NYSGA 1984
NEW YORK STATE GEOLOGICAL ASSOCIATION
56th Annual Meeting
FIELD TRIP GUIDEBOOK
Donald B. Potter, Editor
Department of Geology
Hamilton College
Clinton, New York 13323
Printed at Hamilton College for the New York State Geological Association. Additional copies may be obtained from the permanent Executive Secretary, Fred Wolff, Department of Geology, Hofstra University, Hempstead, NY 11550

AB2a: CROSS SECTION OF THE LOON POND SYNCLINE, TUPPER LAKE QUADRANGLE, NEW YORK
D. B. Potter, Jr.
Department of Forestry and Geology
University of the South
Sewanee, TN
INTRODUCTION
This field trip crosses the Loon Pond Syncline, an area mapped during the summers of 1978, 1979, and 1980 under the direction of Leo Hall at the University of Massachusetts. The syncline, a northeast-trending elongate basin, was named and first mapped by Buddington and Leonard (1962) as the northeast part of the Bog River Synclinorium (Figure 1).
The syncline occupies most of the southern half of the fifteen minute upper Lake Quadrangle, which lies in the central Adirondacks within the Adirondack Highlands region. The Arab Mt. Anticline, composed of charnockitic gneisses, lies to the north, and the Salmon Lake Anticline lies to the south (Figure 1).
The stratigraphy of the syncline is distinctive. In contrast to most of the Adirondack Highland rocks which are chiefly orthogneisses and anorthosite, a great deal of quartzite, marble, and calc-silicate rock as well as quartzo-feldspathic gneisses constitute the rocks here. In this respect the rocks of the Loon Pond area are similar to those of the Northwest Lowlands (Figure 1). Erosion of the multiply deformed rocks has exposed a structural basin which shows some similarity to the Darning Needle Syncline in the Cranberry Lake Quadrangle (Leavell, 1977).
Access: Route 10, linked to Route 30 by Route IDA, extends west across the field area to the old Sabattis Railroad station and provides the primary access to the sparsely populated region (Figure 2). With the exception of a clear area south of Sabattis that burned in 1903, the region is heavily wooded. Topographic relief is about 800 feet.

AB2: CROSS SECTION OF THE LOON POND SYNCLINE, TUPPER LAKE QUADRANGLE, NEW YORK

View of Loon Pond Mountain to the northwest.

Small outcrops of East Charley Pond Gneiss on both sides the road.

Cross bridge at the head of Little Tupper Lake.

STOP 1. Otter Pond Dioritic Gneiss
Otter Pond Dioritic Gneiss is exposed along the north side of the road. Near the east end of the outcrop, a late 1 meter-thick vertical dike cuts the foliated gneiss. Discontinuous quartz veins help define the edges of the northtrending dioritic dike.
Estimated modes from thin sections of the foliated gneiss at this outcrop (646) and one .3 miles east (647) follow:
| 646 | 647
Quartz | 1 | 12
Plagioclase | 71 | 43
Biotite | - | 1
Augite | 13 | -
Hornblende | 10 | 36
Apatite | tr. | tr.
Zircon | 1 | tr.
Magnetite and Ilmenite | 4 | 8
Foliation is N84W,24SW and parallels foliation in basement rocks to the south. The outcrop was mapped by Buddington and Leonard (1962) as a diorite gneiss, but they did not consider the unit to be as widespread as is shown in Figure 2.

STOP 2. Sabattis Road Member of the Lost Pond Marble
The Sabattis Road Member of the Lost Pond Marble is exposed on the north side of the road. Most of the outcrop consists of brown-to gray-weathering marble beds up to 2 m thick. A few layers of quartzite, .5 m thick, are also present. The graphitic marble includes quartz, microcline, pale green diopside, phlogopite, calcite, sphene, and scapolite. The quartz and diopside stand out as small knobs and clusters on the weathered surface.
F2 fold axes plunge S45W at about 10 degrees, and minor undulations in bedding define a pronounced lineation in places.

STOP 3. Bear Pond Gneiss
The Bear Pond Gneiss is exposed along the northwest shore of Bear Pond. Layering and foliation strike northeast, parallel to the trend of the pond, and dip southeast beneath the Lost Pond Marble of STOP 2. Grain size in the magnetitebiotite-quartz-microcline gneiss varies from fine to pegmatitic.
A biotite-rich unit of the Bear Pond Gneiss lies on the north side of the road .1 mile west of Bear Pond. The gneiss is cut by a coarse microcline pegmatite body that is roughly concordant to foliation.
Near the crest of the hill .2 miles west of Bear Pond a third example of the Bear Pond Gneiss is exposed. The rock is a gneiss. Locally, both sillimanite and coarse garnet constitute more than 10% of the rock. A strong F2 sillimanite lineation plunges S46W at 4 degrees. Garnet distribution in this "chicken pox" rock is locally random, but in some places the garnet is concentrated in layers parallel to foliation.

Swamp to north is underlain by Lost Pond Marble.

Bear Pond Gneiss exposed on left side of road.

STOP 4. Bear Pond Gneiss
This area is not generally accessible to the public. Beginning at the southwest corner of the log landing, walk 400 yards at S40W across uneven terrain to the outlet of a small pond. Here the Bear Pond Gneiss is exposed in the axial region of a map-scale F2 syncline. Both limbs strike NE and dip SE. Many minor structures exposed along the outlet illustrate the second phase of deformation. Fold axes and mineral lineations form a tight southwest-plunging concentration on an equal area net. If water levels permit, a faint F3 magnetite lineation will be seen.
The Loon Pond Dioritic Gneiss is exposed on the other side of the outlet .1 mile southwest along the edge of the pond.

Bear Pond Gneiss on south side of road.

Abandoned Sabattis Railroad Station.
Turn around and return to Little Tupper Lake.

STOP 5. Overgrown quarry on west side of road.
The old quarry is in the Bog River Member of the Lost Pond Marble and contains graphite, calcite, sphere, phlogopite, quartz, calcite, and diopside. Diopside varies in color from pale to dark green and locally forms more than 50% of the rock. The rock is moderately well to poorly foliated, and grain size varies from medium to coarse. There is great variation in the relative proportions of calcite and quartz in the rock. Rocks at this location bear a strong resemblance to the diopsidic marbles of the Sabattis Road Member of the Lost Pond Marble (Stop 2).

AB2b: BEDROCK GEOLOGY OF THE GRAMPUS LAKE AREA, LONG LAKE QUADRANGLE, NEW YORK
Page Fallon
Department of Geology and Geography
University of Massachusetts
Amherst, MA
INTRODUCTION
What follows is a brief description of the geology of the Grampus Lake area. These are the preliminary results of a study conducted under the guidance of Professor Leo M. Hall at the University of Massachusetts. The map area lies in the southwest part of the Long Lake quadrangle and includes a portion of the southeast corner of the Tupper Lake quadrangle (see Figure 1). Previous work in the area was done by Cushing (1907) in the Long Lake quadrangle and Buddington and Leonard (1962) in the Tupper Lake quadrangle.

AB2b: BEDROCK GEOLOGY OF THE GRAMPUS LAKE AREA, LONG LAKE QUADRANGLE, NEW YORK

STOP 1. Buck Mountain Fold Complex
This stop offers the opportunity to see the diopside augen quartz gneiss and other quartz rich gneisses and well exposed examples of second and third phase folds.
Road Cuts: Glassy quartzites and diopside augen quartz gneiss with small sparse diopside augen are exposed on the western side of Route 30. The small outcrop on the eastern side of the highway contains a few large dark green diopside porphyroblasts.
1-A.) Buck Mountain Syncline. Walk east from the highway 600 feet down the logging road. Bear left at a small cabin onto an overgrown skidder trail. Walk 1000 feet approximately N45E along a contour. The outcrop on the steep slope to the southeast exposes the hinge of the Buck Mountain Syncline, a large third phase fold, (see figs. 8 and 9). This is a tight fold which plunges moderately to the southeast on a northwest trending, steeply south dipping axial surface.
I-B.) Proceed west from the highway on an overgrown trail from the south end of the western road cut for about 1000 feet. Turn north and climb the hill to a large pavement outcrop.
The rock is typical diopside augen quartz gneiss. The augen which have weathered out, giving the rock this distinctive texture, are large single crystals or aggregates of smaller grains of green to white diopside. Scapolite is common. Minor K-feldspar, and traces of calcite, sphene, and zoisite are present.
A second phase isoclinal fold, outlined by a thin amphibolite, is refolded by a tight third phase fold, forming a hook interference pattern. Note the lack of an axial plane foliation in the hinge of the second phase fold. A more prominent axial plane feature is present in the hinges of third phase folds. Other folds, and a nice view to the south, are visible higher on the hill.

STOP 2. Rock Pond Syncline
The low outcrop to the left is a buff weathering diopside granulite which contains, in addition to diopside, calcite, plagioclase, and minor microperthite and quartz. Sulfides are present and graphite is abundant.
The structure of this area is poorly understood. The Rock Pond syncline closes around the calcsilicate gneisses just to the northwest. Refolding in the third phase produced north-side up folds (see fig. 4, Section E-F). The inappropriate rotation sense of the third phase fold is attributed to original curvature of the hinge line of the Rock Pond Syncline. Late folding about northwest trending axial surfaces causes local changes in the direction of plunge of the third phase fold.

