper Silurian, Cayugan Series) of New York State, is world renowned for its spectacular eurypterid fossils. However, details of the total fauna (not just the eurypterids) and its significance, along with an understanding of the depositional environment, lags behind most other rock units in New York State. An understanding of the depositional environment of the Bertie is further complicated by a lack of published studies on the sedimentary structures that occur in the formation. Almost without exception, the fossils and the sedimentary structures have been treated as separate and totally unrelated aspects. Only minor attention had been paid to the structures (e.g., mud-cracks, and the windrow accumulations).
The writers are fully aware that the fossils are an important aspect in the overall interpretation of the depositional environment of the Bertie, especially when they are considered as primary sedimentary structures. Matters of identification and errors of stratigraphic relations of the fossils in the Bertie strata severely limit their usefulness and delay understanding of their significance (see further comments under Paleontology).
With regard to the sedimentary structures, we know of no published studies that list, describe, and discuss all of them. Buchwald (1963) did study some of them. The main purpose of this paper, then, is analyses of all of the known sedimentary structures of the Bertie, with emphasis on their use in the interpretation of the depositional environment.
Although only three stops will be made in the field, all are key outcrops. Stop 1 is at Forge Hollow, New York, where a complete sequence of the Bertie with both lower and upper contacts with the Camillus and Cobleskill Formations, respectively, are exposed. Stop 2 is at Jerusalem Hill, where the upper Fiddlers Green and the lower Scajaquada Members are exposed. Stop 3 is at Passage Gulf, where the lower contact with the Camillus is exposed.

BC5: SEDIMENTARY STRUCTURES AND PALEOENVIRONMENTAL ANALYSIS OF THE BERTIE FORMATION (UPPER SILURIAN, CAYUGAN SERIES) OF CENTRAL NY

Bridge over Oriskany Creek

STOP 1. Forge Hollow, New York
Outcrop on right. Big Creek on left. Parking on right.
On Route 315 (fig. 14) Oriskany Falls, N.Y., 7 1/2 minute topographic quadrangle
Rickard (1953) locality No. 43.
This locality is believed by Leutze (1959, p. 101- 102) to be the Waterville outcrop cited by Vanuxem (1982) and Hall (1859). Rickard (1953, 1962) designated this site as the type locality for his Forge Hollow Member (= Scajaquada Member of present terminology).
This is the only complete sequence of the Bertie Formation in east-central New York. Both the lower and upper contacts with the Camillus and Cobleskill Formations, respectively are exposed. The lower contact is at the southern end of the exposure.
Fossils collecting is highly discouraged during this field trip because of the dangerous conditions at this outcrop (e.g., blind curve, narrow road, steep outcrop). KEEP OFF THE ROAD.
Nearly all faunal and sedimentary structural elements discussed in this paper have been found by the writers or reported by others as occurring here. The purpose of this stop, then, is examination of the fossils and sedimentary structures, as well as their stratigraphic sequence.

Outwash Plain

STOP 2. Jerusalem Hill Rd. outcrop
Parking in lot of Town of Litchfield Town Hall, across from outcrop.
Jerusalem Hill, Litchfield, New York (fig. 15a) West Winfield, N.Y. 7 1/2 minute topographic quadrangle Lautze (1959) locality No. 207
This locality is the Litchfield outcrop cited by Vanuxem (1842) Hall (1859), Clarke and Ruedemann (1912), and Ruedemann (1925). The wheelock Hill locality is located about 1 1/2 miles to the NW.
Although many eurypterids have been collected here in the past, NO collecting is authorized by the town board.
The purpose of this stop is to examine the geographic and stratigraphic continuity of the fossils and sedimentary structures with those seen at stop 1, located about 16 1/2 miles straight-line distance to the west of this stop.

Quarry on right. Camillus Formation
Quarry on right. Camillus Formation, 80 feet exposed. STOP: Depends on time. (Ref. Treesh, 1972. Stop III). Beckus Gulf. CAUTION, narrow road. Syracuse Formation, nearly complete section, (Treesh, 1972, Stop II).

Vernon Shale on right, (Treesh, 1972, Stop I)

STOP 3 Passage Gulf (Spohn Rd.).
Passage Gulf, on Spohn Road (fig. 15b). Millers Mills, N.Y. 7 1/4 minute topographic gradrangle
Rickard (1953) locality No. 39; Leutze (1959) locality No. 211.
This locality exposes an areally small outcrop, that is remarkably productive with regard to fossils. The upper-most beds of the Fiddlers Green Member are often excavated, giving the appearance of a battlefield.
The farmer who owns the land at this locality has recently bulldozed off the top layers of a portion of this site.
The entire Fiddlers Green Member is easily accessible for detailed examination of the sedimentary structures and their stratigraphic sequence.
The purpose of this stop is to examine the continued geographic and stratigraphic continuity of fossils and sedimentary structures with those seen at stop 1, located about 20 miles straight-line distance to the west of this stop. Also, discussion is encouraged at this last stop relative to epeiric sea environments and the Bertie Formation.

BC6: THE STERLING MINE. ANTWERP. NEW YORK A NEW LOOK AT AN OLD LOCALITY
S. C. Chamberlain
Institute for Sensory Research
Syracuse University
Syracuse, NY 13210
The Sterling mine was the first American locality for the nickel sulfide, millerite. In the last hundred years it has produced many fine specimens of that mineral, including some that many regard to the the finest examples of the species ever found. In the past several years George Robinson at the National Museums of Canada and I have reexamined the geology, mineralogy, and origin of this landmark locality (Robinson and Chamberlain, 1984). Our interest was stimulated by our finding that much of the crystallized hematite in the ore had been reduced to magnetite and that some of the millerite had altered to the rather rare nickel silicate, pecoraite. The following pages summarize the history, geology, mineralogy, and paragenesis of this locality.

STOP 1. The Sterling Mine
The Sterllng Mine is in Jefferson County, New York, along US Route 11 between Watertown and Gouverneur (Fig. 1). The water-filled open pit (Fig. 2) and surrounding dumps may be reached by foot via a farm lane which runs east from US Route 11 at a point 3.75 miles north of the intersections of Routes 11 and 26 in the village of Antwerp. The mine appears on contemporary topographic maps of the Antwerp Quadrangle as a small pond surrounded by low hills between Route 11 and Hawkins Creek. The property is owned by Mr. Raymond Villeneuve whose farm is 0.6 miles south of the entry lane on the east side of Route 11. Permission to collect must be secured before visiting the mine.

BC7: PLEISTOCENE GEOLOGY, GROUNDWATER, AND LAND USES OF THE TUG HILL, AND BRIDGEWATER FLATS AQUIFERS, ONEIDA COUNTY, NY: A CASE STUDY
Kenneth Jeffrey Goldstein
Environmental / Water Resourse Planner
Oneida County Planning and Environmental Management Council
Utica, New York
No Road Log

B8: DEGLACIATION AND CORRELATION OF ICE MARGINS, APPALACHIAN PLATEAU, NEW YORK*
P. Jay Fleisher
Dept. of Earth Sciences
SUNY, College at Oneonta
Oneonta, NY 13820
Donald H. Cadwell
Geological Survey
New York State Museum
State Education Department Albany, NY 12230
The field trip area (Fig. 1) is located in the Susquehanna River Drainage Basin and includes parts of the Unadilla River, Wharton, Oaks, and Butternut Creek valleys. Local relief of the bedrock-drift interface reaches 1200 ft, while surface elevations range between 1050 and 2350 ft. The bedrock is predominantly Devonian sandstone, siltstone, shale (Hamilton Group) and limestone (Onondaga and Helderberg Groups). The purpose of this report, and associated field trip, is to establish and illustrate criteria for the recognition and correlation of ice margin positions in the upper Susquehanna River Drainage Basin.
This part of New York State was no doubt subjected to repeated glaciations during the Pleistocene Epoch. Multiple glaciations are suggested in the subsurface by interbedded diamictons (tills) and outwash gravels (Randall, 1972). However, the abundant glacial deposits within the field trip area formed during the advance and retreat of the Late Woodfordian ice sheet.
Six ice-marginal positions were held during Late Woodfordian time. They are, from south to north, the Wells Bridge, Oneonta, New Berlin, Cassville-Cooperstown, Middleburg, and Valley Heads ice margins. The Wells Bridge, Oneonta, and New Berlin ice margins were established during what is inferred to have been a semi-continuous retreat of the glacier. The glacier readvanced to form the Cassville-Cooperstown margin. The Middleburg ice margin developed during subsequent retreat from the Cassville-Cooperstown position. The final event within the field trip area was a glacial readvance that deposited the Valley Heads Moraine.
*Paper number 435 in the journal series of the New York State Science Service

B8: DEGLACIATION AND CORRELATION OF ICE MARGINS, APPALACHIAN PLATEAU, NEW YORK

Highway begins to climb valley wall behind Valley Heads Moraine

Hummocky crest of moraine on both sides of road

STOP 1. Ludlow Sand And Gravel Company
This gravel pit is located at the Valley Heads Moraine. Past exposures have illustrated the complex environments of deposition associated with this ice-marginal position.
Materials: well sorted, stratified sand, silt and clay; coarse cross bedded gravels; delta foreset gravels; laminated lake clay; poorly stratified fine sand; compact clay diamict (till).
Sedimentary structures: cross-bedding; channel lag gravels; cut and fill; large foreset beds; ripple drift laminations; slumped sands, gravels and silts.
Environment of deposition: Large(?) lake with meltwater streams of variable discharge, with deposition of gravels, sands and silts; near glacier terminus (possibly ice-contact) with deposition of sediments over blocks of glacier ice.
Noteworthy characteristics: ice-contact collapse features; thick, poorly stratified sands; well stratified, interbedded sands and gravels; channel cross bedding; delta foreset beds; compact clay layer with boulders concentrated at the base. This is diamict, deposited during an oscillation of the ice margin.

Segment of Valley Heads Moraine (on left and right)

On left (East) are ice contact, cross bedded outwash gravels.

Pitted outwash on right (West).

PICTURE STOP: "Smith Esker" on right.
This esker can be traced for almost a mile.

Cross Cedarville meltwater channel

Small gravel pit on right in outwash gravels

STOP 2. Hussey Quarry
This gravel pit contains a diamict (till) that documents the Cassville-Cooperstown readvance. The main things to see here are the stratigraphic units and the nature of their deformation.
There are three fundamental stratigraphic units exposed in the south wall of the quarry (see STOP 2 diagram). They are 1) a compact, fine-grained, matrix-supported gray diamict, which overlies 2) a tightly compact stratified drift containing fine gravels, interbedded coarse sands, and well sorted, highly distorted fine sands, and 3) a lower gravel unit containing well washed medium to coarse grained pebbles, cobbles and boulders. The compact stratified drift occurs as distorted lenses of cross-bedded sand and silt within the diamict. The lenses are upturned at their edges and contain distorted sand and silt and show thickening of each unit along fold axes. This thickening suggests that the sand and silt were NOT frozen during deformation. The underlying gravel is not well enough exposed to determine if it too is distorted.
The following questions must be addressed.
1. Origin of the compact stratified drift -
a. Were the sand and silt lenses sheared up from the lower outwash and included in the diamict by overriding ice movement?
b. Were the lenses deposited at the same time as the diamict?
c. Were the lenses deposited after the diamict and subsequently distorted by the diamict squeezing up and around them?
2. Causes of compaction and distortion -
a. Were the lens edges folded during emplacement through shearing?
b. Were the lenses deposited within the diamict with subsequent glacier overriding and deformation?
c. Were the lenses distorted during "dewatering" of the diamict?

Rt. 80 traverses hanging delta to Lake Cooperstown

Rt. 26 climbs up the kame and kettle topography
Rt. 26 climbs up the kame and kettle topography of the Cassville-Cooperstown Moraine (excellent view of moraine to the left)

PICTURE STOP

Esker on valley floor to the left, associated with ablation till

Esker complex on left

Entrance to New Lisbon Landfill - along New Berlin ice margin

Hill on left is the upvalley end of an esker

Additional eskers are seen downvalley

Quarry in deltaic outwash
Entrance on left to quarry in deltaic outwash establishing a body of water in Butternut Creek valley at approximately 1150'

STOP 3. Morris Kame Quarry
In this quarry are exposed deposits typical of non-through valley deposition (stagnant ice blocks) and the associated conditions of glacier retreat. This kame and other landforms across the valley to the south depict an ice-contact environment dominated by local ponding and glacio-fluvial deposition.

Climb up the Aldrich Creek valley.
Turn left on Otsego Co. Rt. 49, which climbs up the Aldrich Creek valley. Aldrich Creek is an underfit stream occupying a valley that was enlarged by meltwater discharge along the New Berlin ice margin. Patches of discontinuous ablation till are found scattered along the valley.

House and outbuilding on the right are situated on ablation till

STOP 4. Divide Facies Of Ice-Marginal Deposits
This semi-active small quarry lies along the trend of the New Berlin ice margin. Typically, ice-marginal positions are correlated across divides by recognizing erosional features such as cols, meltwater channels or underfit streams. Here, however, is a rare view of the materials constituting a depositional landform, which resembles an ice-contact kame.
Unit | Thickness | Description
A | 36" - 48" | poorly sorted fine gravel, distorted in places
B | 24" - 30" | well stratified coarse sand, distorted by slump, collapse or injection from below
C | 6" - 12" | fine gravel with sand and silt matrix
D | 30" - 40" | compact diamict with clay matrix and striated cobbles
E | 36" - ? | washed gravels interbedded with a few layers of well sorted sand (few inches thick) which seems compact

Rt. 17 follows along the New Berlin ice margin
Rt. 17 follows along the New Berlin ice margin as it descends from the divide through the small hamlet of Cardtown and toward Pittsfield.

Kame moraine complex on the right
Kame moraine complex on the right is separated from valley wall by an outwash channel

Climb up back side of a kame moraine-outwash complex
Highway climbs up the back side of a kame moraine-outwash complex that swings across the valley marking a brief hesitation along the retreating New Berlin ice margin. Several similar complexes are found northward along Wharton Creek toward Edmeston.

Descend the pitted outwash surface
Rt. 80 descends the pitted outwash surface and follows the southern margin of a prominent dead-ice sink.

View of dead-ice sink on the right.

Another dead-ice sink can be seen on the valley floor at 2 o'clock

New Berlin valley train on left

STOP 5. New Berlin Gravel Quarry
The gravel quarry has been developed at two levels within a deltaic valley train. The upper level is primarily within the topset beds and the lower level (adjacent to Rt. 8) exposes massive foreset beds. Limestone and associated chert are major lithologic components constituting approximately 26% of all clasts (14% limestone, 12% chert). Postglacial leaching and reprecipitation of carbonates accounts for the various stages of induration found within some of the gravel units.
The topsets consist of 20 to 25 feet of moderately to poorly sorted, horizontal cobble gravels that contain some coarse sand lenses. Coarse lag gravels are common and depict a cut and fill origin. Crude channel cross bedding also is evident. Some of the sand lenses contain small-scale collapse features which are too small to have disturbed the associated gravel.
The underlying foreset beds are inclined at 28° to the southeast (S 30°-50° E) and generally consist of a finer pebbly gravej interbedded with sand. The gravel units consist of both well sorted, clast supported, matrix-free layers and sandy, pebbly fine gravel. The sand ranges from fine to coarse, with occasional silt layers up to 1 foot in thickness. No major collapse features or contorted beds were exposed in 1983.
This deposit is interpreted to be part of a massive deltaic valley train that was prograded downvalley from the New Berlin ice margin (just .5 mile to the north) into an ice-contact lake. The dam was located 15 miles downvalley in the vicinity of Mount Upton and Rockdale. The elevation of the dam corresponds to the topset-foreset contact elevation here. A major dead-ice sink marks the ice-marginal position at the head (upvalley extent) of the valley train. These depositional landforms and their association are helpful in recognizing the valley facies of ice-marginal positions.

Highway follows base of kame terrace scarp for the next 2.5 miles.
Kame terrace stands at 1300 ft. The kame terrace represents outwash shed along an ice margin that paralleled the Unadilla River valley, from New Berlin to Columbus Quarters. Associated kame moraines also occur along the valley, as at South Edmeston on the east side of the valley and Columbus Quarters on the west side. Late glacial discharge from the north (possibly associated with the Valley Heads readvance) dissected all of these ice-marginal landforms.

Highway climbs onto outwash associated with kame moraine

Kame-moraine complex to the right.

Highway descends north side of kame moraine
Highway descends north side of kame moraine, which is part of the New Berlin ice margin

Remnant of Cassville-Cooperstown Moraine
Breached and eroded remnant of Cassville-Cooperstown Moraine can be seen on the valley floor

Outwash plain forming the valley floor
Outwash plain forming the valley floor on the right developed from Valley Heads discharge originating from the north

Outwash surface on the right grades northward to Valley Heads
Outwash surface on the right grades northward to Valley Heads ice-marginal position near Cassville, 3 miles to the north

Characteristic hummocky topography
Road crosses characteristic hummocky topography of Cassville-Cooperstown Moraine for about one mile

Road crosses trend of Valley Heads Moraine
Road crosses trend of Valley Heads Moraine, which is not well expressed in the topography here.

BC9: SEDIMENTOLOGY AND FAUNAL ASSEMBLAGES IN THE HAMILTON GROUP OF CENTRAL NEW YORK
Bruce W. Selleck and Robert M. Linsley
Colgate University
Hamilton, NY 13346
The Middle Devonian (Givetian) Hamilton Group in Central New York State consists of approximately 1600 ft. (approximately 490 meters) of richly fossiliferous interbedded shales, siltstones and sandstones. During Givetian time, the central New York region lay to the west (present geography) of the Appalachian mobile belt. The sediments derived from this orogen were transported to the west and northwest into an epicratonic foreland basin. Other studies (Brett et al., 1983; Baird, 1979) suggest that deposition in western New York took place on a topographically subdued bottom. Regionally, paleoslope was SW-directed, but local swells and depressions of 20-100 km wave length were present (Baird, 1979). In the region of this study, the Hamilton has been the subject of numerous paleontological studies, from the pioneering work of James Hall through the biostratigraphic studies of Cooper (1930, 1933). More recently, the integration of paleontological data and detailed sedimentologic/stratigraphic studies have resulted in the development of depositional/paleoecological models (e.g. Brett et al., 1983). The purpose of this trip is to introduce participants to the varied faunas and lithofacies of the Hamilton and to document the cyclic arrangement of faunas and facies. It is this cyclicity that provides us with a key to understanding the sedimentological evolution of the Hamilton Group.

BC9: SEDIMENTOLOGY AND FAUNAL ASSEMBLAGES IN THE HAMILTON GROUP OF CENTRAL NEW YORK

Active limestone quarry on eastern valley wall.
Low hills in center of valley are part of the Munnsville kame-moraine complex. On the eastern valley wall, an active limestone quarry in the Helderberg Group and Lower Onondaga Limestone is visible.

Outcrops of Upper Helderberg Group and basal Onondaga Limestone (Edgecliff Member) on right.

Outcrop of Seneca Member on right.

Outcrops of Cherry Valley Limestone on right.

STOP 1. Chittenango Shale-Member of Marcellus Fm
Roadcut on left.
Stratigraphy/Sedimentology.
This roadcut exposes a typical section of the black silty shales that dominate the lower Marcellus Formation. Fissile, organic-rich silty shales record deposition on an anaerobic/dysaerobic marine substrate. The extreme limitation of oxygenation and bottom circulation during deposition of this facies suggests that the waters of the basin may have been stratified in a manner analogous to the modern Black Sea. Large carbonate-cemented concretions are well-exposed mid-way up the outcrop face, and cearly demonstrate that pre-compaction cementation occurred. Note that the laminae in the silty shales are deformed by compaction around the concretions. Septarian fractures in the concretions have yielded finely crystalline dolomite, calcite and barite. Note that the surfaces of some concretions appear to have preserved burro and steinkerns of gastropods. Is there a linkage between tne presence of the burrows/fossils and the formation of the concretions?
Fauna
The fauna at this stop is exceedingly limited, dominated by Styliolina with occasional specimens of Nowakia, Leiorhychus and "Euryzone". The styliolinids and Nowakia occur abundantly on particular bedding planes that occur sporadically throughout the section. It is presumed that these are planktonic forms for they are occasionally found in almost all of the lithologies of the Hamilton Group, including the apparently inhospitable environment suggested by these non-bioturbated black shales. It has recently been persuasively argued (Yochelson, in press) that Stylio1ina is not a mollusk, and although he did not assign it to any other higher taxon, we are persuaded that it is safest to assume that it is not a member of an extant phylum, and Fisher's assignment to the Cricocondarida seems as sound as any. Nowakia occurs much more rarely (about 1% of the fauna), but is found with the styliolines and presumably shares a similar mode of life even though taxonomically it is a tentaculitid rather than a styliolinid.
Leiorhychus and "Euryzone" are not usually found in association on the same bedding plane as Styliolina, but scattered throughout the section. Two very different interpretations have been placed on the paleoecology of these genera. It has been suggested that "Euryzone" could have had a mode of life similar to the extant genus Ianthina, which builds a bubble raft to which it clings until it bumps into its prey, the Portuguese Man-of-War, Porcellia. It has similarly been suggested that perhaps Leiorhychus was attached by its pedicle to floating pieces of wood. These interpretations thus attribute the occurrence of these genera to being introduced from outside the immediate environment. However, since both species are restricted to the black shale environment of the Hamilton we suspect that they are indeed adapted to maintaining a marginal existence in an environment that is an abomination to other faunal elements.
(Note: we have placed quotation marks around "Euryzone" because we have never seen a specimen that was determinable below the ordinal level of Archaeogastropoda. Other members of the genus Euryzone are associated with reef deposits and the anomalous environment of the Hamilton form suggests that it is probably not appropriately assigned to this genus.)

STOP 2. Bridgewater and Solsville Members of Marcellus Formation.
The basal section of the exposure here consists of dark, fissile to blocky silty shales which bear a rather limited fauna. The section coarsens upward, corresponding with gradual increase in faunal diversity. The basal portion of the Solsville Member is difficult to access at this stop, but a fair selection of typical Solsville forms can be found in talus mid-way up the exposure.
The preservation of the fossils at this locality is quite exceptional. Thin sections of the material shows that growth lines are well preserved, suggesting that the calcitic shells preserved here are probably original material. Some aragonite is still preserved, but most has been altered to calcite. Still even the mollusks exhibit good growth lines which suggests that the replacement of aragonite is a very precise molecule for molecule substitution.
This unit is also the site of some rather rare and unusual fossils including the monoplacophoran Cyrtolites and the bellerophont Praematarotropis and soft bodied preservation of annelids (Cameron, 1967).
The fauna is dominated by the brachiopods Spinocyrtia in the upper sandier facies, and Mucrospirifer in the middle siltier layers, along with the bivalves, Ptychopteria flabellum, Gosseletia triquetra, and a variety of nuculids, gastropods including Bembexia sulcomarginata and Palaeozygopleura hamiltoniae plus a variety of orthoconic cephalopods.
One unusual aspect of the preservation in this quarry is the fact that a very large percentage of the bivalves are preserved with both valves intact. This is no surprise for nuculids which are infaunal and typically are entombed in the sediments which prevents their valves from gaping open upon death. However, for bysally attached semi-infaunal forms like Gosseletia, mobile semi-infaunal forms like Grammysia and epifaunal genera like Ptychopteria, it is unexpected to find both valves intact. It would seem possible that quick burial may have been an intermittant, but relatively common cause of death in this assemblage. This interpretation is also consistent with the rather large escape burrows that are abundant in this unit.
Many faunal elements in this unit are restricted to single bedding planes that may repeat throughout the quarry. For example, Palaeozygopleura has been found on only three horizons, but within those horizons they may be very abundant. The axis of coiling of the shells of Palaeozygopleura in this quarry are randomly oriented allowing us to infer that they have not been aligned by current action. Yet twice as many are found in an aperture down position as in an aperture up position. Since all positions of this shell exhibit equal hydrodynamic stability, we infer that the shells were occupied at the time of death, and the orientation of the shells reflects the life position.
Other bedding planes are dominated by Bembexia sulcomarginata, a pleurotomarian which was probably an algae grazer or possibly a deposit feeder. Many of the shells of Bembexia in this unit are encrusted with a trepostomatous bryozoan (Leptotrypella). Most frequently it is the upper surface of Bembexia that is encrusted, though some specimens exhibit encrustation of the base while the spire remains clean. Very rarely is a specimen found in which the encrustation spreads very far from one side onto the other.
We suspect that encrustation primarily developed on dead shells on Bembexia. Bembexia is a genus that is only found in the Marcellus and Skaneateles Formations of the Hamilton Group while Palaeozygopleura is found throughout.

