NYSGA 1961
GUIDEBOOK TO FIELD TRIPS
NEW YORK STATE GEOLOGICAL ASSOCIATION
33rd Annual Meeting
Robert G. laFleur
Editor
Contributing Authors
James R. Dunn
Donald W. Fisher
Philip C. Hewitt
Shepard W. Lowman
Lawrence V. Rickard
Host
RENSSELAER POLYTECHNIC INSTITUTE
Troy, N. Y.

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

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

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

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

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

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

STOP 2e. Esker along Vlockie Kill

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

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

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

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

STOP 3d. Solitary kame

STOP 3e. Solitary Kame

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

STOP 2D.

STOP 2E. North side of Beman Park

STOP 2F. Dunn Garden Apartments.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

STOP 3. Eastward dipping Stockbridge carbonates

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

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

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

STOP 7. "Berkshire" black phyllite.

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

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

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

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

STOP 12. Balmville Limestone thrust on Walloomsac Slate

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

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

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

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

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

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

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

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

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

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

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