AB2c: A TRAVERSE ACROSS THE SOUTHERN CONTACT OF THE MARCY ANORTHOSITE MASSIF, SANTANONI QUADRANGLE, NEW YORK
Paul Ollila
Department of Geology
Vassar College
Poughkeepsie, NY 12601
INTRODUCTION
The 15' Santanoni quadrangle is located between 44°00' and 44°15' north latitude and 74°00' and 74°15' west longitude in what is known as the High Peaks region of the Adirondack Mountains of New York State (Figure 1). The nearest towns of any size are Lake Placid, which is northeast of the quadrangle, and Saranac Lake, which is north of the quadrangle (Figure 2).
Approximately 80% of the quadrangle is underlain by anorthosite or anorthosite-related rocks. The remainder of the area is underlain by pyroxene syenite gneisses (commonly ascribed to a mangerite-charnockite series), amphibolites, granitic, pelitic and calc-silicate gneisses, marbles and quartzites. All of these rocks have been affected by the approximately one billion year old Grenville metamorphism and form the southeastern part of the Grenville province of the Canadian shield. Bedrock geologic mapping of the Santanoni quadrangle at a scale of 1:62 500 was carried out between 1978 and 1982 under the direction of Howard Jaffe from the University of Massachusetts.
AB-2

AB2c: A TRAVERSE ACROSS THE SOUTHERN CONTACT OF THE MARCY ANORTHOSITE MASSIF, SANTANONI QUADRANGLE, NEW YORK

STOP 1 Gooseberry Mountain Gneiss
The Gooseberry Mountain Gneiss consists of pink-weathering, medium-grained granitic gneiss, black-and white-weathering amphibolites that average 1 m in thickness and gray-weathering layers 1 to 3 mm thick rich in sillimanite, biotite and quartz. Sillimanite gneisses are the key to identifying the Gooseberry Mountain gneiss. Other rocks included within this unit are quite similar to rocks included in the Moose Mountain Gneiss.
Sillimanite gneisses form only a small part of the unit but have been found on the north side of Gooseberry Mountain, on the southern end of a hill just east of Deer Pond, and on the southwestern side of Gooseberry Mountain in the Long Lake quadrangle.
North of Gooseberry Mountain, zones characterized by abundant sillimanite rich layers occur within pink granite gneiss. Within these zones, sillimanite-rich layers are separated by 1 to 2 cm layers of quartz and pink microperthite augen. Granitic gneiss within the Gooseberry Mountain gneiss is typically composed of anhedral quartz, and microperthite, brown biotite, magnetite, and may contain green hornblende and orthopyroxene. Sample 17-1 (Table 1) is fairly representative except that the granitic gneisses commonly contain higher modal proportions of magnetite. Average grain size is 1 to 2 mm and foliation is defined by oriented biotite. Sillimanite rich layers and amphibolite layers parallel foliation. Both weathered and broken surfaces of granitic gneiss are pink to brown. Locally the granite gneiss is garnetiferous and garnetiferous granitic pegmatites are fairly abundant on the southwest side of Gooseberry Mountain.
Amphibolite layers are abundant at low elevations on the northern side of Gooseberry Mountain and also north of Deer Pond in the Long Lake quadrangle. The amphibolites are medium-grained but range in texture from well-foliated to granular. They are black-and white-weathering and typically have a color index near 50. Hornblende and plagioclase are the dominant minerals but amphibolites also contain brown biotite, orthopyroxene and oxides. Both garnetiferous and non-garnetiferous varieties have been observed. At location 17-22, granitic gneiss and amphibolite layers average 1 m in thickness and granitic gneiss forms about 60% of the outcrop. Going south from this location, the amount of amphibolite decreases, until near the summit of Gooseberry Mountain, the rock is almost entirely granitic gneiss. This sequence is reversed down the south side of Gooseberry Mountain. This repetition, and the occurrence of sillimanite gneisses on the north and south side of Gooseberry Mountain, suggest that this unit has been doubled by folding.

STOP 2 Moose Pond Formation-Ymp
The Moose Pond formation is extremely poorly exposed. One probably loose block of coarse-grained calcite marble (sample 17-6, Table 2) is located at the south end of Moose Pond. A mixture of rusty-brown medium-to-fine-grained diopside-quartz-microperthite granulites (17-7, Table 2) and fine-grained biotite-quartz-microperthite gneisses crops out along the western shore of Moose Pond at location 17-7. Although there is abundant quartzite and diopsidic quartzite float northwest of Shaw Pond a nearby outcrop northwest of Shaw Pond contains only a few thin diopside-rich layers. Most of the rock at this location is a medium-to fine-grained brown augite-biotite-quartz-plagioclase-microperthite gneiss.
No outcrops were observed in the region between Gooseberry Mountain and Wolf Pond Mountain. The Moose Pond marble is inferred to go through this region on the basis of topography and the geometry of folds in the Moose Mountain gneiss and the Gooseberry Mountain Gneiss. The aeromagnetic map (1978) shows a magnetic low east of Gooseberry Mountain which is consistent with the presence of marble in this valley. Mineral assemblages in rocks from the Moose Pond marble are listed in Table 2.

STOP 3 Calcareous Quartzites of the Moose Pond Formation.
These rocks contain quartz, diopside, calcite, sphene, microcline and scapolite. The scapolite is partially altered to prehnite.
The dominant foliation in these rocks trends 276°, 26 S and a strong lineation defined by trains of diopside trends 213°, 20°.
The rotation sense of minor folds at this outcrop indicates south side down movement.

STOP 4. Mylonitic pyroxene quartz syenite gneiss.
This rock is more intensely foliated and finer grained than normal for pyroxene quartz syenite gneiss. Foliation trends 90°, 35 S and locally a strong lineation defined by quartz ribbons trends 222°, 25°. A few asymmetric augen and what are possibly S and C foliations (Berthe et al. 1979, Simpson and Schmid, 1984) suggest south side down movement.
The mineralogy of pyroxene quartz syenite gneiss along Ermine Brook is typical of pyroxene quartz syenite gneiss found elsewhere in the quadrangle. Modes of typical pyroxene quartz syenite gneisses are listed in Table 3.

STOP 5 Gabbroic Anorthosite Gneiss (Ygag)
The gabbroic anorthosite, gneiss map unit trends NW-SE in a zone across the southwestern corner of the quadrangle (Figure 3). It lies between metamorphosed sedimentary and igneous rocks to the southwest and anorthosite to the northeast. The dominant rock type within the unit has a color index (C.I.) equivalent to gabbroic anorthosite but minor amounts of gneissic anorthosite, noritic anorthosite, gabbro, and syenite are included as well. Forty-four samples from the gabbroic anorthosite gneiss map unit were examined in index of refraction oils or in thin-section. Of these 27 have a C. I. equivalent to gabbroic anorthosite, 7 are monzonites, 5 are anorthosites, 2 are gabbros, 1 is noritic anorthosite and 1 is a quartz syenite. The syenitic rocks and the gabbros generally occur as concordant layers or sills. Most of the rock in the unit has a composition similar to gabbroic anorthosite except that it contains more garnet, hornblende, alkali feldspar and quartz. Modes of four samples of gabbroic anorthosite gneiss (Table 4) are representative of the amount of hornblende, garnet, K-feldspar, and quartz typically found in these rocks. Orthopyroxene, although present in all four modes, is not commonly present in anorthosite gneiss. At this locality pyroxene is commonly rimmed by hornblende which locally defines a strong lineation that trends 225°, 24°.
Rock at this locality is heterogeneous, consisting of gabbroic anorthosite gneiss with lesser amounts of gabbro, anorthosite, and syenitic gneiss. This is a good area to look at both intrusive relationships between the different rock types and the intense deformation typical of gabbroic anorthosite gneiss. Note also the different response of the various rock types to deformation.

STOP 6 Anorthosite.
This anorthosite is typical of anorthosite in much of the interior of massif. This rock is probably part of a layer or large xenolith of anorthosite in the gabbroic anorthosite gneiss map unit. More gabbroic anorthosite gneiss crops out to the north along the other branch of Ermine Brook and on Little Santanoni Mountain.

BC3: FORELAND BASIN SEDIMENTATION IN THE TRENTON GROUP OF CENTRAL NEW YORK
C. J. Mehrtens
Department of Geology
University of Vermont
Burlington, Vt. 05405
Purpose
The purpose of this field trip is to re-examine several of the well-known exposures of the Trenton Group in the Mohawk Valley. This re-examination is necessary due to the recent reinterpretations of the depo-tectonic setting and sedimentology of these units. Specifically, the Trenton Group in central New York has been redefined as a foreland basin and a tectonically active shelf edge/trench slope environment (Cisne, et al., 1982). The sedimentology of the Trenton Group has been shown (Mehrtens, in review) to evolve from in situ carbonates to dominantly turbiditic in nature. This field trip will visit several localities where participants will be able to view: (1) variations in the thickness of units over short lateral distances; (2) rapid facies changes within individual stratigraphic sequences; (3) syn-depositional slump fold horizons; (4) internal structures within limestone beds, identifiable as Bouma sequences. These features are all characteristic of sedimentation in the tectonically active foreland basin. The text for this field trip will review the stratigraphic model presented by Cisne and Rabe (1978) and Cisne, et al (1982). Evidence for the interpretation of the limestone and shale couplets of the Denley Limestone and Dolgeville Facies as bioclastic turbidites will also be reviewed. Previous interpretations of the Trenton Group depo-tectonic setting will be presented and compared to the foreland basin model. It is hoped that this field trip will demonstrate, if nothing else, the strong role that a model or paradigm can play in the interpretation of stratigraphic sequences.