STOP 3. Basal Moscow Formation.
This quarry exposes the "interior portion" of a upward-coarsening cycle of the Hamilton Group and can be generalized as consisting of an upper sandy facies dominated by bivalves and a lower silty facies dominated by brachiopods. Separating the two facies is a thin coquina consisting predominantly of the shells of Spinocyrtia granulosa.
The upper sandy unit is dominated by large epi-byssate bivalves and large semi-infaunal bivalves as well as larger spiriferoid brachiopods. There are also occasiona specimens of the burrowing trilobite Trimerus (Dipleura) deKayi and large specimens of Phacops rana.
The lower silty portion of dominated by brachiopods, particularly Chonetes, Devonochonetes, Athyris Rhipidomella, and Mucrospirifer. Bivalves are also abundant, commonly infaunal nuculids or mobile semi-infaunal forms (such as Grammysia). The dominant trilobites in this facies are Greenops and smaller specimens of Phacops. Gastropods are represented by Glyptotomaria and Ruedemannia, the bellerophont Retispira and Palaeozygopleura. Bembexia drops out of the fauna after the Skaneateles. However, the Palaeozygopleura shells in this quarry are barely recognizable for the shells are completely encrusted by the trepostomate bryozoan Leptotrypella. The aperture is always open, but the shell is completely encrusted all the way around which is quite surprising since Palaeozygopleura is a shell dragger, incapable of lifting its shell from the substrate. This leads us to conclude that either Leptotrypella was capable of extending its colony down into the sediment (which no modern bryozoan can do) or that there was a secondary occupant (a sipinculid?) of the dead Palaeozygopleura shell that was capable of elevating the shell off of the substrate so that the bryozoan could establish itself everywhere except the aperture. In some individuals the encrustations became much thicker on one side of the shell than the other, always the adapertural side is thickened, which leads us to believe that the secondary occupant is still occupying the shell, but the mass of bryozans has forced him to resort to a shell dragging mode, thus killing the bryozoans on the apertural side of the colony.
There are also massive colonies of other trepostomatous bryozans in the lower part of the quarry.

STOP 4. Geer Road - Quarry
Stratigraphically and faunally this locality is similar to STOP 3. The faunal elements are essentially as described for the previous locality. Some of the rarer elements of the fauna of both quarries include Hyolithes, occasionally with helens and operculum in place, and two different phyllocarids with their bivalved cephalothorax and segmented abdomen with the telson composed of three spike-like projections.
A prominent surface near the basal portion of the section exposes a phosphate pebble bed containing abundant brachiopods and rare fish plates.

STOP 5. Roadside Quarry and rubble: Mottville Member of Skaneateles Fm.
Roadside Quarry and rubble: Mottville Member of Skaneateles Fm. Sedimentology:
The exposure at this stop nicely exhibits the shaley siltstoneto-sandstone transition of the Mottville Member. The lowermost portion of the outcrop consists of relatively fissile to blocky shaley siltstones dominated by small brachiopods. The section coarsens rapidly upward to silty, fine-grained sandstones which exhibit some cross-lamination and rare hummocky bedding.
Fauna
This stop is dominated by the higher energy faunal elements that characterize the silty sandstones of the Hamilton Group. These include the large epifaunal byssate pectinoid bivalves including Glyptodesma, Leiopteria, Pterinopecten, Actinopteria and Limoptera as well as semi-infaunal bivalves such as Grammysia. The typical trilobite of the unit is the large burrowing trilobite Trimerus, whose punctate carapace comprises one of the dominant skeletal elements of this locality. Complete specimens are fairly common, most commonly not enrolled and not infrequently oriented on edge or on end as some other unusual position relative to the sediments. It is suggestive that the area was occasionally subjected to events, which involved rapid burial. Other common elements include the brachiopods Spinocyrtia, Mucrospirifer, Camarotoec and Devonoproductus. The gastropods are not well preserved here, but include Bembexia and Palaeozygop1eura.

C10: THE LATE WISCONSINAN GLACIATION OF THE WEST CANADA CREEK VALLEY
Jack C. Ridge
Dept. of Geology
Syracuse University
Syracuse, NY
David A. Franzi
Lafayette College
Easton, PA
Ernest H. Muller
This field trip focuses on the glacial stratigraphy of the West Canada Valley and the interpretation of the Late Wisconsinan history ot the region. The Late Wisconsinan stratigraphic record in the West Canada Creek Valley (Figure 1) is unique in central New York in terms of its completeness and in the complexity of the glacial events that it represents. The significance of such lithostratigraphic documentation of the glacial record is underscored by the lack of success in developing a regional glacial chronology based on morphostratigraphic relationships (Coates, 1976; Calkin and others, 1982). Correlations based solely on morphologic evidence are often ambiguous due to the time transgress1ve and composite nature of many glacial landforms. The glacial deposits of the West Canada Creek Valley provide an important lithostratigraphic basis for correlations to the well-developed time-stratigraphic and geologic-climate classifications in the eastern Great Lakes Region (Dreimanis and Karrow, 1972; Dreimanis and Goldthwait, 1973).
The West Canada Creek Valley is an area where the sedimentology of readvance deposits and relative chronology of simultaneous readvances from several different ice flow directions may be studied. Ice from the Ontario Lobe (Black River and Oneida Sublobes) and the Hudson-Champlain Lobe (Mohawk Sublobe) as well as Adirondack through flow and possible Adirondack ice cap sources encroached on this region during the Late Wisconsinan (inset on Figure 1).
The field trip is designed to give an introduction to as many of the glacial stratigraphic units as possible and to show their sedimentologic diversity. It can in no way, however, show all the stratigraphic relationships which were used to determine the glacial history of the region. This would require too many stops for a one day excursion. In addition, many exposures that would be more informative than those shown on this trip are not readily accessible or are inappropriate for a group of this size. Important localities which are not included as stops on the field trip are discussed in the text.

C10: THE LATE WISCONSINAN GLACIATION OF THE WEST CANADA CREEK VALLEY

Kast Bridge.
The course of West Canada Creek has been straightened in this section of the valley. Note the flat topped bluff on east bank of West Canada Creek.

Holland Patent and Norway tills
Bluffs on left side of highway (to west) expose Holland Patent and Norway tills. North Creek enters West Canada Creek from the east. West Canada till and striations on bedrock of the Trenton Group (N60W) are exposed along the last mile of North Creek before it enters West Canada Creek.

Bluffs on east bank of West Canada Creek
Bluffs on east bank of West Canada Creek expose units from Holland Patent till at the top through Norway and Hawthorne tills to West Canada till at the base. The bluffs are typical of many high banks along West Canada Creek between Kast Bridge and Middleville. These bluffs do not exist on the west bank of West Canada Creek because of the asymmetry of the bedrock profile of the valley. The apparent flat-topped surfaces of the bluffs are capped by till and lacustrine sediments. The flat benches may be the result of initial fluvial downcutting in the valley or the floors of lakes that existed during recession of the Barneveld Readvance.

View of STOP 1 from KOA campground.
Bluff on east bank of West Canada Creek (Section 9 on Figure 3). Ahead on left are commercial Herkimer "diamond" (more appropriately Middleville "diamond") prospecting grounds.

Exposures of Little Falls Dolostone on left while entering town of Middleville.

STOP 1. West Canada Creek bluff exposure.
Park vehicles on shoulder of Rt. 169 next to entrance to pasture on right. Walk on dirt road to right to top of hill and across pastures for 0.5 miles to West Canada Creek bluff exposure.
Features and topics for discussion: (Section 9 on Figure 3)
1) Lithology and genesis of unit equivalent to the Norway till.
2) Lithologic and provenance changes within lacustrine sediment between the Norway till equivalent and the Hawthorne till.
3) Nature of contact of Hawthorne till and upper Newport beds.
4) Transition from upper Newport beds to West Canada till.
5) Compact and stony character of West Canada till.
6) Paleomagnetic samples were taken from the upper Newport beds and from three levels within the lacustrine sediments between the Norway till equivalent and the Hawthorne till.

Terrace along West Canada Creek.
Many terraces in the valley are graded to lake levels in the lower West Canada and Mohawk valleys (Figure 13). They contain alluvial fan sediment and slope away from large gullies cut in the glacial deposits along the valley sides.

Outcrops of Little Falls Dolostone
Right side or Rt. 28 and continuing for the next l.5 miles are outcrops of Little Falls Dolostone. Behind the exposure on the right is a large quarry noted for its Herkimer "diamonds".

STOP 2. White Creek
Park vehicles and walk across pasture on west side of White Creek Road.
Features and topics for discussion: (Section 5 on Figure 3)
1) Upper Newport beds appear at top of bluffs in soil profile.
2) Clayey and silty character of West Canada till.
3) Deformation of lower Newport beds beneath West Canada till. Nappe-like folds and thrusts with northwest directed displacement.
4) Transition from lower Newport beds to White Creek till and associated sediment flows.
5) Topography on the upper surface of the White Creek till (morainic or drumlinoid features or neither?).
6) Very stony character of the White Creek till which contains a high proportion of metamorphic clasts.
7) Subglacial grooving on the surface of the White Creek till has been exposed here in the past.

Large bluff on the west bank of West Canada Creek
In view to the west-southwest from this intersection is a large bluff on the west bank of West Canada Creek (Section 6 on Figure 3). This section contains all the units from the lower Newport beds to the Norway till on top.

Hawthorne till overlying upper Newport beds
Right side or highway. Bluff exposure of Hawthorne till overlying upper Newport beds.

Old meander scar of West Canada Creek.
Right side of highway. Across pasture are bluff and gully exposures (Sections 3 and 4 on Figure 3) which contain all units from basal White Creek till up thru Norway till.

Lacustrine sands
Right side of highway. Lacustrine sands which lie stratigraphically below the Norway till and may predate or be time-equivalent to the Hawthorne till and Salisbury Readvance

Fluvial terrace on right
Fluvial terrace on right is inset in an older alluvial fan which slopes toward the center of the valley from large gullies to the northeast.

STOP 3. Poland sand and clay pits.
Two exposures:
1) pit exposing outwash sands. Fluvial sand infilling early incision of the valley cut during fall in lake levels proceeding the Barneveld Readvance.
2) Clay Pit exposure of Phase II sediments.
Section: (similar to Sections 1 and 2 on Figure 3 and northwest end of West Canada Valley profile on Figure 7)
(top) |
6 ft. | oxidized varves (soil profile)
1 ft. | sediment flows
6 ft. | clayey dark gray till with high proportions of sandstone and Trenton Group limestone clasts (Norway till)
1 ft. | deformed lacustrine beds
4 ft. | thin varve couplets (less than 2 inches) containing a p1nk and tan clay component and red rain-out sediment (Oneida Sublobe provenance); flutes indicate paleocurrent flow to the southeast.
12 ft. | thick varve couplets (greater than 2 inches) with dark gray and drab colors and black rain-out sediment near base (Mohawk Sublobe provenance); couplets thicken downward; rib and furrow structures indicate paleocurrent flow to the northwest.
2 ft. | lacustrine sand and silt, oxidized at top and contain calcareous cement
25 ft. | rippled lacustrine sands with calcareous cemented layers and lenses; paleocurrent flow to the east
| (limit of exposure)
Note especially change from Mohawk to Oneida Sublobe provenance within the varve section accompanied by a change in paleocurrent directions from northwest to southeast.

Ice-marginal delta at the maximum position of the Barneveld Readvance.
Flat-topped hill to right with gravel pit excavations is capped by an ice-marginal delta at the maximum position of the Barneveld Readvance.

STOP 4. Cincinnati Creek sections (Figure 5).

Incised portion of a delta
The highway crosses an incised portion of a delta deposited during recession from the Hinckley Readvance.

Hinckley Moraine System
Hills on both sides of the highway are a part of the Hinckley Moraine System.

Exposure on the east side of the road
Exposure on the east side of the road contains calcareous western provenance gravel overlying older non-calcareous gravel of Adirondack provenance.

STOP 5. Dirt driveway leading to Trail's End bluff
Dirt driveway leading to Trail's End bluff exposure on Hinckley Reservoir (Figure 10). NOTE: This is private property.

STOP 6. Balley Hills delta.

Hummocky topography
On both sides of the road is hummocky topography resulting from stagnation of the Black River Sub lobe as it thinned over the Black River-West Canada Creek divide during recession from the Hinckley Readvance. The drift is composed of both stratified deposits and ablation till.

C11: STRUCTURE AND ROCK FABRIC WITHIN THE CENTRAL AND SOUTHERN ADIRONDACKS
James McLelland
Colgate University
Hamilton, NY
2011: This following trips are identical:

C11: STRUCTURE AND ROCK FABRIC WITHIN THE CENTRAL AND SOUTHERN ADIRONDACKS

STOP 1. Peck Lake Fm.
This exposure along Rt. 29A just north of Peck Lake is the type locality of the sillimanite-garnet-biotite-quartz-feldspar gneisses (kinzigites) of the Peck Lake Fm. In addition, there are exposed excellent minor folds of several generations. Note that the F2 folds rotate an earlier foliation.
The white quartzo-feldspathic layers in the kinzigites consist of quartz, two feldspars, and garnet and are believed to be anatectic. Note that fish-hook terminations on some of these suggest that they have been transposed. It is also clear that these anatectites have been folded by F2 indicating a pre-F2 metamorphic event(s). In a similar fashion some garnets in the rock appear to be flattened while others do not. It is believed that the anatectites formed at the muscovite-quartz reaction and are essentially in situ melts. Further anatexis did not take place due to absence of vapor.

STOP 2. Irving Pond Fm., .5 mile north of Nick Stoner's Inn, Canada Lake .
The outer portion of the Irving Pond Fm. is exposed in low cuts along the east side of Rt. 29A just prior to the crest in the road heading north.
At the southern end of the cut typical, massive quartzites of the Irving Pond are seen. Proceeding north the quartzites become "dirtier" until they are essentially quartzose sillimanitegarnet-biotite-feldspar gneisses (kinzigites).
At the northern end of the cut, and approximately on the Irving Pond/Canada Lake Fm. contact there occurs an excellent set of F2 minor folds. Polished slabs and thin sections demonstrate that these fold an earlier foliation defined by biotite flakes and flattened quartz grains.
The Irving Pond Fm. is the uppermost unit in the stratigraphy of the southern Adirondacks. Its present thickness is close to 1000 meters, and it is exposed across strike for approximately 4000 meters. Throughout this section massive quartzites dominate.

STOP 3. Canada Lake Charnockite
These large roadcuts expose the type section of the Canada Lake charnockite. Lithologically the charnockite consists of 20-30% quartz, 40-50% mesoperthite, 20-30% oligoclase, and 5-10% mafics. The occurrence of orthopyroxene is sporadic. These exposures exhibit the olive-drab coloration that is typical of charnockites. Note the strong foliation in the rock.
Although no proto1ith is known with certainty for these rocks a metavolcanic history is suggested by their homogeneity and lateral continuity. Their bulk chemistry corresponds to dacites.

Canada Lake Store. Good exposures of Royal Mt. member of Green Lake Fill.

STOP 4. Rooster Hill megacrystic gneiss at the north end of Stoner Lake.
This distinctive unit is believed to be, in part, correlative with the Little Moose Mt. Fm. Here the unit consists of a monotonous series of unlayered to poorly layered gneisses characterized by large (1-4") megacrysts of perthite and microcline perthite. For the most part these megacrysts have been flattened in the plane of foliation as well as elongated in an E-W direction with concomitant developed of tails of grain-size reduced tails asymmetric to foliation. However, a few megacrysts are situated at high angles to the foliation. The groundmass consists of quartz, oligoclase, biotite, hornblende, garnet, and occasional orthopyroxene. An igneous rock analogue would be quartz-monzonite or granodiorite depending on concentration of K-feldspar.
The origin of the Rooster Hill is obscure. Its homogeneity over a thickness approaching 2.5 km suggests an igneous parentage. This conclusion gains support from the presence of localities where megacrysts appear to retain a random orientation, and from the occasional presence of what may be drawn out xenoliths of biotitic or amphibolitic gneisses. However, these features may be explained by other models. The contacts of the Rooster Hill are always conformable with enclosing units, and this suggests a metastratified (metavolcanic?) origin. However, the anorthosites of the region also show conformable contacts, and this may, in part, be due to tectonic flattening.
Recently Eckelmann (pers. comm.) has studied zircon population morphologies in the Rooster Hill and similar lithologies. His results strongly suggest an igneous plutonic origin. This would be consistent with the igneous origin assigned the Hermon granite of the northwest Adirondacks - a rock that is markedly similar to the Rooster Hill.

Low roadcut in kinzigites of Tomany Mt. Fm.

Long roadcuts of quartzo-feldspathic gneisses and metasediments
Long roadcuts of quartzo-feldspathic gneisses and metasediments of Lake Durant Fm. intruded by metagabbro and anorthositic metagabbro.

Roadcut of anorthositic metagabbro and metanorite.

Excellent examples of anorthositic gabbros
Roadcut on west side of highway shows excellent examples of anorthositic gabbros intrusive into layered pink and light green quartzo-feldspathic gneisses. The presence of pegmatites and cross-cutting granitic veins is attributed to anatexis of the quartzo-feldspathic gneisses by the anorthositic rocks.

Stop 5. Lake Durant and Sacandaga Fms.
Stop 5. Lake Durant and Sacandaga Fms. intruded by anorthositic gabbros and gabbroic anorthosites. These roadcuts are located on Rt. NY 10 just south of Shaker Place.
The northernmost roadcut consists of a variety of metasedimentary rocks. These lie directly above the Piseco anticline and are believed to be stratigraphically equivalent to the Sacandaga Formation. The outcrop displays at least two phases of folding and their related fabric elements. These are believed to be F2 and F3. A pre-F2 foliation is thought to be present. Both axial plane foliations are well developed here. Several examples of folded F2 closures are present and F2 foliations (parallel to layering) can be seen being folded about upright F3 axial planes.
Farther to the south, and overlooking a bend in the west branch of the Sacandaga River, there occurs a long roadcut consisting principally of pink and light green quartz-perthite gneiss belonging to the Lake Durant Fm. About half-way down this roadcut there occurs a large boudin of actinolitic and diopsidic gneiss. To the north of the boudin the quartzo-feldspathic gneisses are intruded pervasively by anorthositic gabbros, gabbroic anorthosites, and various other related igneous varieties. At the north end of the cut and prior to the metastratified sequences these intrusives can be seen folded by upright fold axes. They are crosscut by quartzo-feldspathic material.
Within this general region the Lake Durant Fm. and other quartzofeldspathic gneisses seem to have undergone substantial anatexis. This is suggested by the "nebular" aspect of the rocks. Good examples of this are seen in the manner in which green and pink portions of the quartzo-feldspathic gneisses mix. Note also the clearly cross-cutting relationships between quartzofeldspathic gneiss and mafic layers at the south end of the roadcut. Here it seems that mobilized Lake Durant is cross-cutting its own internal stratigraphy. Also note that the quantity of pegmatitic material is greater than usual. This increase in anatectic phenomena correlates closely with the appearance of extensive metagabbroic and metanorthositic rocks in this area. It is believed that these provided a substantial portion of the heat that resulted in partial fusion of the quartzo-fe1dspathic country rock.

Red-stained basal quartzo-feldspathic gneisses that have been faulted along NNE fractures.

Stop 6. Core rocks of the Piseco anticline.
Hinge line of Piseco anticline near domical culmination at Piseco Lake. The rocks here are typical basal quartzo-feldspathic gneisses such as occur in the Piseco anticline and in other large anticlinal structures, for example Snowy Mt. dome, Oregon dome.
The pink "granitic" gneisses of the Piseco anticline do not exhibit marked lithologic variation. Locally grain size is variable and in places megacrysts seem to have been grain size reduced and only a few small remnants of cores are seen. The open folds at this locality are minor folds of the F3 event. Their axes trend N70W and plunge 10-15° SE parallel to the Piseco anticline. Co-axial F2 isoclines are also present.
The most striking aspect of the gneisses in the Piseco anticline is their well-developed lineation. This is expressed by rodding and ribbon fabrics. These may consist of alternating ribbons of quartz, quartzo-feldspathic gneiss, and biotite-rich layers. In some instances the rods represent transposed layering on the highly attenuated limbs of early, isoclinal minor folds. Near the northeast end of the roadcut such minor folds are easily seen due to the presence of more massive layers in the rock. Slabbed and polished specimens from this and similar outcrops demonstrates that these early folds are exceedingly abundant in the Piseco anticline. Examination of these folds shows that the dominant foliation in the rock is axial planar to them.
The lineation in these outcrops is shown in Fig. 8a while slabbed sections are shown in Figs. 8b,c. Fig. 8b is cut perpendicular to foliation and both parallel to (left face) and perpendicular to (right face) lineation. As can be seen K-feldspar augen have been elongated in the direction of lineation. Together with elongated quartz aggregates, these grain size reduced minerals form the prominent mineral lineation that characterizes foliation surfaces (Fig. 8a). Note that the K-feldspar augen exhibit shapes closer to equant on the right hand face at perpendicular to lineation. This strongly suggests that the rock fabric is the result of rotational strain in the direction parallel to lineation, i.e., the lineation is an elongation, or stretching type. Fig. 9 shows a less deformed sample slabbed perpendicular to foliation and parallel to lineation. The development of tails on K-feldspar augen are clearly visible. These are the result of grain size reduction during ductile rotational strain. A sinistral (east over west) sense of motion is indicated. At more extreme conditions of strain the K-feldspar augen and quartz aggregates are drawn into ribbons as in the present outcrop. Long dimensions of 40-60 cm are common along with thicknesses of a millimeter, or less. Clearly strain has been extreme and elongations of 30-40 times are not unusual.
Ribbon gneiss origin by rotational strain is also suggested by the parallelism between lineation and F2, F3 fold axes. It is believed that these fold axes were drawn into parallelism with the lineation by ductile, rotational strain directed from east to west. The most satisfactory mechanism for this configuration is the stacking of thrust sheets and thrust nappes during plate collision. Thrusts have been recognized to the east of Lake George (Fig. 4) and others probably exist although the intense, ductile nature of the deformation has resulted in extremely subtle truncations that are difficult to recognize. Sheath folds (Fig. 10) with tube axes parallel to lineation are consistent with this model. Presumably crustal thickening during the Grenville Orogeny was caused by the stacking of these thrusts.

Stop 7. Blue Mt. Lake Fm. exposed in roadcuts on both sides of highway.
The Blue Mt. Lake Fm. is exposed in roadcuts on both sides of the highway. These exposures show typical examples of the extreme ductility of the carbonate-rich units. The south wall of the roadcut is particularly striking, for here relatively brittle layers of garnetiferous amphibolite have been intensely boudinaged and broken. The marbles, on the other hand, have yielded plastically and flowed with ease during the deformation. As a result the marble-amphibolite relationships are similar to those that would be expected between magma and country rock. Numerous rotated, angular blocks of amphibolite are scattered throughout the marble in the fashion of xenolith, in igneous intrusions. At the eastern end of the outcrop tight isoclinal folds of amphibolite and metapelitic gneisses have been broken apart and rotated. The isolated fold noses that rema in "floating" in the marble have been aptly termed "tectonic fish." The early, isoclinal folds rotate on earlier fo1iation.
Near the west end of the outcrop a deformed layer of charnockite is well exposed. In other places the charnockite-marble interlayering occurs on the scale of one to two inches.
Exposed at several places in the roadcut are cross-cutting veins of tourmaline and quartz displaying a symplectic type of intergrowth. Other veins include hornblende and sphene bearing pegmatites.
Commonly included in the Blue Mt. lake Fm., but not exposed here, are quartzites, kinzigites; sillimanite rich, garnetiferous quartz-microcline gneisses; and fine grained garnetiferous leucogneisses identical to those characterizing the Sacandaga Fm. These lithologies may be seen in roadcuts .5 mile to the south.
Almost certainly these marbles are of inorganic origin. No calcium carbonate secreting organisms appear to have existed during the time in which these carbonates were deposited (> 1 b.y. ago). Presumably the graphite represents remains of stromatolite-like binding algae that operated in shallow water, intertidal zones. If so, the other roadcut lithologies formed in this environment as well. This seems reasonable enough for the clearly metasedimentary units such as the quartzites and kinzigites. The shallow water environment is much more interesting when applied to the charnockitic and amphibolite layers. The fine scale layering, and ubiquitous conformity of these, strongly suggests that they do not have an intrusive origin. Perhaps they represent the metamorphosed products of volcanic material in a shelf like environment. Such intercalation is now occurring in many island arc areas where shallow water sediments cover, and in turn are covered by, ash and lava. Alternatively they may represent metasediments. A large lumber of minerals are developed within these outcrops. Both calcite and minor dolomite are present in the carbonate horizons. These are accompanied by green diopside and serpentinized forsterite as well as by tourmaline, graphite, and various sulfides. In calcsilicate horizons phlogopite, diopside (white), and tremolite occur. Wollastonite is locally present. The presence of tremolite and wollastonite is believed to be a function of the relative concentration of CO2 and H2O in the vapor phase Valley et al., 1983).

