Contains all the trips from these eleven guidebooks, with a folder for each trip.

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).

Trip 1A

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.

Trip 1B

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.

Trip 2

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

Trip 3A

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.

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

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

NYSGA 1957 Trip A-1

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

NYSGA 1957 Trip B

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.

NYSGA 1957 Trip D

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

NYSGA 1957 Trip E

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.

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

Trip 1

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

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.

Trip 3

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
The City College
Trips 4-B and 4E.

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

Trip C

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

Trip D

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.

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

1959 trip A

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

1959 trip B

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

1959 trip C

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.

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.

Trip A

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.

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).

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.

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.

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.

NYSGA 1962 Trip A

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.

NYSGA 1962 Trip B

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.

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).

NYSGA 1962 Trip C

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.

NYSGA 1962 Trip D

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/

A: UPPER DEVONIAN STRATIGRAPHY AND SEDIMENTOLOGY IN THE BINGHAMTON AREA
James E. Sorauf and Herman E. Roberson
Department of Geology
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

Trip B Path

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

Trip C Path

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 Cyrtospirifer sp. 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

Trip D Path

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.

Bainbridge
Bainbridge is built on the 1010' terrace. Susquehanna River is 975!

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...

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

NYSGA 1964 Trip B

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

NYSGA 1964 Trip C

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

1964 Trip D
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

NYSGA 1964 Trip E

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.

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

Trip 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

Trip 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
Department of Geology
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
by
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

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

1966 trip A

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

1966 Trip B

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

1966 Trip C

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
State University of New York at Buffalo

1966 Trip D

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

1966 Trip E

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.