BC3: FORELAND BASIN SEDIMENTATION IN THE TRENTON GROUP OF CENTRAL NEW YORK

Pass lower portion of City Brook on right.

STOP 1. Buttermilk Creek
Park immediately beyond the bridge and descend to Buttermilk Creek. The section downstream of the bridge is part of the Black River Group (Gull River), consisting of calcareous limestone. Underneath the bridge and a short distance upstream are ledges of coarsely crystalline limestone alternating with massive calcareous sandstone beds. These are the lagoonal sediments of the Napanee and Selby Limestones. These rocks have been described by Titus and Cameron (1976) and are characterized by their aphanitic texture, birdseye structures, massive bedding, and disseminated quartz sand. This facies continues in a series of benches going upstream. The contact of the Napanee and Selby with the Kings Falls occurs immediately above the pool below the first waterfall. The Kings Falls is differentiated from the underlying facies by the first appearance of fossiliferous calcarenites that are thinner bedded and exhibit lateral thickening and thinning of individual beds. The Kings Falls continues upstream to the larger waterfall, consisting of beds of calcarenite and bioturbated calcilutite. The lateral lensing of the beds, so characteristic of the Kings Falls is readily visible.
While at this stop you should: (1) examine the Napanee and Selby (lagoonal) facies as this is the only stop where they will be seen on this trip; (2) examine the Kings Falls, noting in particular the features which may suggest that it accumulated near wave base. Are there any internal structures within the limestone beds? How much shale, if any, is present? Are the beds laterally continuous? How frequent was bioturbation? Where are the fossils within limestone beds or on bedding planes?

STOP 2 City Brook
After disembarking from the cars, descend to City Brook upstream of the bridge. The section downstream is one of the most beautiful exposures of the Black River, Selby, Napanee and Kings Falls Limestones in the Mohawk Valley but is off limits. Under the bridge, and continuing up section, are small benches of the Sugar River Limestone. These bedding planes are distinguished by their abundant Prasopora colonies, along with the typical Sugar River benthic fauna described in Titus and Cameron (1976). Compare the Sugar River Limestone to the Kings Falls Limestone seen at STOP 1. How does it differ? What is the evidence that it might have accumulated at slightly deeper depths? How laterally continuous are these beds? Do they exhibit the same degree of lateral lensing? Is there a change in the relative percentage of calcarenite versus calcilutite beds? The contact of the Sugar River and the Denley Limestones occurs in the small waterfall. The basal Denley seen here is similar to the basal Denley seen at the next stop (Shedd Brook) but is very different than the basal Denley at Trenton Falls Gorge.
Here the Denley is much less fossiliferous and much finer-grained. Note the nodular limestone bedding. Bedding planes are not littered with fauna, except for an occasional trilobite and cephalopod. Continuing up the stepped benches note the abundance of calcilutite, mostly all barren. The dominant two lithologies of the Denley here are: (1) a barren calcilutite with planar bottoms and reworked (bioturbated) tops and (2) a nodular, more argillaceous calcilutite. These lithologies continue upstream until the waterfall is reached. Here, on the cliffs above the stream, the contact with the overlying Dolgeville Facies is seen. The Dolgeville is characterized by the interbedded planar calcilutite with thick interbeds of shale (see Figure 15). This City Brook section is interesting because it records a very rapid, nongradational facies change in the Sugar River/Denley contact. It also is unusual in that the Denley here is such a deep water deposit. Examination of the limestone beds reveals a dominance of planar laminations interpreted as Td and structureless, bioturbated micrite interpreted as Td'. While at this stop you should ponder the nature of the facies change from the Sugar River to Denley. Do you think it's the result of lateral facies mosaicing accompanying gradual transgression, or, could it be the result of a rapid drop of the fault block, drowning the shelf?

STOP 3. Shedd Brook
After parking at the top of the hill, cross the road and descend to the stream bed. Walk down to the base of the section. Exposed at the base of Shedd Brook is the upper Kings Falls Limestone. It should look similar to the upper part of the section at Buttermilk Creek, that is, coarse calcarenite to calcirudite beds which exhibit lensing. All of the Sugar River Limestone is exposed in this stream cut, and comparisons can be made between the Kings Falls and Sugar River. Study the Sugar River lithologies and bedding styles to draw some conclusion about environment of deposition relative to wave base. This is an important point because the Sugar River is interpreted to represent "normal" carbonate accumulation below wave base. If this is what "normal" below-wave base sedimentation looks like, what interpretations can be made about the overlying Denley Limestone? The contact of the Sugar River and the Denley Limestone occurs at the top of the waterfall. Examine the upper horizons of the Sugar River. Note the abundance of relatively unfossiliferous calcilutite beds with shale interbeds. How gradational are the Kings Falls to lower Sugar River to uppermost Sugar River facies? The top of the waterfall represents the last of the fossiliferous calcilutite and calcarenite beds in this section. The percentage of interbedded shale is also increasing. A bentonite horizon is present in the bushes on the left side of the stream. There is a long bench in the stream bed of the nodular barren calcilutite beds with thick shale interbeds of the Denley Limestone. This should look similar to the Denley seen at the previous stop. Up stream at the bend in the brook, Dolgeville beds of planar calcilutite and shale are seen. Passing under the road you continue to walk on nodular bedded, calcilutite horizons of the Denley Limestone. About 50 feet above the road on the right side of the stream, there is a small exposure of interbedded nodular calcilutite and planar calcilutite beds with bioturbated tops, also of the Denley Limestone. Two more bentonite horizons are located in this small cliff. The stratigraphic section seen along Shedd Brook is very similar to that in City Brook but it is worth walking this section to demonstrate: (1) the gradational Kings Falls to Sugar River section; (2) interbedded bentonite horizons.

West Canada Creek on right, access to Trenton Falls Gorge is ahead.

STOP 4. Prospect
(needs special permission from Niagara Mohawk Power Corp.)
After parking the cars across the bridge, descend the cliff to West Canada Creek carefully. Standing on the bedding plane above the creek, turn around and examine the cliff face. A prominent slump fold horizon is visible (Figure 16). Note that the slump fold can be traced laterally to an undisrupted horizon of calcarenite. The nose of the fold is characterized by brecciated clasts of limestone so the sediment was fairly lithified at the time of emplacement. Paleoslope measurements on this and other slope indicators (aligned fossils) indicate a paleoslope of S80E (Cisne and Rabe, 1978). Note the sediment in which the slumping occurred. This is the Denley Limestone, but a very different Denley than what has been seen at Stops 2 and 3. Note how fossiliferous some of the calcarenite and calcirudite beds are. The strophomenid Rafinesquina is especially abundant, as is Prasopora. Interbedded with this fossiliferous facies of the Denley are lithologies we have already seen: nodular, bioturbated calcilutite and calcilutite with planar bases and bioturbated tops (Td'). Also present are beds of graded skeletal debris (Ta), and horizontally laminated skeletal debris (Tb). Looking upstream a wide waterfall can be seen and individual beds can be traced across this exposure. Beds which exhibit this degree of lateral continuity, with negligible change in thickness could not have accumulated near wave base.

STOP 5. Dolgeville
This stop along East Canada Creek in Dolgeville is made for examination of the basinal shales. Parking on the hill and descending to the stream below the dam, the calcareous turbidites and interbedded shale horizons of the Utica shale are exposed. The calcareous turbidites are identifiable by their buff yellow weathering. Tc and Td horizons are the only Bouma Units present. The thick shale interbeds contain numerous good graptolites. Based on the Bouma Units present within the turbidite horizons and the thickness of the inter-turbidite deposits, it is possible to interpret this section as representing a distal turbidite facies. The source of the calcareous horizons is the foundered shelf (Dolgeville Facies) inter-tonguing with the basinal terrigenous muds. Continuing down to the pool at the base of the waterfall, drag folds associated with the Little Falls Fault are visible.

STOP 6. Canajoharie Creek
Descend to the creek from the parking lot. The creek bed is Chuctanunda Creek Dolostone of Lower Ordovician age. The lower cliff face contains the unconformity between this dolostone and the interbedded limestone and shales of the Kings Falls Limestone. Looking up the cliff the Kings Falls is overlain by the Canajoharie Shale (Figure 15). In other words, all of the Lower Trenton is missing, with the exception of a thin section (15 feet) of Kings Falls, and all of the upper Trenton is missing. Cameron (1971) described this section of limestone as Sugar River, but noted that it represents a shallower water environment than the Sugar River seen to the northwest (Stops 2 and 3). This unit can be better described not by the fossil assemblage it contains, but by the lithofacies present. The bedding style is identical to that of the Kings Falls seen earlier: laterally discontinuous beds exhibiting lensing and cross laminations. Looking at this section you can ask yourself: How can wave-reworked limestones and basinal shales be juxtaposed with no intervening deeper water limestones? Why are there no lower Trenton units between the Kings Falls and the Lower Ordovician dolomites? Do these abrupt facies changes represent lateral mosaicing produced by sea level changes or does it seem more probable that movement on a syndepositional block fault could generate this type of sequence?