Extensive roadcuts in lower part of Blue Mt. Lake Fm.
Quartzites, kinzigites, and leucogneisses dominate. Minor marble and calcsilicate rock is present.

Large roadcuts in lower Lake Durant Fm.
Pink, well-layered quartzo-feldspathic gneisses with subordinate amphibolite and calcsilicate rock.

Stop 8. Intermediate Adirondack anorthositic gneiss
On the west side of the road small roadcut exposes an excellent example of Adirondack anorthositic gneiss intermediate in character between the so-called Marcy type (coarse) and the Whiteface type (fine grained). About 50% of the rock consists of fine grained crystals of andesine plagioclase. Some of these crystals appear to have measured from 6-8" prior to grain size reduction. Excellent moonstone sheen can be seen in most crystals. In places ophitic to subophitic texture has been preserved with the mafic phase being represented by orthopyroxene.
In addition to the anorthosite there exists a clearly crosscutting set of late iron-rich orthopyroxene rich dikes containing xenoliths of coarse grained anorthosite. The latter may represent a late mafic differentiate related to cotetic liquids responsible for the ophitic intracrystalline rest magma. This would be consistent with the iron enrichment trend characteristic of Adirondack igneous differentiation.
Near road level there can be found several inclusions of calcsilicate within the anorthositic rocks. These are believed to have been derived from the Cedar River Fm. and are consistent with a non-basement status for the anorthosite.
The upper, weathered surface of the outcrop affords the best vantage point for studying the textures and mineralogy of the anorthositic rocks. In several places there can be seen excellent examples of garnet coronas of the type that are common throughout Adirondack anorthosites. These coronas are characterized by garnet rims developed around iron-titanium oxides and pyroxenes. Recently McLelland and Whitney (1977) have succeeded in describing the development of these coronas according to the following generalized reaction:
Orthopyroxene + Plagioclase + Fe-bearing oxide + quartz = garnet + clinopyroxene.
This reaction is similar to one proposed by de Waard (1965) but includes Fe-oxide and quartz as necessary reactant phases. The products are typomorphic of the garnet-clinopyroxene subfacies of the granulite facies (de Waard 1965). The application of various geothermometers to the phases present suggests that the P,T conditions of metamorphism were approximately 8 Kb and 700 ± 50°C respectively.

Cedar River Fm. Minor marble, amphibolite, and calcsilicate rock.
Predominantly very light colored sillimanite-garnet-quartz-K-feldspar leucogneisses.

Leucogneisses of the Blue Mt. Lake Fm.
To the west of the intersection are roadcuts in leucogneisses of the Blue Mt. Lake Fm. A large NNE normal fault passes through here and fault breccias may be found in the roadcut and the woods beyond.

Entering Little Moose Mt. Fm.
Entering Little Moose Mt. Fm. on northern limb of the Glens Falls syncline. Note that dips of foliation are to the south.

Downdropped block of lower Paleozoic sediments.
Entering town of Wells which is situated on a downdropped block of lower Paleozoic sediments. The minimum displacement along the NNE border faults has been determined to be at least 1000 meters.

Silver Bells ski area to the east.
The slopes of the ski hill are underlain by coarse anorthositic gabbro intrusive into the Blue Mt. Lake Fm.

Lake Durant Fm
On the north side of NY Rt. 30 are quartzo-feldspathic gneisses and calcsilicate rocks of the Lake Durant Fm. An F1 recumbent fold trends subparallel to the outcrop and along its hinge line dips become vertical.

Gabbro and anorthositic gabbro.

Stop 9. Pumpkin Hollow.
Large roadcuts on the east side of Rt. 30 expose excellent examples of the Sacandaga Fm. At the northern end of the outcrop typical two pyroxene-plagioclase granulites can be seen. The central part of the outcrop contains good light colored sillimanite-garnet-microcline-quartz gneisses (leucogneisses). Although the weathered surface of these rocks are often dark due to staining, fresh samples display the typical light color of the Sacandaga Fm. The characteristic excellent layering of the Sacandaga Fm. is clearly developed. Note the strong flattening parallel to layering and the lineation developed on many foliation surfaces. These gneisses are similar to so-called straight gneisses found in proximity to ductile shear zones. The Sacandaga Fm. may represent mylonitic rocks of this type and its layering may, in fact, be tectonic.
Towards the southern end of the outcrop calc-silicates and marbles make their entrance into the section. At one fresh surface a thin layer of diopsidic marble is exposed. NO HAMMERING PLEASE. Many "punky" weathering layers in the outcrop contain calc-silicates and carbonates.
At the far southern end of the roadcut there exists an exposure of the contact between the quartzo-feldspathic gneisses of the Piseco anticline and the overlying Sacandaga Fm. The hills to the south are composed of homogeneous quartzofeldspathic gneisses coring the Piseco anticline (note how ruggedly this massive unit weathers). The Sacandaga Fm. here has a northerly dip off the northern flank of the Piseco anticline and begins its descent into the southern limb of the Glens Falls syncline.
No angular discordance or other indications of unconformity can be discerned at the base of the Sacandaga Fm. However, this does not preclude the prior existence of an angular discordance which may have been swept into pseudoconformity by tectonism.
Along most of the roadcut there can be found excellent examples of faults and associated pegmatite veins. Note that the drag on several of the faults gives conflicting senses of displacement. The cause of this is not known to the author. Also note the drag folds which indicate tectonic transport towards the hinge line of the Piseco anticline.

Core of the Piseco anticline.
All exposures are within the basal quartzo-feldspathic gneisses at the core of the Piseco anticline.

Re-enter the Sacandaga Fm. Dips are now southerly.

Southerly dipping quartzo-feldspathic gneisses of Lake Durant Fm.
In long roadcuts of southerly dipping quartzo-feldspathic gneisses of Lake Durant Fm.

C12: GROUNDWATER CONTAMINATION FROM A SANITARY LANDFILL: INVESTIGATIONS, REMEDIAL ACTION AND ENERGY RECOVERY AS A POSSIBLE SOLUTION
Kenneth Jeffrey Goldstein
Environmental / Water Resourse Planner
Oneida County Planning and Environmental Management Council
Utica, New York
PURPOSE
The purpose of this field trip is to view the adverse impacts resulting from the improper disposal of solid and hazardous wastes. A tour of the Rome Sanitary Landfill will reveal the impacts on the environment resulting from hazardous waste landfill leachate. Leachate can be seen at the landfill and in nearby streams. The participants will be able to view the remedial measurees being conducted at the site, including, the construction of a barrier cap, gas vents and monitoring wells. A discussion on the elements of the site investigation and remedial actions utilized will be conducted while touring the facility. Questions are encouraged! Later in the day the participants will tour the Oneida County Energy Recovery Facility in Rome, N.Y. This facility, which will not be operational at the time of the field trip, is one of Oneida County's solutions to the land burial of industrial and municipal solid waste. Although the facility will not be operational, all equipment will be on-line and will be reviewed.

C13: SEISMICITY IN THE CENTRAL ADIRONDACKS WITH EMPHASIS ON THE GOODNOW, 10/7/84 EPICENTRAL ZONE AND ITS GEOLOGY
Lamont-Doherty Geological Observatory
of Columbia University
Palisades, New York, 10964

FIELD TRIP GUIDEBOOK
Richard H. Lindemann, Editor
Department of Geology Skidmore College
Saratoga Springs, N.Y.

A1: A TRIP TO THE TACONIC PROBLEM AND BACK
PHILIP C. HEWITT
Department of the Earth Sciences
SUNY College at Brockport
Brockport, NY 14420
The purpose of this paper is to provide background information needed for both the full-day trip (A1) and the half-day trip (B1). The full day trip involves data from the entire paper while the half-day trip concentrates on the Taconic Problem primarily. However, to understand either day fully, the entire paper must be read. A separate Road Log for each trip is provided at the end of the paper.
The paper describes geologic features to be examined in area from Saratoga Springs, N.Y. to Manchester, Vt. A discussion and overview of the Taconic region and the "Taconic Problem" will be presented. Consideration will be given to both the sequential and fault hypotheses proposed for the High Taconic region.
The Taconic region is subdivided into the High Taconics and the Low Taconics based on the extreme difference in relief. The High Taconics are the mountains of Vermont, west of the Vermont Valley, with elevations of approximately 3000-4000 ft. The Low Taconics are the hills primarily in New York, west of the High Taconics, with elevations up to approximately 1500 ft. (Hewitt, 1961a). Lithologic and other distinctions will become apparent in the later discussion.

A1: A TRIP TO THE TACONIC PROBLEM AND BACK

STOP 1. The Springs, Tufa Terrace, And Flat-Lying Snake Hill Shale
The Spring along the pathway is typical of the mineralized and carbonated springs in the region. Do taste the water but with caution. Firstly, the water at this Spring passes through the dark shale and therefore, contains iron and sulfur. The amount of sufur is sufficient to "surprise" the unwary. Secondly, the water contains the radioactive gas radon. Thirdly, the bedrock from which the water rises is a dolostone and in addition to the calcium it contains magnesium. Therefore, this water is an excellent laxative. "A word to the wise is sufficient."
All of the springs are the result of the expansion, along the faults, of carbon dioxide gas released by the weathering of dolomite at depth. Acid water percolates downward to the dolostone, weathers the rock and forms mineralized water plus gas. As the water reaches the faults the carbon dioxide gas expands with the reduction of pressure and the gas carries the water to the surface.
The "Island Spouter" is, of course, not truly a geyser. In this case it is gas within a constricting pipe which allows the water to spurt into the air.
Walk north approximately 500 ft. along the path. Note dark gray to black flat-lying shale. Approximate equivalents to these shales (Snake Hill, Canajoharie?) will be seen later as metamorphic rock. These shales are medial Ordovician in age.
Note the Tufa Terrace. Formed of colloidal and precipitated calcium carbonate from the Spring on the hill above (west) the terrace. Here leaves and insect fossils are formed each year as the organic material is trapped, coated and then permineralized with the calcium carbonate.

Sand dunes.
Some totally and partially exhumed. Probably from Lake Albany equivalent. Note long axes to west. Possible 5 minute "extra" stop here if time permits.

View of Taconics ahead (east).

Saratoga National Monument on right.
Battle of Saratoga took place here during Revolutionary War.

STOP 2. Stark's Knob Area. Folded, Distorted Shale
Note badly distorted black shale on right side of road. These are equivalent of those at Stop 1 (Snake Hill). This is part of Logan's Zone and the rocks are faulted, badly fractured and somewhat metamorphosed. Note limestone and dolostone pebbles (gray to blue-gray) in shale and oxidation of parts of shale surfaces. Limestone and dolostones are not indigenous to this locality. They are from the area far to the east. We will see these later in the day in situ. The red oxidized zone probably represents a "baked" zone as the area moved westward during faulting. The "baking" might also have resulted from the emplacement of the basaltic pillow lavas of which Stark's Knob is composed.
Walk uphill and to the right for a quick examination of Stark's Knob.
This is a flow of basalt (now pillow basalt) which apparently formed when lava flowed into the sea and across a shaly (or muddy) shoreline with fragments of limestone and dolostone present. The lava and the shale which enclosed it were later thrust westward during the faulting which produced Logan's Zone. We will see basic material similar to this lava but as dikes on Rt. 7 in Vermont. Stark's Knob was formerly used as road metal.
The basalt and the shale are both of medial Ordovician age. Return to cars.

Note folded black shales on right side of road along route.

STOP 3. Folded Wallomsac Formation
This outcrop exposes typical black slate and metamorphosed sandstone (now quartzite) of the Walloomsac formation. Strata here are strongly folded and thrust faulted. Cleavage is readily visible. There is some mineralization along the faults. Folds of various magnitudes may be observed here. This outcrop expresses well the folding in the Low Taconics. Virtually every bed is slickensided. Some folds show evidence of refolding.
No fossils have been found to verify the age of this outcrop. However, it maps well into the Walloomsac which is generally considered to be medial Ordovician (Trentonian) in age. It is probably correlative with the Snake Hill. However, lithologically it resembles the Austin Glen member of the Normanskill formation more closely. This unit is believed to be older than the Snake Hill but still medial Ordovician.

Black slates and phyllites on both sides of roads.
Black slates and phyllites on both sides of roads. These are visible in many locations along the road.

STOP 4. Green Slate And Black Slate Outcrop
Green slate (or phyllite) is exposed on the left (northwest) side of the road. Black slate (or phyllite) lies across the road on the southeast side. The decision as to whether these are slates or phyllites is rather subjective since they appear to border both lithologies. Beds appear to dip to the southeast which is common in the area. The green slates appear to lie under the black beds. The age of the black phyllites is probably medial Ordovician since they are on strike with the Walloomsac beds. If so, they lie above green beds which, in many ways, resemble those of the beds further east in the High Taconics. The green slates are also on strike with known Cambrian beds of the Mettawee slates (the famous purple and green slates) in the Taconic sequence. Some few purple beds are seen at this locality also but they are better exposed 1.6 miles northeast along Rt. 313. Purple and green Mettawee slates are well known in the northwest part of the Equinox quadrangle. The author considers the green slates to be Cambrian Mettawee formation and the black slates to be Walloomsac. In this case a major unconformity is present. This is probably the unconformity recognized by MacFadyen (1956), Thompson (1959) and others. Return to cars. Continue on Rt. 313 to northeast.

Interfolded black and green slates.

Purple and green slates.

Tight folding, chevron folds in green phyllite
Tight folding, chevron folds in green phyllite (Mt. Anthony fm.) in Vermont. On left (north). These are the same phyllites which lie over the carbonate in the High Taconics. Since crossing the State Line into Vermont, we have been in the High Taconics.

STOP 5. Ordovician Carbonate Outcrop
Covered Bridge on right (south) and dolomitic marble outcrop on left (north) Pull to right past Covered Bridge and park.
This outcrop of medial Ordovician gray to blue-gray dolomitic marble contains many fossil fragments (crinoid, cystoid and related groups) and a few remains of a Trentonian cephalopod (probably Endoceras proteiforme). This establishes these strata as medial Ordovician in age. Although these beds resemble closely the Bascom-Beldens (undifferentiated), the age is too young. The Bascom-Beldens is generally considered to be of early Ordovician age. Therefore, these fossiliferous middle Ordovician rocks were mapped separately and with the associated black phyllite as the lower Mt. Anthony formation (Hewitt, 1961a). If the upper part of the Beldens could be demonstrated to be Trentonian (medial Ordovician) these beds could easily be placed, on purely lithologic grounds in that formation.
The strata at this outcrop directly underlie the green phyllites of the High Taconics assigned to the Mt. Anthony formation (MacFadyen, 1956). It is the nature of the contact between these units that is the crux of the present Taconic problem (see paper preceeding this Road Log for details). Some evidence of that contact will be seen at a later stop and more definitive evidence is presented at Stop 2 of the Road Log for the trip entitled "The Nature of the eastern Taconic Contact."
Although some observers may conclude that the folding at this locality is not extreme, it should be noted that green phyllite probably lies below the surface as well as above the carbonate. Many of the beds are up-sidedown and generally the outcrop is an inverted section at road level. Further up the hill above (north) the road the strata are right-side-up.
Some sandy beds show cross-bedding that helps to establish this but the extreme overturning of these folds will be very apparent as the field trip progresses. The nature of the synclinorium actually requires this as our eastward travel will demonstrate. Please return to the cars and drive east, staying on Rt. 313. Note carbonate on drive eastward. We will examine these later.

This is the west side of the Vermont Valley.
Outcrops within the Valley are Cambro-Ordovician Valley sequence strata. On right (east) are the Green Mtns. of Precambrian to earliest Cambrian age.

View of Mt. Equinox ahead.

Delta deposit on left (west) from post-glacial lake (Lake Bennington?).

STOP 6. Mt. Equinox
No mileages will be provided for the drive up Mt. Equinox since easily recognizeable stopping places have been provided. Drive carefully both up and down the mountain! If you do not have faith in your car's brakes and transmission do not attempt the drive. The drive will test your car.
The road up starts gently in the Shelburn formation with a lower member (Sutherland Falls) of creamy to white calcitic marble, a middle (Intermediate dolomite) member and an upper Columbian marble, the commercial marble of the Vermont Marble Belt. None of this formation is exposed until the first bench or terrace is reached. Elsewhere on the mountain, excellent exposures of all three members are easily observed.
Park at the Parking Lot at the first terrace. This is our lunch stop. Rest rooms are opposite the Parking Lot about 300 ft. to the south. Enjoy the view but please keep the area clean.
Before returning to the cars, gather at the picnic tables for a discussion of the geology, history and culture of the mountain. If time permits we will visit a small marble quarry about 900 ft. north of the Parking Lot at an elevation 100 ft. lower than the Parking Lot. You may collect at this quarry. Return to cars and continue drive up the mountain. Do not stop on the road but note when green phyllite first appears. This occurs after first private road on your right (northeast). Continue climb.
Park at Parking Lot on second terrace. This locality is in the green phyllite. It provides excellent samples of the phyllite, pyrite cubes, and pseudomorphs of limonite (goethite) after pyrite, particularly in the northwest part of the exposure. Collect all you want. Return to cars and continue climb.
At first flat area, note Little Equinox Mtn. on right (southeast) and Lake Madelaine on left (west). Note also areas of landslides on right (east) side of sharp turns near top of Mt. Equinox. One of these will be climbed on foot on the trip discussing "The Nature of the eastern Taconic Contact".
At the summit, park but leave car engine running at fast idle for a few minutes before shutting down. This will help cool the engine. Gather in Parking Lot for orientation, geomorphology and overview of Taconic area.
Descend mountain. Keep car in LOW GEAR while descending. Brakes have been known to fade and even burn on descent. Stop at first flat area below summit for view of Lake Madelaine and monastery. Lake Madelaine is totally artificial. That area was formerly Big Spruce Swamp. Continue to base of mountain. Stay in LOW GEAR.

Note Cook Hollow on left (west).
White flat outcrop is Table Rock composed of white marble (Columbian?), Landslide Scar visible above Table Rock. This is carbonate-green phyllite eastern Taconic contact. Hewitt (1961a) concludes that this is a gradational contact.

STOP 7. Dolomite Outcrop. Basic Dikes
This is the Winooski dolostone of medial Cambrian age. Bedding and jointing permit blocks to fall easily so caution is important here. Note basic dikes in wall of exposure near north end.

STOP 8. Overturned Fold
This structure is a classic fold in the Bascom-Beldens formation. The lithology is dolomitic marble and the folding is typical Taconic folding. BE CAUTIOUS AT THIS OUTCROP. FOLLOW DIRECTIONS OF THOSE DIRECTING TRAFFIC. THEY ARE THERE FOR YOUR PROTECTION.

STOP 9. Carbonate-Green Phyllite Contact
Turn left (northwest) over one lane bridge. Corkscrew turn in folded Mt. Anthony formation. Drive through turn and turn at next intersection and reverse direction. Park at end (southeast) of large outcrop.
The green phyllite (Mt. Anthony formation of MacFadyen (1956)) is well exposed here. Intense folding is obvious. These are small folds on successively larger folds in this area. With care, small folds may be collected here. All of this section appears on first glance to be green phyllite. However, at the southeast corner of the last outcrop on this road the application of cold, dilute hydrochloric acid results in effervescence at the base. It is impossible visually to locate the horizon at which calcium carbonate ends and the phyllite begins. Only an acid reaction or lack of it can determine the difference. Is there a fault here or not? It is up to you to decide. Note the valley to the south. Is this a depression within the phyllite or the result of solution of a carbonate? No outcrops have been located within that depression but plentiful float is found there.

A2: THRUSTS, MELANGES, FOLDED THRUSTS AND DUPLEXES IN THE TACONIC FORELAND
WILLIAM BOSWORTH
Marathon International Oil Company P.O. Box 3128
Houston, Texas 77253
WILLIAM S. F. KIDD
S.U.N.Y of Albany
Albany, New York 12222

A2: THRUSTS, MELANGES, FOLDED THRUSTS AND DUPLEXES IN THE TACONIC FORELAND

STOP 1A. Potsdam Formation
Quartzites, arenites and dolomitic micrites of the Potsdam Formation (medial Cambrian). Williams Street in Whitehall.
Grenville gneisses are exposed in the riverbed directly below this outcrop; although the unconformity is not exposed here, it is elsewhere along strike north and south. The main purpose of this stop is to see that the strata in this outcrop show no prominent signs of deformation, being part of a gently east-dipping regional homocline. Although not a main focus of this field trip, the evidence for both shallow marine to beach facies (prominently cross-bedded and rippled clean arenites and quartzites) and lagoonal supratidalflat facies (dolomitized micrites and thin shales, laminated in places with small stromatolites and locally with sand-filled vertical burrows) are well displayed here. Some layers, with pebbles of dolomitized micrite, may well be storm deposits.

STOP 1B. Limestones of the Whitehall Formation (late Cambrian).
Sciota Road 1.6 miles from Whitehall. These strata also are part of the regional gently east-dipping homocline of autochthonous shelf strata (typically 5-10 degrees east dip). No folds or cleavage are visible in these strata, and oolites which are locally abundant in some beds do not appear strained to any significant extent. Stylolites do occur in some beds but they are bedding-parallel, presumably compactional in origin. Laminated algal micrites, locally stromatolitic, can be seen, along with micrite edgewise breccias with oolites, all evidence of shallow marine to intertidal/supratidal facies. Nodular chert layers occur locally in this outcrop. It should be emphasized that most of the volume of the pre-medial Ordovician autochthonous shelf sequence is dolostone. Limestones form an overall small proportion and this unit (part of the Whitehall Formation) is, after the medial Ordovician limestones, the most prominent limestone in the early Paleozoic shelf sequence. Dolostones occur at the east end of the quarry where the outcrop nears the road - we will not examine these.

STOP 2. Thrust of limestones over shaley melange.
Thrust of medial Ordovician Isle la Motte (or Middlebury) limestones over medial Ordovician shaly melange. Locality indicated with an "X" on Fig. 2.
Carbonate exposures such as this one form lenticular belts bounded by medial Ordovician shales and finegrained wackes (flysch) in a zone near this vicinity a few kilometers wide between the western edge of the Taconic Allochthon and the eastern edge of gently east-dipping, unfolded strata that rest with intact unconformable relationship on crystalline Grenville basement (such as those exposed at Stops la and b).
Where contacts are exposed, such as here, and Stops 6 and 9, evidence for faulted lower contacts of limestone over shale are seen. In particular, the underside of the limestone is coated with fibrous vein-type slickensides, the lineation plunging close to down-dip. Truncation of stratification in the limestone is seen locally. An abundance of veins in the limestone within about 50cm of the thrust surface suggests hydrofracturing and high fluid pressures during thrusting. A crude, lenticular cleavage in the underlying shales is deflected adjacent to the fault surface. A small horse of shale, isolated above the main thrust surface by a duplex mechanism , can be seen approximately half way along the exposure of the. thrust (Fig. 3). Towards the western limit of the overlying carbonate sheet a detached sliver of carbonate about a meter long lies in the cleaved shale just below the prominent fault surface. This may be a structurally detached piece or (less likely because of its shape) an olistolith. Similar lozenge-shaped pieces of medium-grained graywacke up to about 1/2 m long occur sparingly in the phacoidally-cleaved shale in the western part of the cut. Slickensided surfaces suggest that they too are products of structural disruption ("structural slicing"), although an olistolithic origin cannot be discounted. The shale and siltstone is locally bedded, with minor folds in part of the outcrop. Most is pervasively disrupted by the phacoidal cleavage whose microstructural character, with abundant evidence for shear offsets, is clearly related to faulting (Bosworth and Vollmer, 1981; Bosworth, 1982, 1984). This carbonate and other exposures like it are shown on the New York State geological map and by Fisher (1985) as giant olistolithic blocks. We find this interpretation of the outcrops to be unconvincing and prefer an interpretation, as shown on Fig. 2, where the carbonates and stratigraphically overlying shales form thin thrust sheets accreted beneath the Taconic Allochthon. Demonstrable tight folds and internal duplex faults within these carbonate sheets account for the many places where stratigraphic continuity is disrupted within them.