STOP 7. Caroga Creek
After parking, descend to the creek below the bridge under Route 5. The section below the bridge and downstream are undifferentiated Black River deposits. Depending on the height of the stream, variable amounts of rock are exposed here. At low stage, aphanitic dolostones with birdseye structures are visible. The section between the two bridges has many covered intervals but ledges of coarsely crystalline limestone outcrop and are interpreted as Kings Falls. Under the second bridge ledges of laminated calcarenites outcrop, exhibiting planar tops and bottoms and lacking fossils. Upstream of these are beds of the bioturbated, barren calcilutites,. These last two lithologies are characteristic of the Denley Limestone as seen on City and Shedd Brooks.
A covered interval occurs above this and below the cliff with Utica Shale. This section then, is another thinned section of Trenton. Both the lower Trenton and upper Trenton units are missing or greatly reduced in thickness. Because the quality of this exposure is not equal to that at Canajoharie Creek, it is not as spectacular, but the significance of the facies changes is equally important. Note that as one progressed east for the last two outcrops, the magnitude of the variation in stratigraphic sections became more significant. This is in keeping with our moving further into the foreland basin from the stable shelf represented in the earlier outcrops.

BC4: ANIMAL-SEDIMENT RELATIONSHIPS IN MIDDLE ORDOVICIAN HABITATS
David W. Larson
Hamilton College
Clinton, New York 13323
In recent years a number of workers have presented arguments to suggest that utilization of infaunal life strategies by marine organisms has varied through the Paleozoic. Evidence for a progressive "infaunalization" of Paleozoic communities comes from functional analysis of trace fossils (Seilacher, 1977), patterns of taxonomic richness of skeletonized bioturbating organisms (Thayer 1979, 1983), and the sedimentary record of the effects of burrowing organisms (Garrett, 1970; Sepkoski, 1982; Larson and Rhoads, 1983). Between the Middle Ordovician and Early Devonian, it seems that the depth of biogenic reworking of sediment in marine shelf settings increased from essentially zero to over 5 cm. Exploitation of buried food resources by deposit-feeders propels this infaunal invasion (Larson and Rhoads, 1983). Miller and Byers (1984) present an opposing view, that infauna are abundant and diverse throughout the early Paleozoic. At present, there is no consensus as to the style and degree of biogenic reworking in the early Paleozoic.
This field trip is meant to provide an opportunity to examine some of the evidence that has convinced me that biogenic reworking in Ordovician sedimentary environments was much reduced in comparison to recent counterparts. We will visit a series of four outcrops of Middle Ordovician carbonate rocks in the Black River Valley of northwestern New York (Figure 1). Our trip will take us on a transect of facies from the intertidal carbonates of the Black River Group through a range of shallow to deep shelf and basinal environments in the Trenton Group. The goal is to examine Ordovician animal-sediment relationships and their sedimentologic and paleoecologic implications.

BC4: ANIMAL-SEDIMENT RELATIONSHIPS IN MIDDLE ORDOVICIAN HABITATS

Bridge across Sugar River.
Upstream is an excellent exposure of the limestones in the lower portion of the Trenton Group. The quarry on the right side of the highway is in the Black River Group. Downstream, solution cavities and channels in the Black River Group cause subsurface drainage of Sugar River. At low discharge all of Sugar River disappears into the stream bed.

STOP 1. Road cuts in the Black River Group
Road cuts in the Black River Group on north and south side of Turin Road.
The Black River Group is a well documented example of tidally influenced carbonate deposition. This discussion of the stratigraphy and sedimentology of the Black River Group is largely drawn from Walker (1973) and Walker and Laporte (1970).
Here the Black River Group is divided into three formations:
Chaumont Formation: burrowed, fossiliferous wackestone.
Lowville Formation: fenestral, laminated mudstone, wackestone, and packstone.
Pamelia Formation: dolostone and dolomitic sandstone.
The sequence Pamelia/Lowville/Chaumont is interpreted by Walker (1973) to record the progressive transgression of the Middle Ordovician sea onto an eroded Grenville terrane. From base to top the Black River Group records the transition from supratidal to intertidal to shallow subtidal conditions.
The Lowville Formation includes a number of sedimentologic features indicative of an intertidal origin: mudcracks, fenestral fabric, and algal laminations. In addition, oolites, intraformational conglomerates, and fragmented mounds of Tetradium indicate vigorous stirring of the bottom.
The Chaumont Formation contains fewer sedimentologic criteria on which to base an environmental interpretation. Walker (1973) bases his assignment of the Chaumont to the shallow subtidal on the presence of brachiopods and bryozoa in the Chaumont and the interbedding of Lowville and Chaumont lithologies.
A striking feature of the outcrop is the contrast in sedimentary fabrics between the Lowville and Chaumont Formations. Burrows are rare in the Lowville. The sedimentary structures that permit such a straight-forward facies assignment are barely altered by biogenic reworking. Chaumont sedimentary fabrics on the other hand are dominated by burrows. In many cases the outlines of individual burrows are distinct; in others, the burrow outlines are diffuse. Importantly, other than laterally discontinuous bedding units, the biogenic structures have very nearly obliterated the depositional features. This style of bioturbation is characteristic of deposit-feeding communities (Rhoads and Young, 1970; also Rhoads and Boyer, 1982).
Here then we are able to see that for these Ordovician habitats, like their recent counterparts, the effects of bioturbation increase in an offshore direction. A deposit-feeding community was clearly active in this shallow subtidal setting.

STOP 2. Steuben Limestone of the Trenton Group.
Abandoned railroad cut through the Steuben Limestone of the Trenton Group. From this vantage point you can see the Tug Hill Plateau, underlain by the Utica Shale and Lorraine Group, to the west. To the east across the Black River Valley are Grenville rocks of the Adirondacks.
At this exposure we will examine a ten meter section of the Steuben Limestone (Figure 6). About 40 cm of Hillier Limestone is exposed at the top of this cut. We will see a much thicker section of the Hillier at Stop 4.
The Steuben Limestone is generally a thickly bedded fossiliferous packstone with some important variations in lithology. Near the base of the exposure, fossiliferous mudstones and wackestones are interbedded with centimeter thick argillaceous mudstones. Both grain size and bed thickness increases upward through the Steuben. Midway through the section are cross-laminated grainstones and packstones, some with mega-rippled upper bedding surfaces. There are shaly partings near the top of the Steuben, but no interbedded lime or argillaceous mudstones. The upper portions of the Steuben accumulated in more turbulent, more frequently agitated waters than the sediments at the base of the exposure. On the onshore-offshore gradient, I assign the Steuben to an open marine shelf subject to occasional stirring by currents or waves (Figure 3). Certainly the Steuben was deposited in a more exposed environment than the Chaumont of Stop 1.
Trace fossils are prominent throughout the Steuben. Near the base of the exposure are examples of Palaeophycus, Planolites, and Chondrites. These burrows are confined to bedding surfaces or generally penetrate the sediment only several cm. Monocraterion, a vertical sediment filled tube one cm in diameter and up to 8 cm long, is common in the crinoidal packstones near the top of the Steuben.
The style of bioturbation also varies vertically in the Steuben. Although nowhere is the Steuben completely burrow reworked, it seems that the greatest degree of biogenic alteration of the sedimentary fabric occurs in the upper Steuben with Monocraterion. This trend runs counter what we would expect from the modern: rather than finding the greatest degree of biogenic reworking in fine-grained sediments at depth, here the coarser-grained, shallow-water environments are more reworked. Consequently, at this point Figure 3 shows the divergence in bioturbation trends for the Recent and Ordovician.

STOP 3. Whittaker Falls Park.
Nearly all of the Trenton and Black River Groups are exposed along Roaring Brook. In a combination of rapids, falls, and level stretches, the rocks are exposed in both vertical section and on bedding planes. A long, nearly continuous exposure of the Denley Limestone is the focus of our attention.
On the basis of smaller grain size and fewer indications of turbulent conditions, I have assigned the Denley to a position further offshore than the overlying Steuben Limestone. The upper 50 m of the Denley contains mega-rippled and cross-stratified grainstones interbedded with finer-grained lithologies. This portion of the Denley was deposited within the reach of storm wave base. Because the basal 9 m of the Denley lack these grainstones, this portion of the formation appears to have accumulated below storm wave base.
The Denley Limestone contains a diverse fauna including brachiopods, bryozoa, crinoids, and trilobites. Many of the body fossils apparent on outcrop here are fragmented, abraded, and occur in grainstone or packstone units. Overturned heads of the bryozoan Prasopora attest to disturbance and relocation of many of the fossils. Figure 7 is an illustration of the role of turbulent events, major storms, in producing both the sedimentary structures and the fossil assemblages in the Denley.
Not all of the fossils are reworked, however. Adhering to the tops of limestone beds, or entombed within centimeter thick shaly partings are some fossil assemblages that indicate in place accumulation. Evidence for in place accumulation includes lack of abrasion and fragmentation and the co-occurrence of fossils ranging in size from .1 to 1.5 cm. In addition, several specimens of juvenile crinoids, complete with holdfast, suggest in place burial rather than transportation before burial.
Trace fossils are abundant here. Palaeophycus and Chondrites are the most conspicuous. Again, despite the presence of burrows, the sedimentary fabrics of the Denley retain their original features. Maximum depth of burrowing is about 3 cm.

Crummy roadcut on left is Steuben Limestone.

Excellent exposures of Trenton Group.

We are climbing to the top of the Tug Hill Plateau.

STOP 4. Bridge over Gulf Stream
Park off of road on left-hand side.
Cut along Gulf Stream where we can examine the contact between the Utica Shale and the underlying Hillier Limestone of the Trenton Group.
Watch out! Poison ivy is abundant and lush here, especially on the Utica Shale.
This is a 13 m section that records the transition from wave influenced shelf to deep, anaerobic basin (Figure 8). Illustrating this trend through the Hillier Limestone is a decrease in grain size, loss of mega-rippled and cross-laminated beds, and an increase in number and thickness of shaly partings in the limestone.
Here the transition to deeper water is marked by an increase in burrowing. Palaeophycus, Planolites, and Chondrites are present, but evidence of a bioturbating, deposit-feeding community is absent. Here, too, the conspicuous body fossils are brachiopods, bryozoa, and crinoids although the gastropod Liospira is locally abundant.
The uppermost Hillier is an interesting lithology with lumpy nodular bedding. The fauna here includes mostly phosphatic forms: trilobites, conularids, and lingulids with setae preserved around the margin of the valves.
The Utica Shale is a black, fissile, argillaceous mudstone. Careful collecting can turn up cephalopods, graptolites, and the trilobite Triarthrus.

BC5: SEDIMENTARY STRUCTURES AND PALEOENVIRONMENTAL ANALYSIS OF THE BERTIE FORMATION (UPPER SILURIAN, CAYUGAN SERIES) OF CENTRAL NY
Victor P. Tollerton, Jr. and Herman S. Muskatt
Utica College of Syracuse University
Utica, N.Y.
The Bertie Formation (Upper Silurian, Cayugan Series) of New York State, is world renowned for its spectacular eurypterid fossils. However, details of the total fauna (not just the eurypterids) and its significance, along with an understanding of the depositional environment, lags behind most other rock units in New York State. An understanding of the depositional environment of the Bertie is further complicated by a lack of published studies on the sedimentary structures that occur in the formation. Almost without exception, the fossils and the sedimentary structures have been treated as separate and totally unrelated aspects. Only minor attention had been paid to the structures (e.g., mud-cracks, and the windrow accumulations).
The writers are fully aware that the fossils are an important aspect in the overall interpretation of the depositional environment of the Bertie, especially when they are considered as primary sedimentary structures. Matters of identification and errors of stratigraphic relations of the fossils in the Bertie strata severely limit their usefulness and delay understanding of their significance (see further comments under Paleontology).
With regard to the sedimentary structures, we know of no published studies that list, describe, and discuss all of them. Buchwald (1963) did study some of them. The main purpose of this paper, then, is analyses of all of the known sedimentary structures of the Bertie, with emphasis on their use in the interpretation of the depositional environment.
Although only three stops will be made in the field, all are key outcrops. Stop 1 is at Forge Hollow, New York, where a complete sequence of the Bertie with both lower and upper contacts with the Camillus and Cobleskill Formations, respectively, are exposed. Stop 2 is at Jerusalem Hill, where the upper Fiddlers Green and the lower Scajaquada Members are exposed. Stop 3 is at Passage Gulf, where the lower contact with the Camillus is exposed.

BC5: SEDIMENTARY STRUCTURES AND PALEOENVIRONMENTAL ANALYSIS OF THE BERTIE FORMATION (UPPER SILURIAN, CAYUGAN SERIES) OF CENTRAL NY

Bridge over Oriskany Creek

STOP 1. Forge Hollow, New York
Outcrop on right. Big Creek on left. Parking on right.
On Route 315 (fig. 14) Oriskany Falls, N.Y., 7 1/2 minute topographic quadrangle
Rickard (1953) locality No. 43.
This locality is believed by Leutze (1959, p. 101- 102) to be the Waterville outcrop cited by Vanuxem (1982) and Hall (1859). Rickard (1953, 1962) designated this site as the type locality for his Forge Hollow Member (= Scajaquada Member of present terminology).
This is the only complete sequence of the Bertie Formation in east-central New York. Both the lower and upper contacts with the Camillus and Cobleskill Formations, respectively are exposed. The lower contact is at the southern end of the exposure.
Fossils collecting is highly discouraged during this field trip because of the dangerous conditions at this outcrop (e.g., blind curve, narrow road, steep outcrop). KEEP OFF THE ROAD.
Nearly all faunal and sedimentary structural elements discussed in this paper have been found by the writers or reported by others as occurring here. The purpose of this stop, then, is examination of the fossils and sedimentary structures, as well as their stratigraphic sequence.

Outwash Plain

STOP 2. Jerusalem Hill Rd. outcrop
Parking in lot of Town of Litchfield Town Hall, across from outcrop.
Jerusalem Hill, Litchfield, New York (fig. 15a) West Winfield, N.Y. 7 1/2 minute topographic quadrangle Lautze (1959) locality No. 207
This locality is the Litchfield outcrop cited by Vanuxem (1842) Hall (1859), Clarke and Ruedemann (1912), and Ruedemann (1925). The Wheelock Hill locality is located about 1 1/2 miles to the NW.
Although many eurypterids have been collected here in the past, NO collecting is authorized by the town board.
The purpose of this stop is to examine the geographic and stratigraphic continuity of the fossils and sedimentary structures with those seen at stop 1, located about 16 1/2 miles straight-line distance to the west of this stop.

Quarry on right. Camillus Formation
Quarry on right. Camillus Formation, 80 feet exposed. STOP: Depends on time. (Ref. Treesh, 1972. Stop III). Beckus Gulf. CAUTION, narrow road. Syracuse Formation, nearly complete section, (Treesh, 1972, Stop II).

Vernon Shale on right, (Treesh, 1972, Stop I)

STOP 3 Passage Gulf (Spohn Rd.).
Passage Gulf, on Spohn Road (fig. 15b). Millers Mills, N.Y. 7 1/4 minute topographic gradrangle
Rickard (1953) locality No. 39; Leutze (1959) locality No. 211.
This locality exposes an areally small outcrop, that is remarkably productive with regard to fossils. The upper-most beds of the Fiddlers Green Member are often excavated, giving the appearance of a battlefield.
The farmer who owns the land at this locality has recently bulldozed off the top layers of a portion of this site.
The entire Fiddlers Green Member is easily accessible for detailed examination of the sedimentary structures and their stratigraphic sequence.
The purpose of this stop is to examine the continued geographic and stratigraphic continuity of fossils and sedimentary structures with those seen at stop 1, located about 20 miles straight-line distance to the west of this stop. Also, discussion is encouraged at this last stop relative to epeiric sea environments and the Bertie Formation.

BC6: THE STERLING MINE. ANTWERP. NEW YORK A NEW LOOK AT AN OLD LOCALITY
S. C. Chamberlain
Institute for Sensory Research
Syracuse University
Syracuse, NY 13210
The Sterling mine was the first American locality for the nickel sulfide, millerite. In the last hundred years it has produced many fine specimens of that mineral, including some that many regard to the the finest examples of the species ever found. In the past several years George Robinson at the National Museums of Canada and I have reexamined the geology, mineralogy, and origin of this landmark locality (Robinson and Chamberlain, 1984). Our interest was stimulated by our finding that much of the crystallized hematite in the ore had been reduced to magnetite and that some of the millerite had altered to the rather rare nickel silicate, pecoraite. The following pages summarize the history, geology, mineralogy, and paragenesis of this locality.

STOP 1. The Sterling Mine
The Sterling Mine is in Jefferson County, New York, along US Route 11 between Watertown and Gouverneur (Fig. 1). The water-filled open pit (Fig. 2) and surrounding dumps may be reached by foot via a farm lane which runs east from US Route 11 at a point 3.75 miles north of the intersections of Routes 11 and 26 in the village of Antwerp. The mine appears on contemporary topographic maps of the Antwerp Quadrangle as a small pond surrounded by low hills between Route 11 and Hawkins Creek. The property is owned by Mr. Raymond Villeneuve whose farm is 0.6 miles south of the entry lane on the east side of Route 11. Permission to collect must be secured before visiting the mine.