STOP 3. Pre- to syn-cleavage thrust
Pre- to syn-cleavage thrust of Poultney Formation over gray slates, above Taconic Frontal Thrust. Locality marked "P" on Fig. 2.
Plude's Quarry (Fig. 4) provides one of the few known exposures of Taconic continental rise rocks lying directly upon the underlying melange/flysch sequence. Several complexities of Taconic thrusting are evident at this stop. Along Carleton Road the shales and graywackes of the Taconic flysch are broken into a melange fabric, that grades up into the quarry with progressively less disruption, until a planar slaty cleavage is found. This is the Taconic Frontal Thrust, and can be mapped as in Fig. 2. Within the quarry a second, earlier fault is present, separating easily identified Lower Poultney slates and thin arenites from an underlying gray slate. The regional slaty cleavage cuts the fault, suggesting that this structure may be of the same generation as Rowley and Kidd's (1982) "Taconic Basal Thrust". 'The gray slates are interpreted to be a unit within the Middle Ordovician Taconic Flysch (allochthonous? parautocththonous?), and hence the fault is inferred to be a thrust. Fig. 4. Exposed pre-slaty cleavage thrust in quarry face (Plude's Quarry, Stop 3; location marked "P" on Fig. 2). Allochthonous Poultney Formation rocks were thrust over gray shales and then folded and cleaved. Thrusting and folding were apparently in part synchronous, as the amplitude of the fold in the thrust surface in the easternmost anticline is less than the amplitude in the folded Poultney. The gray slates most closely resemble a flysch lithology, although whether it is allochthonous or parautochthonous flysch cannot be demonstrated without biostratigraphic control.

STOP 4. Delaware and Hudson Railroad cut
Delaware and Hudson Railroad cut 300m NE of crossing Whitehall-Fairhaven Turnpike. Locality shown with "R" on Fig. 2.
At the east end of the cut (Fig. 5), both sides expose thinly laminated, brown fine-grained arenites in dark slate belonging to the upper Hatch Hill or lowermost Poultney Formations (Cambrian - earliest Ordovician) of the Taconic Allochthon. These are in contact across a steep fault with thicker bedded coarse dolomitic (locally calcareous) quartz arenites and quartzites in black slate of the middle to lower Hatch Hill Formation *(mid-late Cambrian). In the western portion of the exposures, best seen on the northern side, these dark slates, with variable quantities of arenite beds, are in repetitive thrust fault contact with massive greenish micaceous wackes of the (Taconic) Bomoseen Formation (early Cambrian or older). At the western end of the cut, the last exposure contains a fold in Hatch Hill slate and arenites such that bedding surfaces in the slate form the face of the exposure on one limb of the synformal fold. This western end is close to but not quite at the Frontal Thrust seen at Stop 3. On the hill to the north a southward-thinning thrust sheet of shelf limestones occurs between shaly melange below and Taconic rocks above, such as are seen in this cut and at Stop 3. A unit of shaly melange up to a few meters thick occurs between the limestone and the Taconic rocks, and was seen at Stop 3. The western part of this exposure, with the complex slicing and phacoidal cleavage in the black argillite, can be regarded as transitional, in a structural sense, to the melange. The disposition of the Hatch Hill and Bomoseen can be interpreted as an earlier thrust that has been folded and cut by younger, more steeply inclined thrust faults. Fig. 2 shows that the occurrence of a Bomoseen-derived slice immediately above the Taconic Frontal Thrust, followed by a Hatch Hill/Poultney-derived slice, is characteristic of much of the Taconic area bounded by the folded thrust that occurs near the Allochthon boundary in this region. Structures in the railroad cut that we connect with the emplacement of the thrust sheet are fault-related features, particularly slickensides, summarized in Fig. 6. A Riedel and anti-Riedel fault set are interpreted to be present and are consistent with thrust movement towards the west-northwest. We emphasize the brittle nature of this deformation.
* bolded material was inadvertently omitted from the printed copy in the published field guide

STOP 5. Mettawee River Section
Parautochthonous flysch in contact with autochthonous(?) shelf carbonates. Lunch stop; location given in Fig. 7.
The Mettawee River here provides a superb series of exposures that cross from autochthonous(?) shelf carbonates (where we will stop for lunch), through alternating zones of flysch and melange, to a large sliver of Chazyan carbonate, and on into allochthonous Taconic lithologies (Fig. 7). The only area that is poorly exposed in the river is the eastern edge of the carbonate sliver, but mapping demonstrates that this fault contact (the Taconic Frontal Thrust) cuts obliquely across Taconic stratigraphy and large-scale fold axes, and is therefore a post-slaty cleavage generation structure (Figs. 7, 8).
As at Stop 2, some workers are of the opinion that the allochthonous carbonate at this locality (D.W.Fisher, pers. comm.,1983) and along the western edge of the Allochthon in general (J.Rodgers, pers. comm., 1983; Rodgers and Fisher, 1969) is better interpreted as blocks-in-shale (i.e., olistoliths) than as coherent fault slivers. This locality provides an excellent means to test these two hypotheses. The carbonate/melange contact can be walked from point "X" to point "Y" (Fig. 7) with little difficulty (after wading across the Mettawee.... access at "Y" is limited by buckshot). The carbonate is seen to be continuous, essentially unbroken along strike, with internal fold axes approximately parallel to the general contact trend (see Selleck and Bosworth, 1985, Plate 1A). The carbonate must be in the form of a large sheet, or composite sheet, which could be called a single "block". Minor disruption near its margins is undoubtedly present, but the structural style is dominantly detachment of underlying autochthonous shelf rocks and their imbrication at the base of the advancing allochthonous thrust pile. It is misleading to describe the geometry of the large carbonate bodies along the western edge of the Allochthon as "blocks-in-shale", and it is very unlikely that they arose as sedimentary slump features (further discussed in Rowley and Kidd, 1982).

STOP 6. Imbricated carbonates, shales and melange
Imbricated medial Ordovician carbonates, shales and melange just below the Taconic Frontal Thrust. Vermont Route 22A 6.5 km north of Fair Haven. Location shown with arrowhead on Fig. 9. The part of this roadcut to be examined is illustrated in Fig. 9, and consists of the outcrop opposite the parking area and its continuation to the north. A thrust-repeated section of medial Ordovician strata is discernable from medium-bedded limestone (fossiliferous calcarenites to calcisiltites) without shale - Orwell Limestone, passing up abruptly into thin-bedded limestones (micrites) interbedded with dark shale - Glens Falls Limestone, overlain by dark shale, in part melange - here referred to as Hortonville shale (and the melange perhaps as Forbes Hill "conglomerate"). It is important to recognize that the dark shale, in the first instance, is a stratigraphic member of this succession, just as it is in the autochthon to the west (e.g., in the Mohawk Valley). That some of it has been structurally damaged by the imbrication and duplication of the sequence is a secondary effect, reflected in the lenticular (phacoidal) cleavage visible especially in the shale closest to the base of the succeeding limestone. Two of the eight sections lack the basal Orwell Limestone, probably because of local ramping of the active thrust, or original irregularities in the depositional arrangement. It is not valid, in our view, to regard this exposure as "all melange" with blocks of limestone floating in shale. Rather, it is a thrust-imbricated repeated lithic sequence, probably forming a thrust "duplex" above more extensive shaly melange, not containing limestone clasts, that is exposed on the slope to the west of the parking lot and in the separate road cut on 22A about 100 m north of this outcrop. The duplex is below the Frontal Thrust of the Taconic Allochthon which comes to the surface about 50 m east of this road cut; wackes of the Bomoseen Formation of the Allochthon form the prominent topographic feature of "the Great Ledge" visible to the east from the parking lot. More extensive massive limestones (Orwell, and perhaps Middlebury Limestone as well) that form road cuts along 22A just to the south are thought to be larger slices in the duplex zone. Noteworthy in the narrow (less than 1m) zones of shaly melange beneath each slice of limestone in the cut are a few blocks and cobbles of green micaceous arenite identical to the Bomoseen Formation of the Allochthon. The largest of these (approx. 1 m across) occurs at the very northern end of the outcrop, but other smaller ones occur within the outcrop near 30-40 m on the diagram. These we do interpret as olistolithic clasts shed from the front of the Taconic thrust sheet during its motion, and they require that the active thrust outcropped on the sea-floor, at a deep-sea trench-type feature. A similar, but larger (several m across) olistolith of Bomoseen wacke occurs in the outcrop of melange to the north. It is our observation, however, that there is a limit of a few meters to the size of these blocks that are clearly identifiable as olistoliths. Truncated bedding, slickensides and other features characteristic of ramp-flat thrust geometry can be seen in this outcrop. The present attitude inferred for the Taconic Frontal Thrust (about 10° east dip) and the steep east dip of these limestone-shale imbricate slices are consistent with their identification as duplex structures. Their attitude is not consistent with a model of tabular olistolithic slabs lying in the bedding orientation.

STOP 7. Boss Hogg's Quarry
Marked "H" on Fig. 9. Permission must be obtained from the owner to visit this locality.
The quarry exposes part of the early Ordovician Providence Island Formation, mainly dolostones with some limestone, not far below the overlying Middle Ordovician limestones (Middlebury) that outcrop to the east (see Fig. 9). The purpose of this stop is to see the structural condition of carbonates within the areally extensive thrust sheets that exist at this latitude between the Frontal Thrust of the Taconic Allochthon and the autochthonous shelf strata. On the south side of the entrance to the quarry a close synformal fold displays well-developed solution cleavage and marked changes in thickness from the short, west-dipping limb to the long, east-dipping limb due to more homogeneously distributed ductile shape change. A complementary antiform is exposed on the north side of the entrance linked to a synform that trends along the northeast face of the quarry. A wrench fault passing through the quarry entrance must offset the fold hinges in a left-lateral sense. The contrast between the substantial ductile strain shown in this outcrop and the lack of such features at Stop 1b in the autochthon is a reflection of the thrust translation of these carbonates and deformation during active movement on lower thrusts. The cleavage at this stop is roughly parallel with that in Taconic rocks exposed to the east. However, this does not necessarily make the cleavages the same age; evidence exists to suggest that they are not, and that the Taconic rocks were cleaved and folded before emplacement over this portion of the shelf carbonate terrane.

STOP 8. Scotch Hill syncline at Glen Lake.
Permission must be obtained from the owner (in the house across the road). NO HAMMERS ALLOWED. Location shown on Fig. 1.
This outcrop exposes early Ordovician strata of the Poultney Formation, probably about the same age as the carbonates of Stop 7, but a very different facies deposited in deep marine conditions on the continental rise. These rocks consist of green mudrock (slate) alternating with thinner laminated layers of fine sand to silt size arenites and quartzites that are interpreted as contourite deposits, and black/gray mudrock (slate) laminae. The black mudrock layers are probably pelagic; the green are likely mud contourites. The syncline exposed here is the single major hinge of a fold that is in a set with wavelengths of the order of 1 to 3 km and amplitudes of similar amount. The folds are tight to near isoclinal in form. This outcrop does not give the impression that the folds are this tight since the full transition to the fold limb bedding attitudes, particularly on the overturned limb, are not seen in this exposure. This particular fold can be traced north for 3 km and south for 8 km from this place; another single fold in this set in the northern Taconics can be traced for at least 50 km along its axis, characteristic of their subhorizontal to gentle plunges. The overturned nature of this fold, with its moderately east-dipping axial surface and near-axial planar cleavage is also typical of the structure of the low Taconics (Giddings Brook Slice). In detail, small parasitic folds in the quartzites in this outcrop can be seen to be transected by the slaty cleavage, suggesting that buckling of thin layers in response to shortening took place, as is usually the case, before thicker composite layers that generate longer wavelength folds. Thus the cleavage may be axial planar to the large-scale folds but not to the smaller ones. Examples of cleavage refraction can also be seen, and cleavage parallel quartz veins (? post-cleavage) are also present. We emphasize the coherent ductile deformation seen in this outcrop, characteristic of all the western Taconics in the northern part of the Allochthon. In our view it does not support the idea of the emplacement of the Allochthon as a gravity slide of unconsolidated sediments. Comparison of structures here with those in the thrusted carbonates (Stop 7) and at the western edge of the Allochthon (Stop 3) are consistent only with thrust emplacement of coherent, consolidated rock, undergoing related ductile deformation (folding and cleavage formation) at different times in different places during the overall assembly of the thrust sheets.

STOP 9. Shelf carbonate duplex
Shelf carbonate duplex beneath the Taconic Frontal Thrust at Bald Mountain, N.Y. Location given in Figs. 1 and 10.
Bald Mtn. has been a perennial favorite for stops in field guide books of eastern New York, and several excellent descriptions of the locality are available in the older literature (Walcott, 1888; Ruedemann, 1914) More recent discussions can be found in Platt (1960), Sanders, et al. (1961), Zen (1967), Bosworth (1980) and Rowley and Kidd (1982).
We have intentionally placed the Bald Mtn. quarries at the end of our trip, despite their proximity to Saratoga Springs. We have been emphasizing processes related to frontal imbrication, multiple generations of thrusting and the formation of duplexes throughout the day. We feel that the examples we have presented are fairly convincing. Bald Mtn., however, is shrouded with historical overtones, and is also exceedingly complex. The general picture is quite clear: the uppermost portions of the quarries are composed of allochthonous Taconic lithologies, these overly a thin zone of phacoidally cleaved shales, which in turn overly discontinuous masses of shelf carbonate (some quite large) and more phacoidally cleaved shale. But the details are not so clear. Are the carbonate blocks fault slivers, or are they olistoliths within a large-scale sedimentary slump mass, subsequently overridden by the Taconic thrust sheets (Rodgers, 1952; Rodgers and Fisher, 1969)?
We recognize some internal order in the disposition of lithologies in the area of the Bald Mtn. carbonates, with similar lithologies aligned along strike (Fig. 10). Several of the carbonate blocks are probably hundreds of meters in length, not unlike the Chazyan sliver on the Mettawee River (Stop 5). As at Stops 5 and 6, small rounded cobbles of limestone (in this case) within the phacoidally cleaved shale zones may in fact be olistoliths, probably derived at subaqueously emergent fault scarps from the main masses of carbonate themselves (Rowley and Kidd, 1982; Bosworth and Vollmer, 1981). However, we again feel that the structure at Bald Mtn. can reasonably be interpreted as a fault duplex (Fig. 11), as was first proposed by Ruedemann (1932, p. 134). We encourage all participants to share their thoughts with the rest of the group!
A regional compilation of presently identified structures believed to be associated with the Taconic Frontal Thrust System (youngest Taconian deformation) is presented in Fig. 12.

A3: TRI-CORN GEOLOGY THE GEOLOGY, HISTORY, AND ENVIRONMENTAL PROBLEMS OF THE UPPER HUDSON CHAMPLAIN VALLEY
Anson S. Piper
Adirondack Community College
The region of the upper Hudson-Champlain valleys provides an excellent locale for the teaching of introductory geology courses. In addition to the desired examples of geologic phenomena there are ample opportunities to relate geology and human activities past and present and areas where various field methods may be used to solve very simple problems. It is the purpose of this trip to tour the area from Saratoga Battlefield north to Ticonderoga, view points of geologic, historic and environmental interest and to try to relate them one way or another together.

A3: TRI-CORN GEOLOGY THE GEOLOGY, HISTORY, AND ENVIRONMENTAL PROBLEMS OF THE UPPER HUDSON CHAMPLAIN VALLEY

STOP 1. Saratoga National Park Visitors Center
The battles fought here were, collectively, one of the most decisive actions during the course of North American history. They represented the climax of a complex, three-pronged campaign, which, had it succeeded, would have cut the rebelling colonies in two, probably winning the war for the British. The American victory assured recognition by France and subsequently to the alliance.
The choice of ground was made by the Americans, who drew up their lines overlooking a narrow defile along the Hudson. Entrenchments were dug along Bemis Heights under the direction of Col. Kosciusko. The area was sparsely settled, with farms in scattered clearings, connected by wagon roads through the forest. Where the roads traversed sand, they were difficult to move over with heavy loads. Where they traversed clay, they were impossible when wet, and if rutted, nearly the same until beaten down. Burgoyne, with his heavy train of baggage and artillery, was forced to descend the river using batteaus for his supplies while his men trooped along the parallel road. He had crossed to the western side just north of present day Schuylerville (Saratoga). The American defenses, therefore, commanded his route along the river and extended westward to prevent his flanking them.

This is the "280 ft." level of proglacial Lake Quaker Springs.

The "250 ft." level of Lake Coveville.

Coveville Plunge Basin.
Drainage from the Ballston Channel combined with waters of the Kayderosseras dropped into the almost river-like Lake Fort Ann.

Site of Ft. Hardy, Where British grounded arms, is on the flood plain to the right.

Burgoyne's final positions.

STOP 2. Stark's Knob.
Pull off road and park. Hike up road leading west past the knob. THE EXACT OWNERSHIP OF THIS SITE IS, AT THE TIME OF PUBLICATION, UNKNOWN, BUT IT IS NO LONGER THE PROPERTY OF THE STATE OF NEW YORK, HAVING BEEN DEEDED TO THE TOWN OF NORTHUMBERLAND. THE TOWN IS THOUGHT TO HAVE DISPOSED OF IT TO A PRIVATE INDIVIDUAL, WHO DENIES THAT IT IS HIS. AS THE RESULT OF REPEATED INTRUSION ONTO HIS ADJOINING LAND, HE HAS MADE IT KNOWN THAT HE WILL HAVE ALL PERSONS WHO STRAY ON TO HIS PROPERTY ARRESTED.
IT IS THEREFORE IMPORTANT THAT VISITORS STAY ON THE TWO ACCESS PATHS TO THE SITE AND AVOID CROSSING THE OLD FENCE LINES.
The Knob is named for General Stark. who placed his artillery atop of it in the final days of the campaign, thus blocking the withdrawal of the British up the Hudson River and along its western bank. The knob has been formed by the differential erosion of the soft black shale from around the more resistant basalt of the pillow lava. Both the shale and the pillow lava are part of an overthrust block of Ordovician rock displaced a considerable distance from the east during the Taconic events.
The material between the pillows contains fragments of the carbonates through which the lava appears to have passed on the way to the surface. The pillows themselves, have a chilled surface and are laced with quartz and calcite filled fractures. Several small faults cut down through the quarry face and water moving along these has formed a small spring at the base near the large pine tree. The basalt was quarried for "road metal" prior to its acquistition by the state.

Fort Miller
The fort was built on the opposite side of the river, to protect the portage around rapids or a small falls on the river. It was a wood stockaded "star fort".

The old Champlain Canal on the right.
This old canal wanders along, following the contours in order to reduce the number of locks. Rt. 4 crosses its path.

Exposure of black shale and sandstone in a near vertical attitude.
A few graptolites have been collected here dating it as part of the Taconic over-thrust.

Bridge over the Champlain Canal.
The Hudson River is seen below the locks. This water barrier was nonexistent during the 18th century so that it was easier to build the military road down this side of the river.

The Fort House Museum
(Time permitting, a brief stop.) This house was built prior to the revolution of materials said to have been scavenged from the buildings at the fort. There is an old, but never-the-less good, model of Fort Edward - a typical earth and timber fort.

Bridge over Fort Edward Creek with an old canal aqueduct over it to the right.

Site of Fort Edward
All that remains of this, the largest British military installation in North America prior to 1800, is a small portion of the moat. It was essentially a three bastioned earth and timber fort, built over a period of two years on the site of earlier Fort Nickolson. Additional works were built on "Roger's Island" the home base of Roger's Rangers. The fort was never besieged or defended except against small raiding parties. It was placed here at a position of great strategic importance, but like Ticonderoga, it was overlooked by high ground making it indefensible. Seven blockhouses were placed around it to cover the weaknesses in its approaches. This point is the furthest extent of the navigable waters of the Hudson and the southern end of the portages to Lakes George and Champlain.

This canal was completely plugged following the removal of the power dam.

STOP 3. Roger's Island
In the early 1970's, the Niagara-Mohawk Power Corp. received clearance to remove a small power dam located just north of the island. The volume of sediment entrapped behind the dam was greatly underestimated and the P.C.B. content was not recognized as a hazard and ignored. When the spring flood occurred, a huge volume of P.C.B. laden sediment washed down stream, leaving the north channel plugged and the south channel nearly so. This resulted in three major problems: the navigational channels were plugged here and downstream, P.C.B 's entrapped in the sediment were distributed with them and raw sewage from the Village of Fort Edward was piled up atop of the plugged channel.
The New York State Department of Transportation dredged out the channels and stored the material at the DOT sites on Roger's Island and on the Town of Moreau side of the river. It was an annual event for several years until the bulk of the sediment was washed out and the nature of the P.C.B. problem "surfaced". During the last dredging, the P.C.B. threat, having been recognized, workers were required to wear dust masks and the material was encapsulated, the previous dumpsites were covered with a temporary cap of clay. An unexcavated archeological site was buried in the, process.

STOP 4. D.O.T. Site
This is an encapsulated dump site for the P.C.B. laden sediments dredged from the Hudson River at Roger's Island. The debris was placed in a clay lined pit and then covered again with clay. It is a temporary disposal site.

Marker on left for the McCrae House
After making turn note marker on left for the McCrae House where Jane McCrae was taken by Indians. Rt. 4 approximately follows the military road to Lakes George and Champlain.

The approximate site of the killing of Jane McCrae.
A blockhouse was situated about where the school athletic field is. The road is climbing up onto the sand delta deposited into Lake Coveville.

STOP 5. Fort Edward General Electric Plant & Union Cemetery
This is one of two General Electric plants locally which manufacture electrical components (capacitors chiefly) previously using P.C.B.'s. To the right rear, next to the Grand Union Store, is an Agway Farm Store, which sells pesticides and herbicides to local farmers. Union Cemetery, located to right, is the burial place of several persons of note, including Jane McCrae, Duncan Campbell and Tobert Cochran.
The location is atop a sand delta (Lake Coveville) some 15 to 20 feet thick overlying a shale which crests under the General Electric Plant and slopes away toward the river to the southwest and the Champlain Canal to the northeast.
Two groundwater problems have developed here, the first involving agricultural chemicals and the second, P.C.B.'s and T.C.E.. Most of the local dwellings have their own waterwells, some of which have become polluted by either or both types of chemicals. The pesticides and herbicides have shown up in wells on Putnam Avenue and Ethan Allen Street southeast of the Agway Store and extend as far as Burgoyne Avenue. The seemingly harmless act of washing trucks appears to have been the cause of this problem. One more good example of why ordinary people need a better education in geology. The P.C.B. - T.C.E. problem is more complex. Both chemicals were uses extensively at the General Electric Plant and the deliberate and accidental spills over many years have gradually polluted the groundwater about the buildings. In addition, some individuals have dumped the industrial chemicals at their homes where they have been salvaging materials or using T.C.E. on their own projects. Wells along adjoining streets have been abandoned and these homes have been connected to municipal water systems, the cost being borne by G.E. There is very extensive litigation involved in these cases and little information can be gained from the parties involved.

Ciba-Geigy Plant and wastewater treatment plant.
Prior to the construction of the treatment plant, waste water containing heavy metals was discharged into the Hudson adding to the pollution from the paper mills upstream. Following the imposition of environmental controls, this installation was built to separate the toxic components from the water which is returned to the river cleaner (supposedly) than when it is taken out. The solids are then hauled to the Queensbury Landfill where they are placed in a disposal basin.
The road climbs up onto another sand deposit, this one is probably related to Lake Quaker Springs.
Across the river to your rear, is the Glens Falls Cement Quarry showing the thickness of the sand overlying the carbonates. The cement plant was the center of an air pollution study done by Adirondack Community College students many years ago. The study pinpointed the plant as a major source of particulate matter in the air and with the passage of clean air regulations, the old stack was replaced with one containing "scrubbers" and the problem was essentially solved. The Glens Falls Limestone quarried here was previously produced from tunnels underlying the Village of South Glens Falls.

Dix Avenue is following the route of the old military road to Lake George.
It skirted the low area through which we have just passed, and swung west and then north to avoid the swamp through which Quaker Road passes.

Prospective Peat Farm
Peat deposits have formed in swamps which developed on Lake Albany clay which sealed the underlying limestone. The development is stalled pending a decision related to the Wetlands Protection Act.

You are now entering "New France"
You are now entering "New France" as you cross Halfway Brook and enter the St. Lawrence drainage basin.

Brief Pause - Adirondack Community College Quarry.
This exposure of Ordovician, Beekmantown Carbonates, contains a breccia, (fault or collapse ?) some small cephalopods and burrows of a sort. The campus is located on a downfaulted block (a graben) with a fault running approximately across Bay Road and another somewhere between the rear of the buildings and the next ridge to the east. Other structures are suspected because of the change in the attitude of the rocks in the several outcrops on campus. A small fault with a 2 inch displacement has been found. In addition, there is an exposure with enlarged solution joints, perhaps formed during the post-glacial interval while Lake Albany was draining. The soils on campus are lake clays (some varves were found in the building excavations) and to the west and north, is the kame and esker complex.

The road climbs up onto the kame and esker complex.
Blind Rock was a locality where native war parties often took prisoners for torture.