BC7: PLEISTOCENE GEOLOGY, GROUNDWATER, AND LAND USES OF THE TUG HILL, AND BRIDGEWATER FLATS AQUIFERS, ONEIDA COUNTY, NY: A CASE STUDY
Kenneth Jeffrey Goldstein
Environmental / Water Resource Planner
Oneida County Planning and Environmental Management Council
Utica, New York
No Road Log

B8: DEGLACIATION AND CORRELATION OF ICE MARGINS, APPALACHIAN PLATEAU, NEW YORK*
P. Jay Fleisher
Dept. of Earth Sciences
SUNY, College at Oneonta
Oneonta, NY 13820
and
Donald H. Cadwell
Geological Survey
New York State Museum
State Education Department Albany, NY 12230
The field trip area (Fig. 1) is located in the Susquehanna River Drainage Basin and includes parts of the Unadilla River, Wharton, Oaks, and Butternut Creek valleys. Local relief of the bedrock-drift interface reaches 1200 ft, while surface elevations range between 1050 and 2350 ft. The bedrock is predominantly Devonian sandstone, siltstone, shale (Hamilton Group) and limestone (Onondaga and Helderberg Groups). The purpose of this report, and associated field trip, is to establish and illustrate criteria for the recognition and correlation of ice margin positions in the upper Susquehanna River Drainage Basin.
This part of New York State was no doubt subjected to repeated glaciations during the Pleistocene Epoch. Multiple glaciations are suggested in the subsurface by interbedded diamictons (tills) and outwash gravels (Randall, 1972). However, the abundant glacial deposits within the field trip area formed during the advance and retreat of the Late Woodfordian ice sheet.
Six ice-marginal positions were held during Late Woodfordian time. They are, from south to north, the Wells Bridge, Oneonta, New Berlin, Cassville-Cooperstown, Middleburg, and Valley Heads ice margins. The Wells Bridge, Oneonta, and New Berlin ice margins were established during what is inferred to have been a semi-continuous retreat of the glacier. The glacier readvanced to form the Cassville-Cooperstown margin. The Middleburg ice margin developed during subsequent retreat from the Cassville-Cooperstown position. The final event within the field trip area was a glacial readvance that deposited the Valley Heads Moraine.
*Paper number 435 in the journal series of the New York State Science Service

B8: DEGLACIATION AND CORRELATION OF ICE MARGINS, APPALACHIAN PLATEAU, NEW YORK

Highway begins to climb valley wall behind Valley Heads Moraine

Hummocky crest of moraine on both sides of road

STOP 1. Ludlow Sand And Gravel Company
This gravel pit is located at the Valley Heads Moraine. Past exposures have illustrated the complex environments of deposition associated with this ice-marginal position.
F
Materials: well sorted, stratified sand, silt and clay; coarse cross bedded gravels; delta foreset gravels; laminated lake clay; poorly stratified fine sand; compact clay diamict (till).
Sedimentary structures: cross-bedding; channel lag gravels; cut and fill; large foreset beds; ripple drift laminations; slumped sands, gravels and silts.
Environment of deposition: Large(?) lake with meltwater streams of variable discharge, with deposition of gravels, sands and silts; near glacier terminus (possibly ice-contact) with deposition of sediments over blocks of glacier ice.
Noteworthy characteristics: ice-contact collapse features; thick, poorly stratified sands; well stratified, interbedded sands and gravels; channel cross bedding; delta foreset beds; compact clay layer with boulders concentrated at the base. This is diamict, deposited during an oscillation of the ice margin.

Segment of Valley Heads Moraine (on left and right)

On left (East) are ice contact, cross bedded outwash gravels.

Pitted outwash on right (West).

PICTURE STOP: "Smith Esker" on right.
This esker can be traced for almost a mile.

Cross Cedarville meltwater channel

Small gravel pit on right in outwash gravels

STOP 2. Hussey Quarry
This gravel pit contains a diamict (till) that documents the Cassville-Cooperstown readvance. The main things to see here are the stratigraphic units and the nature of their deformation.
There are three fundamental stratigraphic units exposed in the south wall of the quarry (see STOP 2 diagram). They are 1) a compact, fine-grained, matrix-supported gray diamict, which overlies 2) a tightly compact stratified drift containing fine gravels, interbedded coarse sands, and well sorted, highly distorted fine sands, and 3) a lower gravel unit containing well washed medium to coarse grained pebbles, cobbles and boulders. The compact stratified drift occurs as distorted lenses of cross-bedded sand and silt within the diamict. The lenses are upturned at their edges and contain distorted sand and silt and show thickening of each unit along fold axes. This thickening suggests that the sand and silt were NOT frozen during deformation. The underlying gravel is not well enough exposed to determine if it too is distorted.
The following questions must be addressed.
1. Origin of the compact stratified drift -
a. Were the sand and silt lenses sheared up from the lower outwash and included in the diamict by overriding ice movement?
b. Were the lenses deposited at the same time as the diamict?
c. Were the lenses deposited after the diamict and subsequently distorted by the diamict squeezing up and around them?
2. Causes of compaction and distortion -
a. Were the lens edges folded during emplacement through shearing?
b. Were the lenses deposited within the diamict with subsequent glacier overriding and deformation?
c. Were the lenses distorted during "dewatering" of the diamict?

Rt. 80 traverses hanging delta to Lake Cooperstown

Rt. 26 climbs up the kame and kettle topography
Rt. 26 climbs up the kame and kettle topography of the Cassville-Cooperstown Moraine (excellent view of moraine to the left)

PICTURE STOP

Esker on valley floor to the left, associated with ablation till

Esker complex on left

Entrance to New Lisbon Landfill - along New Berlin ice margin

Hill on left is the upvalley end of an esker

Additional eskers are seen down valley

Quarry in deltaic outwash
Entrance on left to quarry in deltaic outwash establishing a body of water in Butternut Creek valley at approximately 1150'

STOP 3. Morris Kame Quarry
In this quarry are exposed deposits typical of non-through valley deposition (stagnant ice blocks) and the associated conditions of glacier retreat. This kame and other landforms across the valley to the south depict an ice-contact environment dominated by local ponding and glacio-fluvial deposition.

Climb up the Aldrich Creek valley.
Turn left on Otsego Co. Rt. 49, which climbs up the Aldrich Creek valley. Aldrich Creek is an underfit stream occupying a valley that was enlarged by meltwater discharge along the New Berlin ice margin. Patches of discontinuous ablation till are found scattered along the valley.

House and outbuilding on the right are situated on ablation till

STOP 4. Divide Facies Of Ice-Marginal Deposits
This semi-active small quarry lies along the trend of the New Berlin ice margin. Typically, ice-marginal positions are correlated across divides by recognizing erosional features such as cols, meltwater channels or underfit streams. Here, however, is a rare view of the materials constituting a depositional landform, which resembles an ice-contact kame.
Unit | Thickness | Description
A | 36" - 48" | poorly sorted fine gravel, distorted in places
B | 24" - 30" | well stratified coarse sand, distorted by slump, collapse or injection from below
C | 6" - 12" | fine gravel with sand and silt matrix
D | 30" - 40" | compact diamict with clay matrix and striated cobbles
E | 36" - ? | washed gravels interbedded with a few layers of well sorted sand (few inches thick) which seems compact

Rt. 17 follows along the New Berlin ice margin
Rt. 17 follows along the New Berlin ice margin as it descends from the divide through the small hamlet of Cardtown and toward Pittsfield.

Kame moraine complex on the right
Kame moraine complex on the right is separated from valley wall by an outwash channel

Climb up back side of a kame moraine-outwash complex
Highway climbs up the back side of a kame moraine-outwash complex that swings across the valley marking a brief hesitation along the retreating New Berlin ice margin. Several similar complexes are found northward along Wharton Creek toward Edmeston.

Descend the pitted outwash surface
Rt. 80 descends the pitted outwash surface and follows the southern margin of a prominent dead-ice sink.

View of dead-ice sink on the right.

Another dead-ice sink can be seen on the valley floor at 2 o'clock

New Berlin valley train on left

STOP 5. New Berlin Gravel Quarry
The gravel quarry has been developed at two levels within a deltaic valley train. The upper level is primarily within the topset beds and the lower level (adjacent to Rt. 8) exposes massive foreset beds. Limestone and associated chert are major lithologic components constituting approximately 26% of all clasts (14% limestone, 12% chert). Postglacial leaching and reprecipitation of carbonates accounts for the various stages of induration found within some of the gravel units.
The topsets consist of 20 to 25 feet of moderately to poorly sorted, horizontal cobble gravels that contain some coarse sand lenses. Coarse lag gravels are common and depict a cut and fill origin. Crude channel cross bedding also is evident. Some of the sand lenses contain small-scale collapse features which are too small to have disturbed the associated gravel.
The underlying foreset beds are inclined at 28° to the southeast (S 30°-50° E) and generally consist of a finer pebbly gravel interbedded with sand. The gravel units consist of both well sorted, clast supported, matrix-free layers and sandy, pebbly fine gravel. The sand ranges from fine to coarse, with occasional silt layers up to 1 foot in thickness. No major collapse features or contorted beds were exposed in 1983.
This deposit is interpreted to be part of a massive deltaic valley train that was prograded down valley from the New Berlin ice margin (just .5 mile to the north) into an ice-contact lake. The dam was located 15 miles down valley in the vicinity of Mount Upton and Rockdale. The elevation of the dam corresponds to the topset-foreset contact elevation here. A major dead-ice sink marks the ice-marginal position at the head (upvalley extent) of the valley train. These depositional landforms and their association are helpful in recognizing the valley facies of ice-marginal positions.

Highway follows base of kame terrace scarp for the next 2.5 miles.
Kame terrace stands at 1300 ft. The kame terrace represents outwash shed along an ice margin that paralleled the Unadilla River valley, from New Berlin to Columbus Quarters. Associated kame moraines also occur along the valley, as at South Edmeston on the east side of the valley and Columbus Quarters on the west side. Late glacial discharge from the north (possibly associated with the Valley Heads readvance) dissected all of these ice-marginal landforms.