Round Pond and Paradise Beach.
A kettle lake with an esker on each side at the far end. The one extending along the north side continues along the right side of the road.

This is near the epicenter of a number of very small quakes
This is near the epicenter of a number of very small 'quakes (.5 Richter or less) which were detected during a study done by the N.Y.S.G.S. Rt. 9 passes over 5 Mile Run, the site of several ambuscades, just in front of the Great Escape Amusement Park! The low area on the right, past the park is an extension of Glen Lake, an iceblock lake .

Kame terrace capped by Lake Albany sands.

STOP 6. Col. William's Ambush
PARK ALONG ROAD SIDES WHERE IT IS SAFE. THIS IS A DANGEROUS SITE.
The outcrop is on the west side of the road and is extremely hazardous because of traffic. The bedrock is Precambrian (Grenville) Gneiss and is cut by several nearly strike-slip faults running parallel to the road. At one point a small dike is cut into three sections by the faulting. Prior to the widening of the road, there was a fine, fluted, slickensided surface exposed. French Mt. opposite, is a horst.
The military road passed below the present road and this was the site of the French ambuscade of the Provincials and Iroquois, known as "The Bloody Morning Scout". Col. Ephraim Williams, whose estate founded Williams College, was killed standing on a glacial boulder, while old "King" Hendrick toppled from his horse and was bayoneted. The colonials and Mohawks successfully withdrew from "Rocky Gulch" to Lake George, leaving about 100 casulties behind.

Bloody Pond, a kettle lake and the scene of two skirmishes.

STOP 7. Fort George And Battlefield
Here is another exposure of Ordovician, Beekmantown carbonates, dipping about 5° northeast and lying between two mountains of precambrian rock. This presents an opportunity for solving a very simple structural problem Three responses are usually evoked from beginning students when asked to explain it:
1. The rocks were derived from the older rocks and deposited here.
2. They were downfolded into the valley form.
3. They were downfaulted.
The first choice is eliminated by the character of the sediment, and the others require further information to be gained at the next stop.
The carbonates were first used to build the stone bastion of Fort George, which was built following the Battle of Lake George. The rocks provided both the building stones and the mortar to hold them in place. The present structure has been partially restored.
The battle here followed the Bloody Morning Scout, Dieskau, the French commander launched a series of assaults on Johnson's camp and was repulsed with heavy losses. Both officers were wounded and Dieskau taken prisoner. The French and their allies fled to Bloody Pond to loot the packs of the men killed there earlier, where a relief column of over 600 men from Fort Edward caught them disorganized and scattered the survivors.
After the battle, Fort William Henry was finished on the sand terrace overlooking the lake. The fort was built of timbercribs filled with sand from the moat. The main gate was on the south side, and a stockaded area on the north. The choice was poor in the sense that the sand, being easy to dig, allowed Montcalm to advance his saps and parallels very quickly when he laid seige two years later in 1757. His artillery quickly reduced one bastion. The sand pouring out through broken timbers caused it to collapse and the fort surrendered. The attack on the unarmed British prisoners following the surrender is a matter of historic record.

STOP 8. Exposure of the upper Cambrian Ticonderoga Formation
This exposure of the upper Cambrian Ticonderoga Formation dips gently toward the northeast and consists of mostly sandstone which places it in the upper third of the formation but not at the top which contains some chert. There are ripples and stromatolites present, the latter being in the reddish-brown dolomitic layer at the top of the ledge. The upper surface has been planed smooth by glaciation and the direction of movement has been recorded in striations found there. Visible to the west is an exposure of precambrian rock at the bend in the road. These observations tend to support the hypothesis that the valley floor is a downfaulted block or graben. Further support to the idea comes from the existence of two magnetic anomalies between the two outcrops. (Personal communication from John Mead) A similar relationship between the Precambrian and the carbonates can be seen along the east side of the valley. (Along Rt. 9-L near Crosbyside)

The road follows the trace of the English Brook Fault.

Brief Pause - The English Brook Saprolith
Note: This exposure of deeply weathered rock has been known since the 1930's and has miraculously survived repeated road improvements. Originally, the exposure was topped with two layers of glacial boulders separated by a lake sand. Each spring these came rolling down - some three feet in diameter - to the dismay of the highway department. Their recent removal and the gradual covering of the face in its own debris has greatly altered the appearance of the site. The preservation of the saprolith is thought to be the result of deep weathering along the plane of the fault and the transverse orientation of the fault to the direction of ice movement. This is one of the few such exposures which can be easily seen in New York State.

Note en route: This valley was occupied by Glacial Lake Warrensburg
Note en route: This valley was occupied by Glacial Lake Warrensburg, evidence for which is seen in the numerous sand deposits along its floor. Just short of Milepost 63, the road cuts show precambrian rocks on one side and layered sediments on the other, the road straddling a fault.

Roger's Rock State Park And Campsite.
Named for Roger's Slide thought to be the fault scarp forming the east side of the Lake George graben and the scene of Major Roger's escape from the French and Indians, March 13, 1758.

Ticonderoga Creek - The outlet from Lake George flowing into Champlain

STOP 9. Fort Ticonderoga (Carillon)
This fort is built near if not on the site of Champlain's skirmish with the Iroquois in 1609. Construction was started in 1755 and essentially completed by 1758. Modifications, repairs and improvements continued until the end of the American Revolution, when it was allowed to fall into total disrepair.
The original construction was of earth and timber, later on improved by stone facints. The fort was designed for a small permanent garrison with extensive outworks for a larger "summer" army. The location was poorly chosen, since the works are well within range of seige guns placed on the heights of Mt. Defiance.
The stone fort was built from Ordovician limestone, quarried on the site, and was in total ruin prior to reconstruction. The stone work, weakened by solution and frost action, had collapsed into the moat, and hauled off to build "celler walls" by the post war settlers. The original foundations can be recognized in the walls by their weathered appearance.
Mt. Independence, on the opposite shore, was linked to the fort by a bridge consisting of 22 sunken piers connected by 12' X 50' "pontoons" chained together. The piers still survive in the muddy floor of the lake and are currently being salvaged (?) along with numerous other artifacts of the Revolutionary War.

South Bay, Lake Champlain

Note Rock Falls along road cuts .

STOP 10. The Hudson-Champlain Canal
The canal follows the general path of wood creek which rises near Fort Edward. During the spring of 1984 this area was badly flooded when water backed up behind a coffer dam following a heavy rain. The dam, installed to permit repairs on the canal, was not designed to accommodate the sudden rise of waters and considerable damage was done to the small museum here and other structures.
Historically, the locality was called Skenesborough, after Philip Skene, a prominent Tory. The claim to be the "birthplace of the United States Navy", stems from the fact that Benedict Arnold's fleet was built here, the first continental squadron. Although it was defeated at Valcour Island, the fleet delayed the Burgoyne campaign until the next year. The hull on display here is a survivor of the Battle of Plattsburg Bay, during the War of 1812. A military road was built from here to Fort Edward and later improved by Burgoyne.

This road will follow closely the old military road parallel to Wood Creek.
It travels over the floor of Lake Fort Ann.

Lake Clays On Right - Note Slumping
Champlain Canal Locks on left.

Note: Rockfalls In Road Cut.

Brief Pause - Road Cut In Precambrian Gneiss.
The foliation and some joints in the gneiss dip toward the east so that the road cut intersects or "daylights" them along the west side of the road. In order to reduce the chance of failure along these planes, the threatening blocks have been bolted into place with heavy threaded rods which penetrate into "solid" bedrock.

STOP 11. Unconformity
The base of the Potsdam Sandstone is exposed here in contact with the precambrian gneiss. The basal conglomerate above the unconformity contains many large quartz pebbles here. Additional exposures of the Potsdam may be found by walking down the side road to the left and just past the small valley, climb down over some old concrete slabs to a flat exposure. Graded bedding, crossbedding and ripples can be found here and in the railroad cut. Glacial striations, chatter marks and quarrying faces may also be seen. A commercial building stone quarry across the canal was previously operated and many local houses are built of this rock.

Battle Mt.
A rear guard action was fought here by the Americans fleeing Burgoyne's army. This was one of the first times that the "Stars and Stripes" were flown in battle.

Entering Fort Ann Village
The reconstructed blockhouse (bank) was originally intended for a museum. It is fairly accurately constructed and very close to the actual site of the fort which guarded the crossing of Halfway Brook where it entered Wood Creek. There was a stockade surrounding the blockhouse. Note the use of Potsdam sandstone in several of the older buildings.

Possible route for Burgoyne
Burgoyne's line of march probably followed Route 4, but it is also possible that he did follow this lower route.

Smith's Basin.
On the far side of the canal is an excellent section of Cambrian and Ordovician carbonates described by Donald Fisher in the N.E.I.G.C. Guidebook 61st mtg. 1969. An old limestone quarry and kiln was operated just across the bridge in an exotic block or thrust slice of Orwell and Glens Falls limestone. The basin was an old canal basin and at one time was a fairly large settlement.

Kingsbury Landfill (Closed)
Note also, the Feeder Canal, five "combines" Locks and small house at right of intersection beyond canal.
The Kingsbury Landfill is now probably the chief source of P.C.B.'s entering the Hudson River. Many capacitors were disposed of here and on summer days, their sweet odor can be detected. The P.C.B.'s are leaching out of the site, into the canal and into the Hudson River. Another path is into the groundwater and the lowlands below the site to the river. Current plans call for the capping of the site hopefully sealing it. General Electric has made a major contribution toward the cost, but the remainder must be borne by the local taxpayers.
The feeder canal served two purposes: to move barges to Hudson Falls and Glens Falls and to maintain the water level of the lower section of the canal.
The small house may have been Burgoyne's Headquarters when his army camped here. In any event, it is thought to be one of only two buildings not burned down during Carleton's Raid in 1780.

This is Baker's Falls, the highest falls on the Hudson.
While it is capped by a dam to increase its generating capacity, it is probably due to a fault. The river has cut a deep gorge through the softer shales below the falls.
It was the presence of this falls which caused Fort Edward to be built and the settlement of "Sandy Hill" to develop into the Village of Hudson Falls. The falls and dams upstream provided the water power for the early mills and later the hydroelectric generating plants, ultimately leading to the locating of the General Electric plants and the P.C.B. problem. It was also found that some P.C.B. was used to produce carbon paper upstream at a paper mill.

Caputo Dumpsite.
This site which is located along the right side of the road, in back of the houses was used to dispose of industrial wastes from the General Electric Company from about 1958 to 1970. It was an open pit into which barrels were placed, filled with waste, P.C.B.'s and T.C.E. The subsurface consists of glacial sands and lake clays overlying bedrock. The watertable is about 25 feet down. ENCON. well information indicates the following:
0 - 70 feet Medium to fine sand
70 - 95 feet Fine to very fine sand with silt lenses 1/8 to 1/2 " thick.
95 - 100 feet Fine sand - clay lenses with brown varves
100 feet + Gray clay and silt lenses over bedrock.
The site has been enclosed by 1600' slurry wall 100 feet deep and three feet thick in an attempt to contain the leakage. The slurry consists of 70% soil, 28% native clay and 2% bentonite. The whole is capped to shed water. The P.C.B.'s appear to be more or less contained and saturate the soil above the watertable. The T.C.E.'s on the other-hand appear to have sunk down rapidly to about 70 feet. A plume has formed between 45 and 70 feet, spread out about one mile down gradient in 2-2.5 years. The water at the watertable appears clean as does the water below 70 feet, thus the plume appears to be moving toward the southeast in a sheet about 25 feet thick at a present rate of eight feet per day.
Many residential waterwells have already been polluted and some properties in close proximity are claiming unsafe levels of vapors within the structures. Because of pending litigation, it is difficult to obtain specific and valid information from some parties. The plume which is moving toward the Fort Edward water supply has shown up in a stream feeding it. A system of aeriating the water has been installed which allows the T.C.E. to dissipate. Additional P.C.B.'s were sprayed along the Fort Edward road to settle dust and this has recently been removed by scooping up the contaminated soil and placing it at the Caputo Site where it is to be encapsulated.

A4: THE MINERALOGY OF SARATOGA COUNTY, NEW YORK
JOHN J. THOMAS AND JENNIFER A. RICHARDS
Skidmore College
Saratoga Springs, NY 12866
Saratoga County includes within its boundaries the Adirondack Highlands and the Hudson and Mohawk Lowlands. The rock types range from the Precambrian Grenvillian granulites of the Adirondacks, located in the northwest quadrant of the county, through Cambro-Ordovician carbonate and clastic rocks. While the area is predominantly covered by Pleistocene glacial till and sediments of glacial Lake Albany, scattered bedrock exposures afford excellent mineral collecting.
Several of the county's most famous mineral collecting localities are either closed to the public or have been lost. An example of the former is the Gailor Quarry in Saratoga Springs. While the quarry is inactive, the faces have become very unstable and because of collector abuses, the owners no longer allow access. An example of a lost locality is the collection site for chrysoberyl, for which Saratoga County is famous.
The original description of the quarry measures its location from Route 9. Since the publication of the location, routes have been renumbered and relocated.
All of the localities that are listed in this guidebook are on private property and require special permission from the landowner to visit.
PURPOSE
The purpose of this field trip is to examine a variety of mining and mineral localities in Saratoga County that are typical of this area and the Southeast Adirondacks in general. The minerals available in large quantity are fairly common, but interesting in terms of size and development. The quarries visited will include a graphite mine and several pegmatites. Opportunities exist to collect a variety of minerals, observe the relationships between them, to study the mines' relationships with the country rock, and to see late 19th and early 20th century mining techniques.

A4: THE MINERALOGY OF SARATOGA COUNTY, NEW YORK

STOP 1. Wilton Graphite Mine
The graphite mine is located to the west of US Route 9. Enter the woods directly opposite Worth Road. There you will find a dirt road leading up the side of the mountain. The following measurements are taken starting from the west edge of US 9. All measurements are in feet.
467 | The foundation of a former building on the left.
1533 | On the right is the foundation of the boarding house for the mine.
1756 | On the left is the foundation for the loading bins. Horse teams took the refined graphite from here to the railroad.
1890 | On the left is the waste water dam and settling pond, even then a matter of controversy. Each year the pond was allowed to flush itself out into the fields below. If you follow the stream valley 1,000 feet upstream, on the right you will find the foundations of the concentrating plant which originally consisted of five levels. The original turbines are still here. There was also a steam generating plant here that supplied power for the mill and mine.
2725 | Stream crossing. Foundations on the left are for the upper level of the mill. A narrow guage railroad serviced the mine from here.
2840 | A fork in the road, take the road to the right.
2935 | The cut on the right and left was a drainage ditch for the underground mine and connects with it.
2890 | The entrance to the underground mine, known as the mine, on the left.
3411 | Follow the main road
3591 | Another drainage ditch.
3833 | The trail from the Wilton-Greenfield Road enters on the right.
3982 | On the left is the large open mine, known as the quarry. Water fills the west end.
4326 | The road is now a trail. The end of the quarry.
The following description is taken from the Adirondack Graphite Deposits by H. L. Alling (1917).
The property was first opened about 1910 by the Saratoga Graphite Company which worked it in a small way for two years. After a few years the mine was taken over by the Graphite Products Corporation which enlarged the plant and the mine and worked it until about 1922.
The original mine is 22 by 30 meters and was worked only by the Saratoga Graphite Company. The Graphite Products workings consist of the mine and the quarry. The mine extends 115 meters along strike, inclines 38-42 degrees south. A number of openings have been driven down dip meeting two parallel horizontal drifts. The quarry is an open pit mine extending eastwest, 125 by 30 meters. Now water filled, in 1917 it was 10 meters deep.
The rock containing the graphite is described as a quartz schist and occurs in two outcrops, the mine and the quarry, repeated by faulting. From Alling (1917, p. 106) describing a south to north section (fig. 1), " ... a serpentinous limestone forms the bed of the brook .. , next rock to the north is a para-amphibolite grading into the quartzite ... injected and saturated by Laurentian Granite a lenticular mass of metagabbro ... a siliceous limestone ... beneath the limestone the graphite schist shot through with 'pegamatitic material which forms knots and stringers' a fault parallel to bedding occurs here ... a gap in the cross section Pegamatite, quartzite, and metagabbro ... a reddish garnetiferous quartzfeldspar para-gneiss ... The rocks here are faulted and penetrated by pegmatite ... It is not possible to name with certainly the rock forming the floor of the quarry ... The north end of the section ends in a limestone." The section as described correlates with the Spring Hill Pond Formation of the southeast Adirondacks. A diabase dike 10 meters wide outcrops just west of the mine. A second dike, 25 cm. wide, outcrops west of the finishing mill.
The ore is similar to the American, Hague, Flake and Hooper ores. Graphite content is 7-8% all flakes are less than a millimeter in diameter. The outcrop is badly weathered, but at the bottom of the inclines in the mine is in better condition.
The mining technique was primitive by any standard consisting of steam drilling, hauling the ore out of the mines with donkey engines, and loading it into wagons. Teams hauled the ore to the narrow gauge mine cars which took it directly to the concentration mill. The usual Adirondack'milling practice of crushing, stamping, buddling, screening and drying was used. The finishing mill used Hooper pneumatic jigs which prepared the graphite for market.
Minerals and Rocks: Apatite; Diabase; Graphite; Pegmatite; Phlogopite; Quartz schist

STOP 2. Black Pond Pegmatite
The Black Pond Pegmatites, unreported in the literature, were mined in the early twentieth century for abrasives used in Bon Ami Cleanser. The description of these bodies is taken from a 1984 field report by Tara Mandeville of Skidmore College.
Black Pond is one mile down the logging road from its intersection with Lincoln Mountain Road. The pegmatites are hard to spot from this direction. Directions for finding the bodies follows, the distances are in feet:
3450 - First sign of crushed pegmatite in the road.
4015 - Pegmatite (Ml) on the west side of the road.
4150 - Road on the west goes to the big pit (M2).
4365 - Pit on the west side of the road (M4).
4590 - Side road to the east (M6).
5110 - Black Pond.
As one approaches the outcrops from Lincoln Mountain Road (fig. 2), the first evidence of the outcrops is a tailings pile (Ti) adjacent to a small mine pit, Ml (approximately 4.6 m. long by 4.6 m. wide by 2.4 m. deep). The tailings are composed of feldspar, quartz and biotite. The pit contains several small pegmatites varying from pure feldspar to quartz-rich pegmatite with large crystals of biotite. The country rock is a biotite-quartz-feldspar gneiss.
The largest pit in the area (M2) is 30 m. x 12 m. x 9 m and is partially water filled. The coarse grainedfeldspar-quartz-biotite pegmatite is discordant to the 280,35W striking, medium grained, biotite-quartz-feldspar gneiss country rock.
Pit #3 (M3), 6 m. x 6 m. x 3 m., contains several smaller pegmatites that are partially concordant and rich in quartz. The surrounding fine to coarse grained gneiss contains abundant biotite. The adjacent tailings pile (T2) includes feldspar and rose and smokey quartz, but little biotite.
A very large tailings pile (T3) lies just south of Mine #3 and is probably the tailings from Mine #2. The tailings are dominantly country rock with some pegmatite. Large crystals of tourmaline were found in this dump.
Further south along the logging road a small overgrown trail enters from the east. Opposite this trail is Pit M4. This is a small quartz-feldspar pegmatite interrupted by a small lens of biotite-rich gneiss. At the entrance to the path is a small tailings pile (T4). Further up the path is a feldspar, quartz, biotite pegmatite mine (Ms) 6 m. x 9 m. x 6 m.
South along the main logging road toward Black Pond, a side road enters from the east. Along this road are feldspar-rich tailings (T5), several test pits containing quartzite (Q), and Mine #6 (6 x 3 x 2 m.) which is another feldspar, quartz, biotite pegmatite.
Along the northwest corner of Black Pond is the last of the pegmatites (M7). Here is a small discordant pegmatite in a gneiss which contains coarse grained feldspar and finer grained quartz and biotite. The tailings (T6) associated with this mine contain feldspar, rose and smokey quartz and biotite.
Minerals and Rocks: Rose quartz; Smokey quartz; Tourmaline; Biotite; Rose quartz graphic granite; K-feldspar; Graphic granite; Granitic gneiss

STOP 3. Mount Anthony West Pegmatite
The following description is taken from Geology of the Luzerne Quadrangle by W. J. Miller (1923). The pegmatite has not been described in detail, but is referred to several times.
Miller (1923) describes west of Mounth Anthony a terrane of metagabbro-granite rocks where many small pegmatites without sharp borders cut across the foliation. Magnetite, in amounts to be classed as ores, in 1923, is observed associated with granite, pegmatite, and metagabbro. This stop has been selected for this magnetite-pegmatite association. The magnetite is always in moderately coarse grained, gray pegmatite in masses up to 2 or more centimeters across. The country rock is a garnetiferous Grenville gneiss or amphibolite. Mines in this area were worked 90-100 years ago and some ore was shipped. Also, attempts were made to use the white feldspar in the pegmatites.
Minerals and Rocks: Pegmatite; Magnetite; Country rock

STOP 4. Overlook Quarry
The following map (fig. 3) and description are taken from Tan (1966). Miller (1923) describes the Overlook Quarry as producing pottery feldspar as late as 1920. pegmatites.
The country rocks are granitic gneiss and magnetite-bearing metagabbro. pegmatites.
The border and wall zone (I) is in sharp contact with the country rock. The border zone is difficult to distinguish from the wall zone. The border zone is fine grained in places. A lense rich in andesine which occurs at the west margin of the ore body is interpreted by Tan to represent an incompletely developed border zone, although a segregation (replacement) origin is possible. In the border and wall zone, both pink and white potassium feldspars are found and a coarse graphic texture is common. Associated biotite plates are more than 1 m. in diameter. pegmatites.
The intermediate zone (II) is mainly white potassium feldspar crystals up to 1 m. across, with subordinate amounts of quartz, plagioclase, and large black tourmaline crystals which reach lengths of 15 cm. or more. pegmatites.
The core zone (III) is rose quartz and crosscuts the intermediate zone (II). pegmatites.
Minerals and Rocks: Albite; Allanite; Magnetite; Manganoaptite; Oligoclase; Orthoclase; Rose quartz; Smokey quartz; Thorite; Tourmaline; Zircon (Cyrtolite); Graphic Granite; Andesine; Biotite; Microcline; Monazite; Plagioclase; Polyclase; Quartz var.; Sericite; Uranite; Uranothorite; Manganoan-flourapatite; Country rock

STOP 5. Batchellerville Quarry
The following description is taken from Tan (1966). The Batchellerville deposits can be reached by a logging road at the rear of the mobile home park east of Saratoga County Route 7. The outcrops consist of two pegmatite bodies (fig. 4) reported by Newland and Hartnagel (1939) and six more bodies found by Tan (1966).
The bodies were worked by the Claspka Mining Company in 1906 and were still mined in 1916 and 1921. Mining was for microcline for the ceramic industry. Most of the pits show only wall rock with the central productive portions, the pegmatite, having been removed. The small size of the mining pits indicates that the production was never great. The deposits are famous for having yielded the largest beryl reported in the state, 69 cm. long and 25 cm. in diameter. The muscovite contains too many iron inclusions for electrical uses.
In the lower pit, the contact between the pegmatite body and the wall is sharp. On the south wall the pegmatite body lies in a gently folded anticline plunging 30 degrees toward the south. Biotite, uraninite, pink and pale green apatite, and bladed allanite are found along the vertical northwest wall of the pit. In the wall zone (III), scrap muscovite (about 1/4 to 1 cm. in width) appears. White graphic potassium feldspar with parallel short quartz rods is exposed in the south wall. The biotite is partly chloritized. Subhedral high-temperature quartz is intergrown with muscovite. Pyrite and low-temperature quartz crystals, with prism faces, are found in small vugs about an inch across. The intermediate zone (III) consists of giant white microcline about 1 m. long, muscovite columns, and small amount of quartz. The quartz core (IV) near its upper margin contains columnar muscovite crystals with lengths of 15 to 25 cm. Veinlets of quartz extend outward from the core and invade the microcline, but no sign of argillization or sericitization is observed.

A5: CORRELATION OF PUNCTUATED AGGRADATIONAL CYCLES, HELDERBERG GROUP, BETWEEN SCHOHARIE AND THACHER PARK
PETER W. GOODWIN, E.J. ANDERSON, LAWRENCE J. SARAKA, WILLIAM M. GOODMAN
Temple University
The purpose of this trip is to instruct participants in the field application of the PAC Hypothesis. Specific objectives include:
1. demonstration of criteria for recognition of PACs in shallow - water carbonate facies of the Manlius Formation;
2. construction of a PAC column by participants at Schoharie N.Y. in the Manlius Formation;
3. observation and evaluation of the stratigraphic section of the Manlius Formation at Thacher Park from an episodic perspective and comparison of those observations to a PAC column constructed by the trip leaders and
4. discussion of the methods, problems and implications of correlation of Manlius PACs between the Thacher Park and Schoharie sections.

A5: CORRELATION OF PUNCTUATED AGGRADATIONAL CYCLES, HELDERBERG GROUP, BETWEEN SCHOHARIE AND THACHER PARK

Large road cut in lower Helderberg Group (STOP 1) on south side of 1-88.

Road cuts in Kalkberg, New Scotland and Becraft fms
Small road cut in Kalkberg Formation on north side of 1-88; large road cut on south side in New Scotland and Becraft Formations.

Small road cut on south side of 1-88 in upper Becraft Oriskany and Esopus Formations.

STOP 1. Brayman, Rondout Manlius and Coeymans Formations
The Cobleskill-Rondout-Manlius interval (85-feet thick) is completely divisible into 13 PACs (fig. 4). The 5 Cobleskill-Rondout PACs comprise a sequence of peritidal cycles initiated and ended by large punctuation events (see water-depth curve). The first of these events followed a sea-level fall which produced the unconformity with the Brayman Shale. After the deposition of 5 PACs, a second large event terminated tidal-flat deposition and initiated a sequence of basically subtidal PACs in the lower Thacher Member of the Manlius Formation. Thus each of these major punctuation events is marked by the introduction of significantly different facies.
Within the sequence of 8 Manlius PACs the boundary between PAC 5 and PAC 6 is unique. At this boundary the upper part of PAC 5 is marked by a laminated cryptalgal crust on a scalloped surface, features which suggest subaerial exposure and erosion resulting from a minor sea-level fall. This surface is a widespread marker horizon traceable throughout the Hudson Valley. The subsequent sea-level rise created water depths sufficient to produce the subtidal bioturbated stromatoporoid-bearing limestones of PAC 6. Another significant punctuation event resulted in even greater water depth and the diversely fossiliferous subtidal facies of PAC 7. PAC 8 is like 7 but is truncated by an unconformity.
The Manlius-Coeymans boundary is a surface with a complex history. At Schoharie, at the top of Manlius PAC 8 (fig. 4), it appears to be a normal PAC boundary marking a major punctuation event which introduced facies very different from Manlius facies below. However, correlation of PACs to the east and south indicate progressive erosion and elimination of PAC 8, 7 and 6 in the Hudson Valley as a result of differential uplift. This erosional surface was then inundated by a sea-level rise which initiated Coeymans deposition throughout the area.
Thus the Cobleskill-Rondout-Manlius interval at Schoharie represents episodic stratigraphic accumulation in response to a complex history of small-scale sea-level fluctuations including 3 sea-level falls and 14 sea-level rises. That each of these events is trUly allogenic and probably eustatic is suggested by correlating each PAC and PAC boundary between Schoharie and Thacher Park (fig. 5).

Quarry in the ManliusCoeymans interval
Quarry in the ManliusCoeymans interval on the south side of road (Rickard Locality 67).

STOP 2. Indian Ladder Staircase, John B. Thacher State Park.
At this locality the Rondout-Manlius-interval consists of 9 PACs, 2 in the Rondout and 7 in the Manlius (fig. 5). The smaller number of Roundout PACs relative to Stop 1 reflects the episodic overstepping of the land mass which was topographically higher at Thacher Park than at Schoharie. Manlius PAC 8 at Thacher Park is absent as a result of pre-Coeymans erosion. Correlation of PACs between the two localities was accomplished by matching unique facies and major facies changes produced by punctuation events. When the columns are correlated by these methods, the number of PACs between major punctuation events is the same at each locality.
Within the Manlius Formation PACs generally consist of facies representing more restricted paleoenvironments than those at Schoharie. For example, PACs 3 and 5 at Thacher Park are capped by a significant thickness of cryptalgal laminites representing aggradation to sea-level. At Schoharie PACs 3 and 5 are capped by shallow subtidal facies reflecting the presence of persistently deeper and less restricted environments at this locality.
Patterns of punctuation events are similar at both localities as interpreted by comparision of facies changes at PAC boundaries. For example a major punctuation event introduced Manlius facies (PAC 1) at both localities; major events also produced marked facies changes at the PAC 3-PAC 4 boundary and at the PAC 6-PAC 7 boundary (fig. 5).
Interpretation of the Manlius-Coeymans Formation boundary as an unconformity at Thacher Park is based on the absence of PAC 8 and on the sharp contact separating markedly disjunct facies. Farther to the south along the Hudson Valley progressively more PACs were eroded as a result of differential uplift of the eastern side of the basin.

A6: STRUCTURE AND ROCK FABRIC WITHIN THE CENTRAL AND SOUTHERN ADIRONDACKS
James McLelland
Colgate University
Hamilton, NY

A6: STRUCTURE AND ROCK FABRIC WITHIN THE CENTRAL AND SOUTHERN ADIRONDACKS

A7: CAMBRO-ORDOVICIAN SHOALING AND TIDAL DEPOSITS MARGINAL TO IAPETUS OCEAN AND MIDDLE TO UPPER DEVONIAN PERITIDAL DEPOSITS OF THE CATSKILL FAN-DELTAIC COMPLEX
Gerald M. Friedman
Brooklyn College
Rensselaer Center of Applied Geology
Affiliated with Brooklyn College of the
City University of New York
P.O. Box 746, 15 Third Street
Troy, New York 12181
This field trip, in which sedimentary facies deposited in Cambrian, Ordovician, and Middle to Upper Devonian shallow-water marine environments will be examined, has been divided into two parts. The first three stops will be devoted to facies of the Cambro-Ordovician period, and the last three will cover the Middle to Upper Devonian facies.

A7: CAMBRO-ORDOVICIAN SHOALING AND TIDAL DEPOSITS MARGINAL TO IAPETUS OCEAN AND MIDDLE TO UPPER DEVONIAN PERITIDAL DEPOSITS OF THE CATSKILL FAN-DELTAIC COMPLEX

STOP 1. Lester Park
PRODUCTS OF INTERTIDAL ENVIRONMENT: DOMED ALGAL MATS (CABBAGE HEADS)
This locality is the site of one of the finest domed algal mats to be seen anywhere preserved in ancient rocks. On the east side of the road in Lester Park a glaciated surface exposes horizontal sections of the cabbage-shaped heads composed of vertically stacked, hemispherical stromatolites (Figure 5). These structures, known as Cryptozoons, have been classically described by James Hall (1847, 1883), Cushing and Ruedemann (1914), and Goldring (1938); an even earlier study drew attention to the presence of ooids as the first reported ooid occurrence in North America (Steele, 1825). Interest in these rocks has been revived as they are useful environmental indicators (Logan, 1961, Fisher, 1965; Halley, 1971). The algal heads are composed of discrete club-shaped or columnar structures built of hemispheroidal stromatolites expanding upward from a base, although continued expansion may result in the fusion of neighboring colonies into a Collenia-type structure (Logan, Rezak, Ginsburg, 1964). The stromatolites are part of the Hoyt Limestone of Late Cambrian (Trempealeauan) age. An intertidal origin has been inferred for these stromatolites (Fig. 6, 7 and 8).
The evidence for deposition under tidal conditions for the Hoyt Limestone at Lester Park includes: (1) mud cracks, (2) flat-pebble conglomerate, (3) small channels, (4) cross-beds, (5) birdseye structures, (6) syngenetic dolomite, and (7) stromatolites (for characteristics on recognition of tidal limestones, see Friedman, 1969).
At Lester Park the heads which are circular in horizontal section range in diameter from one inch to three feet; many are compound heads. The size of the larger heads suggests that they formed in highly turbulent waters.
The line of depositional strike along which the domed stromatolites occur was probably where the waves were breaking as they came across the deeper ocean from the east and impinged on the shelf.
Several petrographic observations in these rocks permit an analogy with modern algal mats in hypersaline pools of the Red Sea Coast (Friedman and others, 1973). Mat-forming algae precipitate radial ooids, oncolites, and grapestones which occur in these rocks; interlaminated calcite and dolomite, which in part compose the stromatolites of the Hoyt Limestone, correspond to alternating aragonite and high-magnesium calcite laminites which modern blue-green algae precipitate. In modern algal mats the highmagnesium has been concentrated to form a magnesium-organic complex. Between the magnesium concentration of the high-magnesium calcite and that of the organic matter, sufficient magnesium exists in modern algal laminites to form dolomite. Hence the observation in ancient algal mats, such as observed in the Hoyt Limestone, that calcite and dolomite are interlaminated, with calcite, probably forming at the expense of aragonite and dolomite forming from high-magnesium calcite.

STOP 2. Fort Hunter Quarry
Stromatolites in the Fort Hunter Quarry consist almost entirely of dolomite in the form of irregularly bedded, finely-laminated, undulating structures (Figure 9). The rocks in this quarry are part of the Tribes Hill Formation of earliest Ordovician age (Fisher, 1954). The lithofacies of the Tribes Hill formation have been studied in detail by Braun and Friedman (1969) within the stratigraphic framework established by Fisher (1954). Figure 10 is a columnar section showing the relationship of ten lithofacies to four members of the Tribes Hill Formation. At Fort Hunter we will study the lowermost two lithofacies of the Fort Johnson Member (see column at right (east) end of section, in Fig. 10).
Two lithofacies are observed: (1) lithofacies 1, mottled f~ldspathlc dolomite (Figure 10), and (2) lithofacies 2,. laminated feldspathic dolomite. Lithofacies 1 is at the bottom of the quarry, and lithofacies 2 is approximately halfway up.
Lithofacies 1
This facies occurs as thin dolostone beds, 2 cm to 25 cm but locally more than 50 cm thick, with a few thin interbeds of black argillaceous dolostone which are up to 5 cm thick. In the field, the dolomite shows gray-black mottling and in places birdseye structures. In one sample, the infilling of the birdseyes shows a black bituminous rim which may be anthraxolite. In the field, trace fossils are abundant, but fossils were not noted. Authigenic alkali feldspar (microcline) is ubiquitous throughout this lithofacies; its identity as alkali feldspar was determined by Xray analysis and staining of thin sections with sodium cobaltinitrite. The insoluble residue makes up 22 to 54% by weight of the sediment in samples studied with most of the residue composed of authigenic feldspar. An iron-poor yellow sphalerite may be occasionally found in the rocks of this lithofacies.
Lithofacies 2
This lithofacies is mineralogically identical to the previous facies but differs from it texturally and structurally in being, irregularly bedded and in containing abundant undulating stromatolitic structures ("pseudoripples"), as well as disturbed and discontinuous laminae. In places there are a few thin interbeds of black argillaceous dolostone. The thickness of the laminites of this facies ranges from 1/2 mm to 2 or 3 mm; on freshly broken surfaces the color of the thinner laminae is black and that of the thicker ones is gray. The insoluble residue, for the most part composed of authigenic feldspar, constitutes between 35% and 67% by weight in samples studied.
These two lithofacies which form the basal unit of the Ordovician, were formed on a broad shallow shelf. Stromatolites, birdseye structures, scarcity of fossils, bituminous material, syngenetic dolomite, authigenic feldspar, and mottling suggest that these rocks were deposited in a tidal environment (Friedman, 1969). Based on analogy with the carbonate sediments in the modern Bahamas, Braun and Friedman (1969) concluded that these two lithofacies formed under supratidal conditions. However, in the Persian Gulf flat algal mats prefer the uppermost intertidal environment and along the Red Sea coast they flourish where entirely immersed in seawater, provided hypersaline conditions keep away burrowers and grazers (Friedman and others 1973). Hence on this field trip we may conclude that the stromatolites indicate tidal conditions without distinguishing between intertidal and supratidal. For more details on these lithofacies refer to Braun and Friedman (1969).

Cross original Erie Canal, built in 1822.
Cross original Erie Canal, built in 1822. Amos Eaton surveyed this route at the request of Stephen Van Rensselaer; after this survey Amos Eaton and Van Rensselaer decided to found a school for surveying, geological and agricultural training which became Rensselaer Polytechnic Institute.

STOP 3. North Tribes Hill Quarry
Route of Walk
Take the trail toward old abandoned crusher, but instead of heading toward the quarry move uphill to the first rock exposures. The rocks to be examined are near the edge of steep cliff.o
Description and Discussion
In the rocks at this exposure the field relationships show typical channels truncated at their bases. Lodged within the channels are limestone blocks of variable shape ranging in diameter from about one to three feet. These blocks resemble similar blocks in tidal channels of the Bahamas which are derived by undercutting of the banks of the tidal channels. The blocks at this exposure are rounded, suggesting that they have undergone some transport.
The rocks composing the channel (the channel fill) and the blocks of rock within the channels have been described as lithofacies 8 (Figure 11) (channel fill) and lithofacies 7 (Figure 12) (blocks) of the Wolf Hollow Member of the Tribes Hill Formation (lowermost Ordovician) (see columnar section of Fig. 10); column at right end of the section) (Braun and Friedman, 1969). The channel fill (lithofacies 8) consists of intrasparite and biointrasparite with sporadic ooids, a high-energy facies, whereas the blocks (lithofacies 7) consist of mottled dolomitic micrite and biomicrite, a low-energy facies of the undercut bank. The micrite blocks which foundered in the channels must have been indurated penecontemporaneously (Fig. 13).

STOP 4. Marsh Facies
STOP 4. MARSH FACIES
No examples of the marsh facies have been found in situ. However, giant seed ferns of the Gilboa Forest (Goldring, 1924, 1927), which grew in a marsh environment, were discovered in the now-inactive Riverside Quarry near here. More than 200 stumps were taken from this single quarry; some of these have been placed at this site, others are now preserved in museums. The "trees" of Gilboa Forest are among the world's oldest; they grew in a marsh environment of the Catskill Deltaic complex. The bulbous bases of these fossils were found in place in dark-colored shale; the upright trunks were encased in olive-gray, cross-bedded sandstone of probable tidal origin. The age of the "trees" is latest Middle Devonian.

STOP 5. Intertidal Facies: Tidal Flats and Tidal Channels
The rocks at this exposure are medium-gray, fine-grained graywackes; tabular cross-beds are ubiquitous, parting lineations are common. The most interesting single feature at this exposure are the tidal channels. These channels are small, about 2 to 10 feet in cross-section; they truncate the underlying strata. The channel fill consists mostly of a lag concentration of transported spiriferid brachiopod shells (Figure 14). Usually the shell material is abundant enough to rate for the channel the name "coquinite." Holes in the coquinites are brachiopod molds. Interestingly, brachiopod shells are confined only to the coquinite lenses; they are not found in the surrounding rock. Hence the brachiopods were treated by the channels as pebbles that were washed in from the open marine environment. In analogous modern tidal channels, typical open sea species are washed into the channels by flood tides (Van Straaten, 1956).
An alternate interpretation for the coquinite lenses is that they may be storm deposits. The lenses are lag concentrates of brachiopod shells; in the contiguous sandstones pelecypods, chiefly Unio, occur. If these lenticular coquinite lenses were tidal channels,then according to this alternate interpretation, lateral cutting should have concentrated the molluscs. Yet these lenses are devoid of molluscs, hence storms rather than tidal action should have caused the coquinite lenses.
Load-flow structures, formerly known as ball-and-pillow structures, load casts or storm rollers are locally present. They represent compactional differential loading. These structures may be related to slumping and are common on the front of modern deltas.
Note that the next exposure south (uphill) is composed of red fluvial rocks.
This exposure has been described by Johnson and Friedman as part of their section 43 (1969, p. 471-475, especially Figs. 22 and 23). These rocks are the clastic correlatives of the Tully Limestone (early Late Devonian or latest Middle Devonian).

STOP 6. Deposits Of Lagoons And Bars Or Tidal Deltas
At this exposure lenticular sandstone bodies interfinger with dark-gray siltstones and shales. The sandstones have a vertically shingled, or en echelon, configuration relative to one another. Even the thickest sandstone, approximately 6 feet thick, thins and pinches out laterally (see Fig. 25, p. 478 in Johnson and Friedman, 1969). The sandstones contain marine fossils and wood fragments. In places they are crossbedded; ripple marks are locally present. In the siltstones and shales wood fragments are abundant. The presence of marine fossils, the absence of channels, and the lenticular geometric configuration of the sandstones within interfingering siltstones or shales suggests that the sandstones may be bars or tidal deltas. If so, the siltstones or shales are of lagoonal origin.
The rocks at this exposure belong to the Hamilton Group (Middle Devonian) and are about 600 feet below the stratigraphic level of the Tully clastic correlatives.

A8: ROCKS AND PROBLEMS OF THE SOUTHEASTERN ADIRONDACKS
PHILIP R. WHITNEY
Geological Survey, New York State Museum*
Purpose of the Trip
This trip is a roadcut tour of the easternmost fault block of Proterozoic rocks in the Southeastern Adirondacks, and has two major purposes. For beginners in Adirondack geology, the trip will provide an introduction to the major rock types of the area, as well as to many of the characteristic structural features. For the advanced student or professional, the emphasis will be on the numerous unsolved or partially solved problems presented by these extremely complex rocks.
This article is not a report on a finished project, because the writer has not done detailed mapping in the area. The discussion therefore consists largely of preliminary descriptive material, based on a few reconnaissance traverses by the writer and colleagues, plus more detailed examination of the rocks at the scheduled stops, and some very preliminary petrographic work. Previous work in the area includes mapping by Hills (1965) in the southern part of the Pinnacle Range, and by Berry (1961) in the portions of the Whiteball and Putnam quadrangles W and N of the trip area.
Location
The rocks seen on this trip are exposed in roadcuts along Routes 4 and 22 in the Fort Ann and Whitehall 7 1/2 minute quadrangles. They are part of a tilted fault block of Precambrian rocks at the southeastern edge of the Adirondack Highlands, which has been called the Pinnacle Range by Hills (1965). The eastern side of this block is close to the contact with overlying Paleozoic rocks; the unconformity itself is exposed at stop 3.
*Contribution number 462 of the New York State Science Service

A8: ROCKS AND PROBLEMS OF THE SOUTHEASTERN ADIRONDACKS

Outcrops of Cambro-Ordovician Beekmantown carbonates.

Fault block of Precambrian rocks
As you leave the village, notice the range of hills straight ahead. The eastern slope is a dip slope on a fault block of Precambrian rocks (known as the Pinnacle Range) bounded on the west by the Welch Hollow Fault (Hills, 1965). The Paleozoic rocks previously noted are on the downthrown (W) side. This is the easternmost of several such fault blocks, all showing a gentle, regional eastward dip of 10-15° on the Precambrian rocks and overlying paleozoics. The eastern slope of this block is a dip surface close to or at the unconformity, which will be seen in outcrop at stop 3. Is the tilt of this surface a result of a rotation of the fault blocks, or a reflection of the Tertiary-Recent doming of the Adirondacks (Isachsen 1975)?

STOP 1. A plaque on the face of the outcrop
Turn into parking area on R (SE) side of road and cautiously cross road to outcrops on opposite side. A plaque on the face of the outcrop commemorates the Battle of Fort Ann (July 8, 1777). The rocks here are intensely foliated and fractured representatives of the anorthosite suite. Although the characteristic andesine megacrysts found in anorthosites elsewhere in the Adirondacks are absent here, they can be found sporadically in other outcrops along the west side of the Pinnacle Range. Minerals in the anorthosite at this stop consists of recrystallized and sericitized plagioclase, hornblende, clinopyroxene and garnet. Large garnets (please do not sample) are surrounded by leucocratic haloes which locally obliterate the foliation, which suggests that the garnet grew at the expanse of mafic minerals which define the foliation, and that it postdates at least the first deformation.
At the eastern end of the outcrop is a large mass of gabbroic rocks (plagioclase-clinopyroxene- garnet-ilmenite) which displays little or no foliation, and around which the foliation in the anorthositic gneiss is deflected. Also present in the outcrop are a breccia zone and numerous closely spaced fractures with a general northeasterly trend; a major high angle fault may exist roughly parallel to the road.

Coarse marble with amphibolite and gneiss
Outcrops in woods to L of road are coarse marble with numerous detached and rotated blocks of amphibolite and gneiss around which the foliation of the marble is wrapped.

STOP 2. Foliated gneiss with banding and folds
Stop #2. Roadcut on R (SE) side of road. Strongly foliated quartz- 2 feldspar-pyroxene-hornblende-garnet gneisses, ±. biotite. Leucocratic bands contain numerous pyroxene megacrysts, both clino and ortho, the latter showing characteristic rusty weathering color. These rocks are close to the charnockitic end of the migmatitic gray gneiss spectrum. Note the presence of at least two types of amphibolite. One is relatively coarse grained, boudinaged and injected with leucocratic veinlets. The foliation within the boudins is locally truncated by that in the enclosing gneisses. The other amphibolite is dark, fine-grained, biotite-rich, and lacks the leucocratic veining and prominent foliation of the coarser amphibolite. The fine-grained, massive amphibolite forms a megaboudin or recumbent fold (which is it?) near the center of the cut. Do these amphibolites represent one, two, or more generations of mafic intrusives?
Numerous complex minor folds are present within the gneisses; also observe the warping of the foliation by larger, open folds. Measure and record lineations and attempt to relate them to the fold axes of both types. Is more than one lineation present in these rocks?
Thin, folded dark bands near the N end of the cut are a peculiar, fine grained carbonate-rich rock with poorly oriented biotite.

STOP 3. Proterozic / Paleozoic unconformity
The outcrop on the R side of Rte. 4 just beyond the intersection exposes the unconformity between Proterozoic and Paleozoic rocks (missing: roughly 500 million years of the geologic record, and 20-25 km of Proterozoic rock). The Paleozoic rocks here are coarse arkosic sandstones and quartz-pebble conglomerates of the Cambrian Potsdam Formation, locally with carbonate cement. Measure the strike and dip of the unconformity surface, and compare this with the 10-15° easterly slope of the fault block as observed driving N out of Fort Ann.
Observe the lack of evidence for deep weathering of the Precambrian rocks beneath the contact, and the absence of a paleosol layer. This suggests deep erosion and scouring (by waves? ice?) shortly before deposition of the Potsdam.
Walk a few meters along the S face of the outcrop, towards the canal. Note the complex fracturing of the gneisses, and the filling of the fractures with dark, fine-grained dolomitic rock. The significance of this feature is unclear, and it will be discussed in more detail on the trip. Note the deeply weathered zone where these rocks are exposed at the surface.
After examining the unconformity, cautiously cross the road to the cut in complexly deformed gray gneisses on the opposite side. Measure several lineations here and compare with what you saw at stop #2. Note not only differences in orientation, but also in the nature of the lineation.

Potsdam Sandstone
Outcrops at edge of woods on R are fine-grained white arkosic Potsdam sandstones.

Granitic gneisses close to a NS brittle fault.
Outcrops on L are extensively fractured granitic gneisses close to a NS brittle fault.

STOP 4. Kinzigite and amphibolite
The rocks immediately to the R are strongly foliated biotite-quartz-2 feldspar-garnet gneisses. This version of the gray gneiss is commonly referred to as "kinzigite". Present in this outcrop are thin quartzo-feldspathic pegmatites in various stages of tectonic disintegration and reorientation. The large K-feldspars survive the tearing-apart process better than quartz, and remain visible as large porphyroclasts, either in strings or as isolated individuals. Be alert for evidence of tectonic rotation of these feldspars, which can be a useful indicator of the sense of shear.
Also observe the variable shape and appearance of the garnets: some are rounded and others elliptical: some are nearly inclusion-free while others are "spongy". Careful study of this variation might, if combined with probe analysis of garnet compositions, yield information on the interrelation of metamorphism and deformation of these rocks.
From here, walk northward along the road past a gap in the outcrop, then enter the S end of a long cut. The first rocks are strongly foliated and lineated gray gneisses with lenses and pods of calcsilicates. Roughly 30 m. northward and uphill, these overlie amphibolitic rocks, which comprise most of the remainder of the cut. The bulk of these rocks are strongly foliated garnet amphibolites and mafic gneisses. Numerous lenses and pods of calcsilicates, garnet hornblendite, and ultramafic rocks are present. (Students: the coarse grained ultramafic pods are a fine opportunity to test your mineral recognition skills). About 90 m. northward along the cut a large pod of calcsilicate granulite (grossular-diopside-quartz) is visible in the mafic gneisses on the opposite side of the road. Near the N end of the cut, still on the R (E) side, two large pods or megaboudins of massive, relatively fine grained, garnet-rich metagabbro are surrounded by strongly foliated amphibolites. The transition between foliated and unfoliated rock is very abrupt. Patches of tourmaline- bearing pegmatite are present at the broken(?) end of one of the megaboudins.