Highway climbs onto outwash associated with kame moraine

Kame-moraine complex to the right.

Highway descends north side of kame moraine
Highway descends north side of kame moraine, which is part of the New Berlin ice margin

Remnant of Cassville-Cooperstown Moraine
Breached and eroded remnant of Cassville-Cooperstown Moraine can be seen on the valley floor

Outwash plain forming the valley floor
Outwash plain forming the valley floor on the right developed from Valley Heads discharge originating from the north

Outwash surface on the right grades northward to Valley Heads
Outwash surface on the right grades northward to Valley Heads ice-marginal position near Cassville, 3 miles to the north

Characteristic hummocky topography
Road crosses characteristic hummocky topography of Cassville-Cooperstown Moraine for about one mile

Road crosses trend of Valley Heads Moraine
Road crosses trend of Valley Heads Moraine, which is not well expressed in the topography here.

BC9: SEDIMENTOLOGY AND FAUNAL ASSEMBLAGES IN THE HAMILTON GROUP OF CENTRAL NEW YORK
Bruce W. Selleck and Robert M. Linsley
Colgate University
Hamilton, NY 13346
The Middle Devonian (Givetian) Hamilton Group in Central New York State consists of approximately 1600 ft. (approximately 490 meters) of richly fossiliferous interbedded shales, siltstones and sandstones. During Givetian time, the central New York region lay to the west (present geography) of the Appalachian mobile belt. The sediments derived from this orogen were transported to the west and northwest into an epicratonic foreland basin. Other studies (Brett et al., 1983; Baird, 1979) suggest that deposition in western New York took place on a topographically subdued bottom. Regionally, paleoslope was SW-directed, but local swells and depressions of 20-100 km wave length were present (Baird, 1979). In the region of this study, the Hamilton has been the subject of numerous paleontological studies, from the pioneering work of James Hall through the biostratigraphic studies of Cooper (1930, 1933). More recently, the integration of paleontological data and detailed sedimentologic/stratigraphic studies have resulted in the development of depositional/paleoecological models (e.g. Brett et al., 1983). The purpose of this trip is to introduce participants to the varied faunas and lithofacies of the Hamilton and to document the cyclic arrangement of faunas and facies. It is this cyclicity that provides us with a key to understanding the sedimentological evolution of the Hamilton Group.

BC9: SEDIMENTOLOGY AND FAUNAL ASSEMBLAGES IN THE HAMILTON GROUP OF CENTRAL NEW YORK

Active limestone quarry on eastern valley wall.
Low hills in center of valley are part of the Munnsville kame-moraine complex. On the eastern valley wall, an active limestone quarry in the Helderberg Group and Lower Onondaga Limestone is visible.

Outcrops of Upper Helderberg Group and basal Onondaga Limestone (Edgecliff Member) on right.

Outcrop of Seneca Member on right.

Outcrops of Cherry Valley Limestone on right.

STOP 1. Chittenango Shale-Member of Marcellus Fm
Roadcut on left.
Stratigraphy/Sedimentology.
This roadcut exposes a typical section of the black silty shales that dominate the lower Marcellus Formation. Fissile, organic-rich silty shales record deposition on an anaerobic/clearly marine substrate. The extreme limitation of oxygenation and bottom circulation during deposition of this facies suggests that the waters of the basin may have been stratified in a manner analogous to the modern Black Sea. Large carbonate-cemented concretions are well-exposed mid-way up the outcrop face, and clearly demonstrate that pre-compaction cementation occurred. Note that the laminae in the silty shales are deformed by compaction around the concretions. Septarian fractures in the concretions have yielded finely crystalline dolomite, calcite and barite. Note that the surfaces of some concretions appear to have preserved burro and steinkerns of gastropods. Is there a linkage between the presence of the burrows/fossils and the formation of the concretions?
Fauna
The fauna at this stop is exceedingly limited, dominated by Styliolina with occasional specimens of Nowakia, Leiorhychus and "Euryzone". The styliolinids and Nowakia occur abundantly on particular bedding planes that occur sporadically throughout the section. It is presumed that these are planktonic forms for they are occasionally found in almost all of the lithologies of the Hamilton Group, including the apparently inhospitable environment suggested by these non-bioturbated black shales. It has recently been persuasively argued (Yochelson, in press) that Styliolina is not a mollusk, and although he did not assign it to any other higher taxon, we are persuaded that it is safest to assume that it is not a member of an extant phylum, and Fisher's assignment to the Cricocondarida seems as sound as any. Nowakia occurs much more rarely (about 1% of the fauna), but is found with the styliolines and presumably shares a similar mode of life even though taxonomically it is a tentaculitid rather than a styliolinid.
Leiorhychus and "Euryzone" are not usually found in association on the same bedding plane as Styliolina, but scattered throughout the section. Two very different interpretations have been placed on the paleoecology of these genera. It has been suggested that "Euryzone" could have had a mode of life similar to the extant genus Ianthina, which builds a bubble raft to which it clings until it bumps into its prey, the Portuguese Man-of-War, Porcellia. It has similarly been suggested that perhaps Leiorhychus was attached by its pedicle to floating pieces of wood. These interpretations thus attribute the occurrence of these genera to being introduced from outside the immediate environment. However, since both species are restricted to the black shale environment of the Hamilton we suspect that they are indeed adapted to maintaining a marginal existence in an environment that is an abomination to other faunal elements.
(Note: we have placed quotation marks around "Euryzone" because we have never seen a specimen that was determinable below the ordinal level of Archaeogastropoda. Other members of the genus Euryzone are associated with reef deposits and the anomalous environment of the Hamilton form suggests that it is probably not appropriately assigned to this genus.)

STOP 2. Bridgewater and Solsville Members of Marcellus Formation.
The basal section of the exposure here consists of dark, fissile to blocky silty shales which bear a rather limited fauna. The section coarsens upward, corresponding with gradual increase in faunal diversity. The basal portion of the Solsville Member is difficult to access at this stop, but a fair selection of typical Solsville forms can be found in talus mid-way up the exposure.
The preservation of the fossils at this locality is quite exceptional. Thin sections of the material shows that growth lines are well preserved, suggesting that the calcitic shells preserved here are probably original material. Some aragonite is still preserved, but most has been altered to calcite. Still even the mollusks exhibit good growth lines which suggests that the replacement of aragonite is a very precise molecule for molecule substitution.
This unit is also the site of some rather rare and unusual fossils including the monoplacophoran Cyrtolites and the bellerophont Praematarotropis and soft bodied preservation of annelids (Cameron, 1967).
The fauna is dominated by the brachiopods Spinocyrtia in the upper sandier facies, and Mucrospirifer in the middle siltier layers, along with the bivalves, Ptychopteria flabellum, Gosseletia triquetra, and a variety of nuculids, gastropods including Bembexia sulcomarginata and Palaeozygopleura hamiltoniae plus a variety of orthoconic cephalopods.
One unusual aspect of the preservation in this quarry is the fact that a very large percentage of the bivalves are preserved with both valves intact. This is no surprise for nuculids which are infaunal and typically are entombed in the sediments which prevents their valves from gaping open upon death. However, for bysally attached semi-infaunal forms like Gosseletia, mobile semi-infaunal forms like Grammysia and epifaunal genera like Ptychopteria, it is unexpected to find both valves intact. It would seem possible that quick burial may have been an intermittent, but relatively common cause of death in this assemblage. This interpretation is also consistent with the rather large escape burrows that are abundant in this unit.
Many faunal elements in this unit are restricted to single bedding planes that may repeat throughout the quarry. For example, Palaeozygopleura has been found on only three horizons, but within those horizons they may be very abundant. The axis of coiling of the shells of Palaeozygopleura in this quarry are randomly oriented allowing us to infer that they have not been aligned by current action. Yet twice as many are found in an aperture down position as in an aperture up position. Since all positions of this shell exhibit equal hydrodynamic stability, we infer that the shells were occupied at the time of death, and the orientation of the shells reflects the life position.
Other bedding planes are dominated by Bembexia sulcomarginata, a pleurotomarian which was probably an algae grazer or possibly a deposit feeder. Many of the shells of Bembexia in this unit are encrusted with a trepostomatous bryozoan (Leptotrypella). Most frequently it is the upper surface of Bembexia that is encrusted, though some specimens exhibit encrustation of the base while the spire remains clean. Very rarely is a specimen found in which the encrustation spreads very far from one side onto the other.
We suspect that encrustation primarily developed on dead shells on Bembexia. Bembexia is a genus that is only found in the Marcellus and Skaneateles Formations of the Hamilton Group while Palaeozygopleura is found throughout.