STOP 5. Gneisses and Gabbros
Cross the road and walk N along the W side. At the S end are more gray gneisses, here with a distinct reddish tinge caused by an abundance of garnet. The gray gneisses here are nearly devoid of K feldspar. They become more strongly foliated toward the contact with overlying pink granitic gneisses. The contact itself is extremely sharp (but note the late spherical, undeformed garnets, some of which are situated directly on the contact). The pink granitic gneisses, which contain biotite, chlorite and garnet, are strongly foliated, approaching mylonitic texture in places, and display prominent quartz ribbon lineation. The less deformed parts of these gneisses contain K-feldspar megacrysts (phenocrysts? porphyroblasts?) in various stages of deformation and recrystallization.
Continuing N, pass a large gabbro pod, broken at the base and injected with granitic material, in part pegmatitic. Look S across the road; the similarly shaped body of gabbroic rock in the pink gneisses is probably the same pod. Then re-enter gray gneisses, here with somewhat more K feldspar, which is concentrated in the leucosomes. Notice the prominent discontinuity in the foliation which is visible for some distance along the cut. Even though little textural evidence (e.g. grain size reduction) for shear displacement exists along the discontinuity, other explanations for this feature are even more difficult to defend. Toward the N end of the cut is another body of gabbroic rock, which also appears to continue on the opposite side of the road. These mafic rocks, which intrude both the gray and pink gneisses, are generally fine grained and massive with a distinct relict igneous texture. Much garnet is present in the form of indistinct coronas. These rocks are the equivalent of the coronitic olivine metagabbros, a more typical example of which will be seen at stop #8. These gabbroic bodies (several are present here) are lensoid to sigmoidal in cross section but apparently elongated in a roughly N-S direction. Their crudely sigmoidal shape yields opposite estimates of shear sense depending on whether they are pre- or syn-tectonic in origin.
Cross the road to the E side, and note the prominent minor folds in the migmatitic gray gneisses near the N end of the cut. Also note the open, upright folds, which warp the foliation of these rocks, then compare the orientation of these with the recumbent, isoclinal minor folds and with the lineation. Then walk S along the E side and return to the starting point. The petrology of the rocks at this outcrop has been studied in detail by William Glassley and students at Middlebury College. Dr. Glassley (pers. comm. 1985) reports the following:
"Garnet-clinopyroxene and garnet-biotite temperatures were computed from microprobe data. Average temperatures from eight samples ranged from 770 C to 850 C, with a strong mode at 810 C. Pressures, calculated from the assemblages garnet-plagioclase-clinopyroxene-quartz and garnet-plagioclase-orthopyroxene-quartz using the method of Newton and Haselton, averaged 7.5 kb + .5 kb.
"Two unusual assemblages can be found along the contact between the two gneiss units. Within 50 cm of the contact occur 1-3 cm long augen which contain the assemblages clinopyroxene-garnet-rutile and biotite-sillimanite-hercynite-kspar-garnet. The former assemblage is a typical eclogite assemblage. Garnets from these eclogitic lenses are similar to those reported from basal gneiss eclogites in Western Norway. The clinopyroxenes, however, are poor in jadeite component, with only 5% of this component present. The sillimanite- spinel-bearing assemblage is clearly consumed and biotite and sillimanite are being generated. The significance of this assemblage for P-T conditions remains obscure, in that we do not yet have compositional data for all of the minerals in the assemblages nor do we have water fugacity values that would allow calculation of the equilibrium conditions."

STOP 6. (Optional) Paragneiss
The rock here is a pale gray biotite-quartz-2 feldspar-garnet-sillimanite-graphite paragneiss with thin layers and lenses of calcsilicates. Compared to the previously examined "kinzigites", this rock is finer grained, more aluminous, and has distinctive lavender garnets. The abundant white layers look like leucosomes in a migmatite, but they contain significant amounts of sillimanite and are thus probably more aluminous than minimum-melt granite. Note the flattening of the quartz in these layers. Look carefully for lineations defined by sillimanite and quartz.
The protolith of these rocks must have had a significant argillaceous component, as indicated by the presence of both garnet and sillimanite. The lavendar-colored garnets are typical of many Adirondack metapelites, a more extreme example of which will be seen at Stop #9.

STOP 7. North end of roadcut.
Pull off road on R and cautiously cross to outcrops at N end of cut on west side; walk S along outcrop. Probably the best way to appreciate these rocks is to move rather rapidly to the S end, scanning the rocks on both sides as you go for major lithologic changes, and then return northward looking at the rocks in detail.
The sequence of rock types going S on the W side is as follows:
A Interlayered (or interleaved?) marbles and paragneisses
B Garnetiferous quartzofeldspathic gneisses intruded by unmetamorphosed mafic dikes
- Gap -
C Charnockitic gneiss
D Thin marble with numerous exotic blocks
E Mafic gneiss
F Calcsilicates and marble
G Interlayered (interleaved?) Paragneiss, charnockite, marble and calcsilicate with amphibolite boudins. An unmetamorphosed mafic dike forms the face of much of this section of the cut.
Details (walking N)
G. Note the wide variety of rock types, including charnockitic gneisses, amphibolites, marble (carefully examine the marble/amphibolite contact), lineated sillimanite bearing metapelites, and calcsilicates. Note the local slickensides along foliation surfaces as well as on vertical fractures. Has there been late movement parallel to the foliation?
F. This thin calcareous unit consists of marble near the base and a complex calcsilicate zone adjacent to the contact with the overlying mafic gneiss. Major minerals in the calcsilicate zone are grossular, diopside, quartz, calcite and K feldspar, with lesser amounts of plagioclase and chlorite as well as several minor phases yet to be identified. Some evidence indicates that wollastonite was initially present but none has yet been positively identified. The calcsilicates probably originated by contact metamorphism at the time of intrusion of the igneous precursor of the overlying mafic gneiss. This contact is irregular and appears to have been folded. The thickness of the calcsilicate layer varies widely, both in this outcrop and on the opposite side of the road.
E. This mafic gneiss contains plagioclase, clinopyroxene, hornblende, biotite, garnet and minor quartz and K feldspar. The composition is probably similar to a monzodiorite. Similar rocks elsewhere in the Adirondacks have been called "jotunite" and are associated with the anorthosite suite of rocks. The rock is well foliated throughout, but becomes more so towards the sharp upper contact. On the opposite (E) side of the road, a detached sliver of the mafic gneiss is found in the overlying marble, and contains carbonate-filled fractures.
D. The next unit upward is a thin (generally < 1 m) band of marble with numerous rotated fragments of other rocks. No calcsilicates are developed near the sharp contact with the mafic gneiss beneath, and the foliation both in the mafic gneiss and in the overlying charnockitic gneiss is strongly developed and parallel to the marble band. In the outcrop on the opposite side of the road, foliation in the charnockite is locally truncated by the marble. This marble is a good example of a possible detachment zone, with relative movement of uncertain direction and magnitude, between the mafic gneiss and the charnockite. The absence of a contact metamorphic zone of calcsilicates at the upper contact of the mafic gneiss may result from its having sheared off during displacement. Alternatively, this marble may be a tectonically emplaced younger rock (see discussion under unit "A", below). Considerable displacement may have taken place along most or all of the marble layers in this outcrop.
C. Above the marble is a thick unit of charnockitic gneiss. This rock, close to granite in composition, consists of quartz, microcline, plagioclase, hornblende, garnet, clinopyroxene and orthopyroxene. The orthopyrcxene is extensively chloritized, which is characteristic of many Adirondack charnockites. The typical green color is well developed toward the center of the unit. Near the northern end of the outcrop both green and white varieties are present, with diffuse color boundaries which crosscut foliation.
Immediately beyond the charnockite unit is a gap in the outcrop, possibly indicating the presence of a fault or thick marble layer.
B. Following the gap is a short section of well foliated, garnetiferous quartzofeldspathic gneisses similar to the charnockite but with green color less well developed. Note the unmetamorphosed mafic dike just back from the face of the outcrop, and roughly parallel to it. A few meters farther N is a complex vertical fault with a zone of carbonate-cemented breccia.
A. The last section of the outcrop, roughly 100 m long, consists of interlayered (interleaved?) paragneiss and marble, with minor amphibolite and thin calcsilicate bands in the paragneiss. Contact surfaces are frequently slickensided and/or coated with graphite. At least two types of marble are present; one is dark, relatively fine grained, brown-weathering dolomite marble, which has a slightly fetid odor when struck with a hammer; the other is coarser grained, has a somewhat lighter color and considerable calcite as well as dolomite. Both marbles contain abundant rounded to angular silicate rock and mineral fragments, including quartz, feldspar and serpentine, and larger rotated blocks of various rock types including amphibolites, serpentinite, paragneiss and calcsilicate granulite. Quartz, dolomite and serpentine coexist in these rocks with no evidence of mutual reaction, indicating that the rock as presently constituted has never undergone high temperature metamorphism. Temperatures must have been sufficiently low to prevent reaction of quartz with either dolomite or serpentine. It is probable that these marble zones, as well as those of units G, F and D, are tectonic breccias formed along thrust faults or low-angle normal faults under conditions that permitted the carbonates to recrystallize and deform in ductile fashion, while silicates behaved in a more brittle manner. The interleaved paragneisses, by contrast, are similar to the gray gneisses seen in previous stops, have a high-T metamorphic assemblage and show little evidence of retrogression.
The age of the tectonic interleaving of the gneisses and marbles may be either late Proterozoic or Taconic. The marbles themselves may be Proterozoic with retrograde serpentine after forsterite and entrained fragments of quartz and feldspar, or they may be Paleozoic carbonates with entrained fragments of ultramafic rocks. This question is now under study and will be discussed on the outcrop.

STOP 8. (Optional) Typical Adirondack olivine metagabbros
Stop #8 (Optional). Park as far off the road to the R as possible. Cross with great care to outcrops on the L, and examine them briefly. These are typical Adirondack olivine metagabbros, with well preserved igneous textures as well as coronitic reaction rims around olivine and ilmenite (see introductory section). The interiors of the olivine coronas here have been retrograded to chlorite and carbonate; otherwise the rocks are quite fresh.

Dip-slope on foliation
Flat outcrops on slopes to the L are a dipslope on foliation in highly strained gneisses. A short distance N, on West Mtn., a mylonite zone close to 300 m thick is exposed. The hills across the valley to the R, and on Skene Mtn. straight ahead, are Cambro- Ordovician carbonates of the Whitehall Formation, resting on Potsdam sandstone.

STOP 9. Typical metapelites
Pull off road to R close to smaller outcrop, and cross to larger cut on L. The rocks here are typical metapelites, consisting of quartz, K feldspar, sillimanite, lavender garnet and varying amounts of biotite and graphite.

Entering series of cuts in highly fractured metasedimentary rocks.

STOP 10. Abandoned Quartzite Quarry
Entrance to abandoned quarry and Washington County Highway Dept. Garage. This is posted private property; if following this road log on your own, ask permission at large brick farmhouse 0.2 miles further along road on R. Be extremely careful climbing and hammering here - there is much loose rock and the quartzite is very splintery when hammered.
This thick unit of quartzite is interlayered with lesser amounts of a greenish rock which forms bands and streaks from a fraction of a millimeter up to several tens of centimeters thick, with knifesharp contacts against the quartzite.
The quartzite, which is visibly foliated in hand specimen, comprises over 95% of strongly flattened quartz; small, flattened and elongated grains of K feldspar and sericitized plagioclase, lensoid garnets, green biotite and chlorite. The interlayered green rock ranges from plagioclase-quartz-garnet-biotite-hypersthene gneiss to a retrograded epidote-chlorite-quartz-plagioclase rock with some muscovite and at least two minerals yet to be identified. Some well crystallized chlorite is present as flakes parallel to the foliation, but chlorite also occurs locally as an alteration product of garnet. Distribution of the retrograde assemblage within the outcrop has not been determined. If it is related to fracture patterns, it may be low temperature alteration along the E-W brittle fault which parallels the road. If not, it may be evidence for localized retrogression associated with renewed, layer- parallel shearing during the latest Proterozoic or during the Taconic event. Supporting the latter hypothesis are slickensides on foliation surfaces at an acute angle to the lineation.
All rocks at this site show extreme foliation and a well developed lineation, here close to E-W, with a 0-20° E plunge. Numerous minor folds are present. These are of two distinct types, both of which are recumbent with axes parallel to the lineation. One type consists of intrafolial, highly asymmetric, isoclinal folds defined by thin micaceous layers in the quartzite. Among folds of this type is an apparent sheath fold strongly flattened in the plane of foliation. The other type is not quite isoclinal, more symmetric, and visibly folds the foliation in the quartzite. The minor folds and petrofabrics at this outcrop have been described by Granath and Barstow (1980), who attribute the deformation primarily to a severe flattening strain.

Fault bounded block
Crossing South Bay on Lake Champlain. The rocks underlying the valley to the North are Paleozoic strata downdropped along a major normal fault which here forms the western side of the Pinnacle Range.
Toward the south, this fault intersects the Welch Hollow fault at an oblique angle. The fault follows the shore of South Bay south of the bridge, then strikes inland and follows the line of cliffs visible to the north. Estimated vertical displacement on this fault based on offset of Paleozoic cover rocks is in the vicinity of 300 m. West of the bay, outcrops of gently E-dipping, highly deformed Precambrian rocks resume.

A9: CAMBRIAN AND ORDOVICIAN PLATFORM SEDIMENTATION - SOUTHERN LAKE CHAMPLAIN VALLEY
Bruce Selleck
Brewster Baldwin
Middlebury College
The Cambrian-Medial Ordovician strata of the southern Lake Champlain Valley record the evolution and demise of passive margin sedimentation on the North American coast of the proto-Atlantic Ocean. The goals of our trip are to examine exposures of key units in this stratigraphy, interpret the depositional environments represented and consider the possible tectonic controls over the history of platform sedimentation during the early Paleozoic in eastern North America.
Our trip will focus on two sections of the stratigraphy: (1) the Late Cambrian Ticonderoga Dolostone and basal Whitehall Formation and (2) the Medial Ordovician Chazy, Black River and Trenton Groups. The general area of interest (Fig. 1) lies within the Ticonderoga and Port Henry, N.Y. 151 Quadrangles.

STOP 1A. Ticonderoga Dolostone
Relatively new roadcuts on Shore Airport Road provide excellent exposures of portions of the Ticonderoga Dolostone and Whitehall Formation. The generalized stratigraphy of this series of outcrops is presented on the following pages. Stop 1A is wholly within the Ticonderoga Dolostone; lB is uppermost Ticonderoga Dolostone or basal Whitehall (Finch Dolostone of Fisher, 1984) Formation; Stop lC is clearly Whitehall Formation, Finch Dolostone Member. We will walk upsection from the base of Stop 1A to Stop 1B, reboard the bus to Stop 1C. Please watch for cars!
A series of normal faults juxtapose blocks containing various sections of the Cambro-Ordovician stratigraphy in the Ticonderoga area. To our southwest, Proterozoic marbles and gneiss hold up Prospect Mountain. The village of Ticonderoga largely sits upon Potsdam Sandstone (Keeseville Member). To our south and east, the younger formations of the Beekmantown Group are exposed in the vicinity of Fort Ticonderoga. At this stop approximately 20 meters of Ticonderoga Dolostone is exposed. The basal 2/3 of the outcrop consists of 0.2 - 1.0 meter units of bioturbated sandy dolostone interbedded with 0.1-1.0 meter units of cross-stratified slightly dolomitic medium to fine sandstones. Rare prism cracks in the fine silty dolostones document sporadic subaerial exposure. "Herringbone" cross-strata, reactivation surfaces and shear-deformed cross-strata are well-exposed on weathered surfaces of the sandstones. Poorly preserved specimens of the gastropod Ophileta sp. are found on the bedding surface of a dolomitic sandstone approx. 8 meters from the base of the section. R. Linsley (personal communication) has suggested that Ophileta, was a relatively sedentary grazer or deposit feeder. The upper 1/3 of the section contains relatively more abundant prism cracks, sha1y interbeds and intraclast breccia horizons, perhaps indicating more regular subaerial exposure.
The rhythmically interbedded bioturbated dolostones and cross-stratified dolomitic sandstones are interpreted as high and low tidal flat/shallow subtidal facies, respectively. Carbonate mud and terrigenous sands deposited on a relatively low energy upper intertidal flat provided a suitable habitat for burrowing infaunal organisms. The lower tidal flat and shallow subtidal environment was characterized by more vigorous current action which limited faunal activity and produced cross-strata and associated structures. The repetitive interbedding of these facies suggests repetitive progradation of burrowed sandy muds over current-bedded sands. The upsection decrease in current-produced structures and increasing evidence of exposure indicates an overall shallowing up trend in the Ticonderoga Dolostone at this locality.

STOP 1B. North side of Shore Airport Road, 150 m from STOP 1A
This outcrop exposes about 7 m of silty, cherty dolostones assignable to either the uppermost Ticonderoga Dolostone or the basal Finch Member of the Whitehall Formation. The pervasive dolomitization plus outcrop weathering have obscured the primary structures and fabrics. The lower approx. 1 meter consists of laminated silty dolostones with ripple cross-lamination and thin intraclastic horizons. The succeeding 1.5 meters consists of thick-bedded to massive coarsely crystalline dolostone containing calcite-filled voids of various sizes. The succeeding 2 meters consists of bioturbated, dark medium crystalline dolostone with vaguely developed digitate algal (?) structures. Laminated, finely crystalline dolostones follow, capped by dolostones with algal mounds. In the upper 1 1/2 m of the outcrop, cherty, laminated dolostones apparently drape an irregular algal mound (thrombolites) surface. Note laminated silty dolostone between algal mounds.
The lack of diagnostic fossils and primary structures ln these lithologies make environmental assignment difficult. If the digitate algal structures and cryptalgal laminites are indeed present, a shallow subtidal to low intertidal environment may be inferred. Bioturbated dolostones could be of intertidal or more offshore origin. Any suggestions?? (We will reboard bus at this point and continue east on Shore Airport Road 400 meters to Stop 1 C.)

STOP 1C. Outcrop on north side of road, 400 m from STOP 1B
Approximately 3 1/2 meters of the Finch Dolostone Member of the Whitehall Formation is exposed at this stop. Three facies occur in a somewhat repetitive fashion: (A) Coarsely crystalline, laminated to slightly bioturbated dolostone (dolomitizad grainstone); (B) "pin-stripe" laminated cherty finely crystalline dolostone with rare burrows; and (C) dark grey to black dolomitic chert with dolomitized molluscan debris and dolomitic digitate algal stromatolites and dolomite "knots" (small algal structures??). The uppermost dolomitic chert bed thickens and thins on outcrop scale. The thicker portions of this bed appears to represent local "domes" or mounds formed by the thrombolites or algal stromatolites. Gastropod debris can be seen in one mound, perhaps representing shell material collected between cylindrical algal pillars.
The absence of direct evidence of subaerial exposure again makes exact environmental assignment quite equivocal. We suggest that the coarsely crystalline dolostones represent a "high energy" shallow subtidal/low intertidal facies; the "pin stripe" laminites a relatively lower energy muddy tidal flat facies. The dolomitic chert facies containing algal structures is probably shallow subtidal. We are again open to suggestions.
The origin of the silica for chertification of these rocks is also something of a problem. Rubin (1975) suggested that subaerial "silcretization" involving dissolution of terrigenous silicates and precipitation of opaline silica or quartz in a pedogenic setting on emergent tidal flats was a factor in chertification of Whitehall Formation carbonates. The fabrics indicating pedogenic silicification reported by Rubin are not present at this locality, however. A possible alternative is fabric-selective replacement of primary carbonate mud by silica derived from a biogenic source (sponge spicules) within the original sediment.

STOP 2A. Outpost fort east of N.Y. 8
Approximately 6 meters of variously burrowed, slightly dolomitic, thin to medium bedded bioclastic packstones are exposein this section. The dolomite occurs in shaly weathering wisps and laminae and in burrow fills. Abundant "Girvanella" algal oncolites (algal accretionary grains) are present in beds approx. 4 meters from the base of the section. Rounded dark calcite grains (abraded gastropod fragments) form the cores of the oncolites, and are scattered in other beds. Fossils are relatively abundant and best seen on bedding surfaces. Trilobite fragments, brachiopods, bryozoans, pelmatozoan plates, nautiloids and large Maclurites magnus are present. The relatively high faunal diversity, abundant lime mud and burrowing argue for a normal marine, low energy shallow subtidal carbonate environment. A possible modern analogue is found in the mixed mud and sand shelf to the west of the emergent Andros Island tidal flats, as described by Bathurst (1971) and Purdy (1963). The 5-10 cm thick beds of "oncolite conglomerate" and other more well-sorted grainstone beds may represent periods of storm winnowing of the bottom, with transportation of abraded sand from adjacent sand shoal environments (e.g. Locality 2B). The wavy, irregular dolomite laminae appear to result from post-depositional dolomitization of lime mud, followed by compaction and local pressure solution of calcite, producing irregular, clay- and dolomite-rich stylocumulate seams. Preferential dolomitization of burrows may be due to contrasts in porosity or permeability of burrow-fill versus burrow-matrix sediment. The burrow-fill sediment may have retained permeability longer during diagenesis, permitting pervasive dolomitization. This sort of fabric selective dolomitization is common throughout the Chazy and Black River Groups in the southern Lake Champlain Valley.

STOP 2B. Ledge immediately NE of gate to Historic Site
Cross-stratified coarse lime grainstones with bipolar crossbed dip directions are well-exposed near the entrance road. Siliciclastic sand grains (angular quartz and feldspar up to 2 mm in diameter) are locally concentrated along prominent stylolite seams. The carbonate particles are dominately subrounded, abraded pelmatozoan plates, plus gastropod and brachiopod fragments. Large Maclurites fragments and grainstone intraclasts are present on the upper bedding plane surfaces of the ledge.
We envision the environment of deposition of this facies as shallow subtidal wave and/or current reworked sand bars. Active transport of abraded grains may have been accomplished by tidal currents as suggested by the bipolar cross-beds. The lack of burrows and well-preserved fossils may be due to the inhospitable shiftng sand substrate. This environment may have been rather like the unstable sand shoal environments described from the Bahamas Platform by Bathurst (1971) and Ball (1967). The scale and style of cross-stratification present here are similar to that predicted by Ball from his studies of the bedforms and primary structures of the Bahamian sand bodies. Similar Chazyan facies in the Northern Champlain Valley contain abundant oolites (Oxley and Kay, 1959).

STOP 2C. Low Ledges on entrance road approx. 50 meters north of 2B
Brown weathering, slightly shaley dolostone exposed here contains small lenses and stringers of fossiliferous lime packestone. Trilobites, small brachiopods and Maclurites fragments are common. This exposure resembles the shelf lagoon facies of Stop 2A, although dolomitization is more pervasive.

STOP 2D. East point of British Fort, by horizontal water tank and south moat
Approximately 3 meters of thickly laminated limestone and dolostone is exposed in the southeast "moat" of the British Fort. The dominant facies here consists of alternating 0.5-2 cm thick laminae of limestone and dolostone - often termed a "ribbon rock". The limestone ribbons are mudstones and appear blue-grey on slightly weathered surfaces and as indentations on highly weathered surfaces. The more resistant dolostone weathers tan to brown. An erosional surface with 10-20 cm of relief is exposed near the base of the southwall. Abundant Maclurites shells occur in a shell bed on this surface. Lateral accretion cross-strata consisting of gently dipping ribbon rock are present above the erosional surface. Dolomitized burrows transect the limestone ribbons in the lower 1 meter of the section. On the less-weathered prominence on the SE corner of the moat, shallow scours containing a shell hash of brachiopods and gastropod debris are present, along with intraclasts of lime mudstone in dolostone and "Mexican Hat" structures (rolled intraclasts or pseudoclasts with a dolomitized burrow center).
We interpret this sequence as a tidal flat facies. The rhythmic limestone/dolostone "ribbon" fabric is interpreted as representing alternating slightly finer (lime mudstone) and coarser (dolostone) "tidal bedding" similar to that described by Reineck and Singh (1980) from the clastic mud/sand tidal flats of the North Sea. The Maclurites shell bed may mark the basal erosional level of a tidal channel, with the cross-stratified ribbon laminites forming by draping on the channelled surface. Variations in degree of burrowing record subtle differences in degree of subaerial exposure of the flat and/or reworking by tidal currents. Limited in situ faunal diversity is also expected in the stressed tidal flat environments. The absence of mudcracks and any indication of evaporite minerals suggests that we are seeing only the lower portion of a wet intertidal flat system preserved here.

STOP 2E. Enter Parade Grounds by barracks.
Around 1916, gunite was sprayed on the interior walls to protect the mortar from deteriorating. Starting in 1976, the N.Y. State Division for Historic Preservation began extensive maintenance, removing loose gunite, replacing rotted stones and repainting the stone walls.
In the outer wall of the first barracks, note at about eye level the stones that are nearly white-weathering. These are lime mudstones from the "Lowville" facies of the Orwell Limestone, exposed at Stop 2F.
The broad limestone outcrop west of the barracks is a cross-stratified lime grainstone with scattered subrounded quartz and feldspar sand grains. Trough cross-strata and "herringbone" co-sets of planar-tabular cross-strata are visible on the low vertical face. Large angular clasts of slightly dolomitic lime grainstones and Maclurites magnus shells are present on the uppermost bedding surfaces.
We interpret this facies as a current-dominated sand shoal environment rather similar to the exposures at Stop 2B.
Westward across the parade grounds there is a massive, bioturbated, brown weathering dolostone unit (similar to Stop 2C), overlain by 0.5 meters of very coarse-grained bioturbated, slightly dolomitic feldspathic quartz sandstone. This sandstone forms the summit of the Chazy Group (Crown Point Formation). The abundant angular quartz and feldspar granules in the sandstone suggest derivation from a relatively close granitic (Adirondack?) source terrane. These sands were apparently transported from the west during an interval of relative emergence of the carbonate platform and were briefly reworked in a shallow marine setting. The basal dolostone bed of the Black River is exposed immediately atop the sandstone.

STOP 2F - Moat Walls at North Entrance to British Fort
The section from here to locality I is within the Orwell Limestone. The basal beds consists of thick-bedded to massive lime mudstones with vertical spar-filled burrows (form - genus Phytopsis) and rare ostracodes. Fossil abundance and diversity increase in the overlying beds, with gastropods (Loxoplocus), corals (Lambeophyllum, Foerstephyllum) and brachiopods appearing. Grain size increases upsection, with sporadic appearance of intraclast grainstones and ripple cross-lamination. Overall this section is similar to the Lowville Limestone of the type Black River Group of the Tug Hill region. The facies pattern here suggests a progression from restricted (tidal or lagoonal?) mud flats (Phytopsis lime mudstones) to more open marine mixed mud/sand shelf environments.
The summit of the moat outcrop exposes a horizon of black chert nodules which can be traced laterally across the road to locality G.

Stop 2G. Ledges extending from service road to lake shore.
Watch for poison ivy!
These exposures closely resemble the Chaumont (House Creek Limestone of Fisher, 1977) facies of the Black River type section. Thick-bedded to massive richly fossiliferous lime packstones and wackestones document a normal marine, relatively low energy carbonate shelf environment. In addition to the forms mentioned earlier, the large stromatoporoid (calcisponge) Stromatocerium, the high-spired gastropods Hormotoma and Subulites, the nautiloids Actinoceras and Geisonoceras, plus bryozoans, brachiopods and pelmatozoan material are common. On some bedding surfaces, black chert nodules follow large horizontal burrows. The chertification here is post-depositional and involved dissolution and reprecipitation of siliceous skeletal material (sponge and radiolarian). The uppermost bed in this set of ledges is a black chert bed approximately 2 cms thick. This bed can be traced to the lake shore where a similar section can be seen. Glacial abrasion obscures much of the detail that is exposed on more weathered surfaces.

STOP 2H. Blocks and Quarry Walls by Lake Shore
The quarry was established in 1870 by the Fletcher Marble Co. in an unsuccessful attempt to find a source of "black marble" dimension stone. The quarry is reportedly only 1 meter or so deep. The narrow spit going north was built to load blocks on barges, but evidently no blocks were shipped. The quarried blocks consist of medium to thick-bedded fossiliferous packstones and wackestones with some ripple cross-laminated grainstone beds visible in the north quarry bench. Strophomenid brachiopods, bryozoans, pelmatozoan stems and fragments of the trilobite Isotelus are present. The environments represented here are similar to those at 2G. As we continue north and walk along the lake shore, more exposures of the upper part of the Orwell can be examined. The bedding surfaces contain abundant opercula of Maclurites logani, and scattered Forstephyllum, Lambeophyllum and Stromatocerium are found. The byssate bivalve Ambonychi is also present.
The transition from the Orwell to overlying Glens Falls Limestone is covered by beach gravels as we continue west along the lake shore.

STOP 2I. Exposures of Glens Falls ls separated by intervals of beach gravels
Stops 2I ,J, ad K - Series of exposures of Glens Falls Limestone separated by covered intervals of beach gravels
The westernmost outcrops are on Private Property beyond Locality K. Do not go onto that part of the shore (marked by fence and stone wall, plus the large dead elm tree).
The Glens Falls limestone consists of medium to thin-bedded lime packstones and wackestones with some well-laminated, fine-grained bioclastic grainstones. Many limestone beds show internal grading from coarse, fossil-rich bases to less fossiliferous, fine-grained tops. Thin shaley interbeds separate the limestone beds. Horizontal trails and burrows (including form-genus Chondrites) are common on some bedding surfaces.
Fossils are abundant and rather diverse. Trilobites (usually fragmental) include Isotelus, Flexicalymene and rare Cryptolithus; the brachiopods Sowerbyella, Rafinesquina, Dinorthis and Dalmanella; bryozoans Prasopora, Eridotrypa and Stictopora; plus orthocone cephalopods and pelmatozoan debris. Gastropods, which are so abundant in the underlying Orwell limestone are exceedingly rare in the Glens Falls.
The environment of deposition for the Glens Falls is a sub-wave base shelf. No shallow water features are observed and the graded limestone beds are evidently deposited by density/turbidity currents generated on adjacent, slightly shallower portions of the shelf. The Glens Falls here records the continuing deepening of the Middle Ordovician shelf that began with the deposition of the Phytpsis lime mudstones at Stop 2F. The shale interbeds and generally more argillaceous character of the Glens Falls document increase in terrigenous mud input, perhaps derived from the rising Taconic Orogenic complex to the east. Quartz and feldspar grains of volcanic origin are also common in insoluble residues of Glens Falls limestones, suggesting increased eruptive activity at this time.
The contrast in terrigenous content of the Chazy Group vs. Black River and Trenton Groups is noteworthy. Insoluble residues from Chazy Group carbonates contain abundant, coarse-grained, rather angular quartz and feldspar grains (e.g. Stops 2B and 2D) plus clay-size material whereas the Black River and Trenton Groups lack coarse sand-size grains and contain either volcanic quartz and feldspar (Black River and Trenton Groups) or clay plus volcanics (Trenton Group). This change is likely related to a shift in available clastic source from the slightly emergent cratonic basement to the west that was exposed during Chazy Group deposition to the rising Taconic volcanic/metamorphic complex to the east during Black River-Trenton Deposition.
Combining the environments of deposition with the time-thickness pattern of sedimentation, the Crown Point section takes on tectonic meaning. The Chazy sediments were deposited just about at sea level -- Girvanella and Maclurites. The Orwell was deposited in shallow sub-tidal conditions -- two corals, the grazing snail Maclurites, and probably the Stromatocerium. The Glens Falls was deposited in a more offshore setting.
A time-thickness graph for the Cambrian-Ordovician sequence of the Champlain Lowlands shows some interesting changes in slope. Sedimentation through the Chazy yields a concave-upward curve that shows a continued slowing of crustal subsidence. Then, starting with the Orwell, the crustal subsidence is greater than the rate of sedimentation, because the water deepens. Using the Middle Ordovician time scale of Churkin and others (1977), it is clear that Chazy sedimentation was scarcely 5 m/m.y.; the Orwell and Glens Falls accumulated at 30 or 40 m/m.y., and the thick shales accumulated at 200 m/m.y. (solid-grain thickness). This high rate is comparable to the rate of subsidence of the Australian platform entering the Timor trench (600 m/m.y.; Baldwin, 1982).
The Crown Point section, then, fits the picture of a cooling and slowly subsiding continental margin, through Chazy time. Then, the margin began collapsing as it tried to enter a subduction zone to the east, causing water to deepen rapidly. The section is a record of the very early part of the Taconic Orogeny, as the "east-moving proto-North American Plate 'felt' the presence of an approaching island arc" (Baldwin, 1982). collision that constitutes the Taconic orogeny.

A10: GLACIAL GEOLOGY AND HISTORY OF THE NORTHERN HUDSON BASIN, NEW YORK AND VERMONT
DAVID J. DE SIMONE
Department of Geology, Rensselaer Polytechnic Institute
Troy, New York 12180-3590
ROBERT G. LA FLEUR

A10: GLACIAL GEOLOGY AND HISTORY OF THE NORTHERN HUDSON BASIN, NEW YORK AND VERMONT

Ahead is the Batten Kill delta (310-320 ft Lake Quaker Springs).

NY 29 climbs the foreslope of the delta
NY 29 climbs the foreslope of the delta approximately along the axis of maximum thickness of gravel and sand. The banks along the road reveal the coarsening-up stratigraphy.

Water well logs record up to 65 ft of deltaic gravel and sand in the area.

STOP 1: Hollingsworth-Vose landfill.
Deltaic topset and foreset beds of the Batten Kill's Quaker Springs delta.

Deltaic gravel and sand, lake clay, and lodgement till are exposed.

Sediment thins rapidly southward
Water well logs and exposures indicate deltaic sediment thins rapidly southward through 30 ft to less than 10 ft. Notice the clay dug up from the pond farther along the road.

Groundwater flows out along the SG-clay contact
Groundwater flows out along the SG-clay contact at the heads of these gullies in Fryer Brook. We observed a pipe with a diameter just right for your arm at the head of one gully in 1977.

Notice the clay gullies as Wilbur Ave. crosses Fryer Brook.

Traversing the dissected clay plain and delta sand is gone
We're traversing the dissected clay plain and delta sand is gone so we cross Flately Brook and turn to the E.

Observe the shoreline profile of Lake Quaker Springs.
No beach sediment is preserved.

Till on your left and the lake clay plain on your right
Till on your left and the lake clay plain on your right with the tops of a few drumlins poking through.

Outwash fan into Lake Albany.
Meltwater flowed between Schuyler and Whelden mountains and deposited an outwash fan into Lake Albany. Minor exposures along the stream to your right (S) reveal gravel overlying clay and basal lodgement till.

STOP 2: Archdale kame moraine.
Exposure of clinoform sand and gravel beds in the moraine. Minor slumping of beds.

STOP 3: Nessle Bros Meats parking lot.
An excellent overview of the Archdale kame moraine deposited against the flank of Herrington Hill. This kame moraine band can be traced southward along the west side of Fly Swamp and across the valley at the southern end of the swamp where a head of outwash is recognized. Return N on WC 74.

Terrace-outwash gravel and sand
Note the terrace-outwash gravel and sand we're crossing with thin till and bedrock uplands to the north. At small rises and around curves in NY 29 till and bedrock are often exposed where the upland thin till and bedrock topography protrudes through the gravel and sand.

Old excavation into a kame ahead on your left.
Note the old excavation into a kame ahead on your left. This is associated with the Battenville moraine.

There is hummocky kamic gravel and sand ahead on your left.
NY 29 used up the till and gravel of the Battenville moraine where the moraine crosses the valley in Battenville.

Flat outwash and terrace gravel and sand
The fairly flat outwash and terrace gravel and sand we're crossing was deposited by meltwater from the ice margin

STOP 4: Tracy Bros excavation.
Horizontally-stratified gravel and sand overlies cross-stratified gravel and sand. Meltwater from the Carter Swamp ice margin deposited this deltaic sediment with sediment sources from the N and E. The Batten Kill has terraced the S end of this deposit.

STOP 5: Lodgement till exposure N side of NY 29.
Both lowland and highland lodgement till facies are similar in Washington County. Why? In contrast, the lodgement till of the Adirondacks is quite different from the Hudson lowland till.

A thick graded gravel bed was observed.
There is an excavation just to your right off of Ferguson Rd where a thick graded gravel bed was observed. How would you describe the sedimentary environment which produced this feature?

Notice the hummocky ice marginal sediment on your left.

Carter's Pond Wildlife Management Area. Lunch Stop.

Smooth rounded drumlinoid topography
Notice the smooth rounded drumlinoid topography developed in these thinly-veneered bedrock highlands.

Argyle sits atop a modest esker delta
The village of Argyle sits atop a modest esker delta deposited into Lake Quaker Springs. Lake clay nearly buried the delta.

STOP 6: Esker gravel and lake clay.
NY 40 rides atop this esker which fed the Argyle delta. Lacustrine clay has partly, and in places completely, buried the esker gravel and sand. Observe the deformed clay and gravel beds here. Is the deformation consistent with what you'd expect from melt-out of buried and/or adjacent ice or would you suggest a minor ice surge after deposition of the clay to account for the stratigraphy? Continue N on NY 40 along the crest of the esker.

STOP 7: Meltwater sediment complex
Harrington Farm excavations expose part of a meltwater sediment complex deposited at the base of the Taconic front along the eastern edge of Tamarack Swamp. The ice tongue responsible for the esker and delta through North Argyle and Argyle stagnated in the swamp. The major meltwater source for this sediment can be traced eastward along Safford Rd. to the town landfill. Coarser gravel and sand, horizontally-bedded and cross stratified, is exposed east of the road. The more distal portion of the delta fan exposed here contains laminated and ripple-laminated sand. A third excavation to the SW in the middle of the swamp contains the most distal and finest-grained sand, silt, and clay beds. The morphology of this last deposit suggests deposition in a tunnel or crevasse in the ice and indicates the rotting ice in Tamarack Swamp was inundated by Lake Quaker Springs.

STOP 8: Outwash gravel and sand in a significant local impoundment.
The north-flowing Mettawee River deposited this outwash gravel and sand in a significant local impondment. The exposed sand, silt, and clay beds accumulated in this Lake Granville whose elevation was approximately 420 ft. Clay is also preserved in the Mettawee valley from Middle Granville westward to Truthville with more silty sediment north of Raceville. There are some concretions in the clay here. Mildly deformed sediment particularly at the north end of the exposure probably resulted from meltout of abandoned ice in the lake. The Hudson ice lobe probably blocked the lower Mettawee valley at Truthville and contained Lake Granville. Retreat of this ice drained the lake and the Mettawee. River deposited its delta into Lake Quaker Springs.

This surface is the top of the Mettawee delta.

STOP 9: Winchell channel overlook.
Park as far off the road as possible and be careful of the traffic! The Winchell channel was one of three channels (the Durkeetown and Ft. Edward are the other two) which carried the outflow of Lake Fort Ann in the Champlain valley through the northern Hudson valley. The present surface stream, Big or Mill Creek, enters the channel from the south through a bedrock gorge (seen as a notch in the distance) and meanders across the channel bottom to Smith's Basin. The channel bottom consists primarily of lake clay while clay, till, and bedrock are all exposed on the flanks of the Winchell channel. This pattern generally holds for the other two channels as well except there is considerably more eroded bedrock along the primary Ft. Edward channel.

Bottom of the broad Durkeetown channel
We're crossing the bottom of the broad Durkeetown channel and will climb up its western escarpment. North-flowing Wood Creek and south-flowing Dead Creek are underfit streams in the bottom of the channel.

We're descending into the Ft. Edward channel.

The canal follows the bottom of the Ft. Edward channel.
Hudson-Champlain canal crossing - the canal follows the bottom of the Ft. Edward channel.

B1: THE NATURE OF THE EASTERN TACONIC CONTACT
PHILIP C. HEWITT
Department of the Earth Sciences
SUNY College at Brockport
Brockport, NY 14420
The purpose of this paper is to provide background information needed for both the full-day trip (A1) and the half-day trip (B1). The full day trip involves data from the entire paper while the half-day trip concentrates on the Taconic Problem primarily. However, to understand either day fully, the entire paper must be read. A separate Road Log for each trip is provided at the end of the paper.
The paper describes geologic features to be examined in area from Saratoga Springs, N.Y. to Manchester, Vt. A discussion and overview of the Taconic region and the "Taconic Problem" will be presented. Consideration will be given to both the sequential and fault hypotheses proposed for the High Taconic region.
The Taconic region is subdivided into the High Taconics and the Low Taconics based on the extreme difference in relief. The High Taconics are the mountains of Vermont, west of the Vermont Valley, with elevations of approximately 3000-4000 ft. The Low Taconics are the hills primarily in New York, west of the High Taconics, with elevations up to approximately 1500 ft. (Hewitt, 1961a). Lithologic and other distinctions will become apparent in the later discussion.

B1: THE NATURE OF THE EASTERN TACONIC CONTACT

STOP 1. Carbonate-Phyllite Contact At Sandgate
The exposure of green phyllite at this locality lies at the axis of a large anticline that lifts the base of the formation structurally. With favorable topography the lower parts of a formation may be exposed as at this locality. In a synclinorium, it is normal to expect that generally, the higher parts of the formations will lie deeper in the earth. When an anticline fortuitously is cut by erosion to expose lower and lower parts of a formation more data become available. In this case, part of the phyllite section responds to hydrochloric acid in a formation that normally has no calcareous beds.
After a general examination of the exposure a study of the lowest part of the formation visible here should be undertaken. This part is located at the southeast end of the outcrop. Note that the base of the exposure appears to be phyllitic and very much like the rest of the rocks here. If cold, dilute hydrochloric acid is applied, the lowest beds will effervesce. Visually one cannot see a difference between those beds that will react with the acid and those that will not. The question that must be asked is "What does this mean?" No other part of the phyllite reacts with acid. Carbonates are known to lie under the phyllite. Therefore, this is probably the contact of the carbonate and green phyllite. The nature of that contact at this locality is for you to decide.
Note also the depression to the south of this outcrop. Two possibilities exist here. The depression may be a combination of structure and topography. That is, the depression might lie in a syncline and therefore lower as a result of structure. This does not appear to be the case here because the anticline passes across the depression. It is also possible that the depression is the result of weathering of a carbonate exposed at the base of the phyllite. Return to cars and proceed southward.

Note folding along road.

STOP 2. Cook Hollow-Exposure Of Contact
It is wise, politic and intelligent to request permission to cross the property here to make the climb. The climb will involve a rise of 1200- 1400 ft. in elevation. Caution is important. Parts of the climb are steep. Some parts are slippery. A slow, steady climb with frequent stops is the best way to see the outcrops and arrive at the contact safely.
Each of the formations mentioned are described briefly in Table 1.
The drive from Rt. 7 crossed the upper Cambrian Danby quartzite and Clarendon Springs formation both of which contain quartzite and dolostone. These formations are not exposed along that traverse. After leaving the cars the traverse begins in the Shelburne marble. Exposures of these strata are best in the creek south of the traverse. It is best to begin the traverse by approaching the creek in order to examine the beds during the climb. However, higher parts of the climb may be difficult or nearly impossible in the creek since this is a landslide area. The easiest climb is on the north (right) side of the creek.
The contact of the Shelburne marble with the overlying Bascom-Beldens formation is at Table Rock. White marble, similar to that of the commercial marble in the Shelburne is also found in the Bascom-Beldens. However, most of the Bascom-Beldens formation is dolomitic marble which is blue-gray to black in color. Near the top of the dolomitic sequence, several hundred feet below the contact with the green phyllite are fossiliferous beds in the marble which contain fossils identical to those at the Covered Bridge on Rt. 313. These indicate an age of medial Ordovician (Trentonian). Beds containing fossils continue across the sequence almost to the contact.
Continued climb will reach a zone of carbonate and phyllite interbeds. Above this zone is a flat area or bench with the contact easily visible. Carbonate ends and the green phyllite continues to the top of Mt. Equinox.
No further description will be presented. It is up to the observer to decide what is seen here. Is this a faulted zone? Where is the fault? Between which strata? Is this a gradational contact? Where does one lithology end and the other begin? How would you describe the bed at the end of the carbonates and the beginning of the green phyllite?
It is up to you.
The descent is probably more difficult than the climb but it is much faster. Be careful.

B7: ROBERTS HILL AND ALBRIGHTS REEFS: FAUNAL AND SEDIMENTARY EVIDENCE FOR AN EASTERN ONONDAGA SEA-LEVEL FLUCTUATION
Thomas H. Wolosz
Center for Earth and Environmental Sciences
SUNY College at Plattsburgh
Plattsburgh, N.v. T2901

B7: ROBERTS HILL AND ALBRIGHTS REEFS: FAUNAL AND SEDIMENTARY EVIDENCE FOR AN EASTERN ONONDAGA SEA-LEVEL FLUCTUATION

STOP 1. Albrights Reef
Park cars along shoulder of road. Main part of reef lies to the right (east). Exposures along road are crinoidal sand/favositid flank deposits. Cliff face about 130 feet to east exposes rugosan constructed Inner Core.

STOP 2. Roberts Hill Reef.
Reef lies to the east of the road and makes up the entire northern portion of the hill. Old logging road marks approximate southern end of reef. Exposures to the west of the road and south of the logging road consist of post-reef growth flanks.
CAUTION: SOLUTION EXPANDED JOINTS ARE COMMON ON THE TOP OF THE HILL AND ARE COMMONLY FILLED WITH LEAVES. PLEASE WATCH YOUR STEP.

B8: DEGLACIATION OF THE MIDDLE MOHAWK AND SACANDAGA VALLEYS, OR A TALE OF TWO TONGUES*
Robert J. Dineen
New York State Geological Survey
The State Education Department
Albany, NY 12230
Eric L. Hanson
Dunn Geoscience Corporation
5 Northway Lane
North Latham, NY 12110
PURPOSE
The middle Mohawk Valley contains a record of the interaction between the Mohawk and Sacandaga glacial lobes, including evidence for several readvances. We will examine exposures in deposits that document these interactions and features.

B8: DEGLACIATION OF THE MIDDLE MOHAWK AND SACANDAGA VALLEYS, OR A TALE OF TWO TONGUES

You are on the Quaker Springs delta.

Kame moraine.

Follow North Street to the right (northeast), along south edge of Interlobate Moraine.

STOP 1: Broadalbin Town Landfill
This pit reveals the products of the ice-marginal environment. Here, the Yosts Readvance reached its maximum extent. The massive basal sands contain dewatering features (flame, dish, ball-and-pillow structures) .. These basal sands are sharply truncated, and overlain by fluvial sand with gravel that contains many reverse graded diamictons (flowtills).
Another pit, 0.4 m (0.7 km) west of Stop 1 shows evidence of more active ice. At this pit, a sequence of trough corssbedded sand is shared and overlain by a thick (1 to 3 m) diamicton.

Proceed along Lake Sacandaga sands to the intersection of NY Routes 29 and 30.

Perth Moraine and Perth Recessional Moraine
The upland that we drove over is the broad platform of the Perth Moraine. The low rise that we cross just before the stoplight is the Perth Recessional Moraine.

STOP 2. Perth Pit
We are on the Perth moraine, in a pit that cuts into the Perth Recessional Moraine. The base of the pit is trough-crossbedded outwash, overlain by 3 m of sand-matrix-supported diamicton. This till is overlain by trough-cross-laminated outwash sand and gravel. Wells nearby indicate that the pit is underlain by 30 to 40 m of interbedded till and sand. The till in this pit probably was deposited by the Yosts Readvance.

The Interlobate Moraine is on the right.
Follow the outlet of Lake Sacandaga to the long access road at the next Stop.

STOP 3. Rex Excavating
This exceptional pit has many instructive exposures. The base of the pit is bluish-gray clayey Mohawk till, overlain by 5 m of laminated fine sand, cut by trough-cross bedded sand and gravel. The sand and gravel is capped by 2 m of weathered till that is overlain by another sequence of lacustrine sand and prograding outwash. Till overlies this outwash, and is interbedded with lacustrine sand.
The multiple tills are the products of at least two readvances. The soil zone between the major sequences suggest several thousand years separated the two advances. Both sequences involved glacial ice overriding proglacial lacustrine and outwash deposits. The several tills above the soil zone probably were mudflows and lodgement tills of the Yosts Readvance. A similar exposure lies 1.1 miles to the east.

Cross the Cayadutta Spillway.

STOP 4. Twin Cities Sand and Gravel
This immense pit is over 300 m long and 7 m high.
It is the distal portion of the Interlobate Moraine, and contains distinct deltaic features. Both thrust and gravity faults are common, especially on the eastern end of the pit. A sandy diamicton caps the sandy deltaic sequence. Aeolian sand unconformably overlies the sandy till on the eastern end of the pit.

Drive up ice-contact slope and onto delta
Drive up ice-contact slope of the Interlobate Moraine and onto the Lake Gloversville delta.

Nice drumlins to the west, the Interlobate Moraine dominates the skyline to the southeast.

STOP 5. Mayfield Pits
This complex of pits is developed in an esker that drained the Sacandaga ice tongue. A subaqueous sand and gravel fan lies at the mouth of this esker. It was built by meltwater flowing in an ice tunnel into Lake Sacandaga. The esker is interbedded with lake sand.