STOP 3. Basal Moscow Formation.
This quarry exposes the "interior portion" of a upward-coarsening cycle of the Hamilton Group and can be generalized as consisting of an upper sandy facies dominated by bivalves and a lower silty facies dominated by brachiopods. Separating the two facies is a thin coquina consisting predominantly of the shells of Spinocyrtia granulosa.
The upper sandy unit is dominated by large epi-byssate bivalves and large semi-infaunal bivalves as well as larger spiriferoid brachiopods. There are also occasional specimens of the burrowing trilobite Trimerus (Dipleura) deKayi and large specimens of Phacops rana.
The lower silty portion of dominated by brachiopods, particularly Chonetes, Devonochonetes, Athyris Rhipidomella, and Mucrospirifer. Bivalves are also abundant, commonly infaunal nuculids or mobile semi-infaunal forms (such as Grammysia). The dominant trilobites in this facies are Greenops and smaller specimens of Phacops. Gastropods are represented by Glyptotomaria and Ruedemannia, the bellerophont Retispira and Palaeozygopleura. Bembexia drops out of the fauna after the Skaneateles. However, the Palaeozygopleura shells in this quarry are barely recognizable for the shells are completely encrusted by the trepostomate bryozoan Leptotrypella. The aperture is always open, but the shell is completely encrusted all the way around which is quite surprising since Palaeozygopleura is a shell dragger, incapable of lifting its shell from the substrate. This leads us to conclude that either Leptotrypella was capable of extending its colony down into the sediment (which no modern bryozoan can do) or that there was a secondary occupant (a sipinculid?) of the dead Palaeozygopleura shell that was capable of elevating the shell off of the substrate so that the bryozoan could establish itself everywhere except the aperture. In some individuals the encrustations became much thicker on one side of the shell than the other, always the adapertural side is thickened, which leads us to believe that the secondary occupant is still occupying the shell, but the mass of bryozans has forced him to resort to a shell dragging mode, thus killing the bryozoans on the apertural side of the colony.
There are also massive colonies of other trepostomatous bryozans in the lower part of the quarry.

STOP 4. Geer Road - Quarry
Stratigraphically and faunally this locality is similar to STOP 3. The faunal elements are essentially as described for the previous locality. Some of the rarer elements of the fauna of both quarries include Hyolithes, occasionally with helens and operculum in place, and two different phyllocarids with their bivalved cephalothorax and segmented abdomen with the telson composed of three spike-like projections.
A prominent surface near the basal portion of the section exposes a phosphate pebble bed containing abundant brachiopods and rare fish plates.

STOP 5. Roadside Quarry and rubble: Mottville Member of Skaneateles Fm.
Roadside Quarry and rubble: Mottville Member of Skaneateles Fm. Sedimentology:
The exposure at this stop nicely exhibits the shaley siltstone-to-sandstone transition of the Mottville Member. The lowermost portion of the outcrop consists of relatively fissile to blocky shaley siltstones dominated by small brachiopods. The section coarsens rapidly upward to silty, fine-grained sandstones which exhibit some cross-lamination and rare hummocky bedding.
Fauna
This stop is dominated by the higher energy faunal elements that characterize the silty sandstones of the Hamilton Group. These include the large epifaunal byssate pectinoid bivalves including Glyptodesma, Leiopteria, Pterinopecten, Actinopteria and Limoptera as well as semi-infaunal bivalves such as Grammysia. The typical trilobite of the unit is the large burrowing trilobite Trimerus, whose punctate carapace comprises one of the dominant skeletal elements of this locality. Complete specimens are fairly common, most commonly not enrolled and not infrequently oriented on edge or on end as some other unusual position relative to the sediments. It is suggestive that the area was occasionally subjected to events, which involved rapid burial. Other common elements include the brachiopods Spinocyrtia, Mucrospirifer, Camarotoec and Devonoproductus. The gastropods are not well preserved here, but include Bembexia and Palaeozygopleura.

C10: THE LATE WISCONSINAN GLACIATION OF THE WEST CANADA CREEK VALLEY
Jack C. Ridge
Dept. of Geology
Syracuse University
Syracuse, NY
David A. Franzi
Lafayette College
Easton, PA
Ernest H. Muller
This field trip focuses on the glacial stratigraphy of the West Canada Valley and the interpretation of the Late Wisconsinan history of the region. The Late Wisconsinan stratigraphic record in the West Canada Creek Valley (Figure 1) is unique in central New York in terms of its completeness and in the complexity of the glacial events that it represents. The significance of such lithostratigraphic documentation of the glacial record is underscored by the lack of success in developing a regional glacial chronology based on morphostratigraphic relationships (Coates, 1976; Calkin and others, 1982). Correlations based solely on morphologic evidence are often ambiguous due to the time transgressive and composite nature of many glacial landforms. The glacial deposits of the West Canada Creek Valley provide an important lithostratigraphic basis for correlations to the well-developed time-stratigraphic and geologic-climate classifications in the eastern Great Lakes Region (Dreimanis and Karrow, 1972; Dreimanis and Goldthwait, 1973).
The West Canada Creek Valley is an area where the sedimentology of readvance deposits and relative chronology of simultaneous readvances from several different ice flow directions may be studied. Ice from the Ontario Lobe (Black River and Oneida Sublobes) and the Hudson-Champlain Lobe (Mohawk Sublobe) as well as Adirondack through flow and possible Adirondack ice cap sources encroached on this region during the Late Wisconsinan (inset on Figure 1).
The field trip is designed to give an introduction to as many of the glacial stratigraphic units as possible and to show their sedimentologic diversity. It can in no way, however, show all the stratigraphic relationships which were used to determine the glacial history of the region. This would require too many stops for a one day excursion. In addition, many exposures that would be more informative than those shown on this trip are not readily accessible or are inappropriate for a group of this size. Important localities which are not included as stops on the field trip are discussed in the text.

C10: THE LATE WISCONSINAN GLACIATION OF THE WEST CANADA CREEK VALLEY

Kast Bridge.
The course of West Canada Creek has been straightened in this section of the valley. Note the flat topped bluff on east bank of West Canada Creek.

Holland Patent and Norway tills
Bluffs on left side of highway (to west) expose Holland Patent and Norway tills. North Creek enters West Canada Creek from the east. West Canada till and striations on bedrock of the Trenton Group (N60W) are exposed along the last mile of North Creek before it enters West Canada Creek.

Bluffs on east bank of West Canada Creek
Bluffs on east bank of West Canada Creek expose units from Holland Patent till at the top through Norway and Hawthorne tills to West Canada till at the base. The bluffs are typical of many high banks along West Canada Creek between Kast Bridge and Middleville. These bluffs do not exist on the west bank of West Canada Creek because of the asymmetry of the bedrock profile of the valley. The apparent flat-topped surfaces of the bluffs are capped by till and lacustrine sediments. The flat benches may be the result of initial fluvial downcutting in the valley or the floors of lakes that existed during recession of the Barneveld Readvance.

View of STOP 1 from KOA campground.
Bluff on east bank of West Canada Creek (Section 9 on Figure 3). Ahead on left are commercial Herkimer "diamond" (more appropriately Middleville "diamond") prospecting grounds.

Exposures of Little Falls Dolostone on left while entering town of Middleville.

STOP 1. West Canada Creek bluff exposure.
Park vehicles on shoulder of Rt. 169 next to entrance to pasture on right. Walk on dirt road to right to top of hill and across pastures for 0.5 miles to West Canada Creek bluff exposure.
Features and topics for discussion: (Section 9 on Figure 3)
1) Lithology and genesis of unit equivalent to the Norway till.
2) Lithologic and provenance changes within lacustrine sediment between the Norway till equivalent and the Hawthorne till.
3) Nature of contact of Hawthorne till and upper Newport beds.
4) Transition from upper Newport beds to West Canada till.
5) Compact and stony character of West Canada till.
6) Paleomagnetic samples were taken from the upper Newport beds and from three levels within the lacustrine sediments between the Norway till equivalent and the Hawthorne till.

Terrace along West Canada Creek.
Many terraces in the valley are graded to lake levels in the lower West Canada and Mohawk valleys (Figure 13). They contain alluvial fan sediment and slope away from large gullies cut in the glacial deposits along the valley sides.

Outcrops of Little Falls Dolostone
Right side or Rt. 28 and continuing for the next l.5 miles are outcrops of Little Falls Dolostone. Behind the exposure on the right is a large quarry noted for its Herkimer "diamonds".

STOP 2. White Creek
Park vehicles and walk across pasture on west side of White Creek Road.
Features and topics for discussion: (Section 5 on Figure 3)
1) Upper Newport beds appear at top of bluffs in soil profile.
2) Clayey and silty character of West Canada till.
3) Deformation of lower Newport beds beneath West Canada till. Nappe-like folds and thrusts with northwest directed displacement.
4) Transition from lower Newport beds to White Creek till and associated sediment flows.
5) Topography on the upper surface of the White Creek till (morainic or drumlinoid features or neither?).
6) Very stony character of the White Creek till which contains a high proportion of metamorphic clasts.
7) Subglacial grooving on the surface of the White Creek till has been exposed here in the past.

Large bluff on the west bank of West Canada Creek
In view to the west-southwest from this intersection is a large bluff on the west bank of West Canada Creek (Section 6 on Figure 3). This section contains all the units from the lower Newport beds to the Norway till on top.

Hawthorne till overlying upper Newport beds
Right side or highway. Bluff exposure of Hawthorne till overlying upper Newport beds.

Old meander scar of West Canada Creek.
Right side of highway. Across pasture are bluff and gully exposures (Sections 3 and 4 on Figure 3) which contain all units from basal White Creek till up thru Norway till.

Lacustrine sands
Right side of highway. Lacustrine sands which lie stratigraphically below the Norway till and may predate or be time-equivalent to the Hawthorne till and Salisbury Readvance

Fluvial terrace on right
Fluvial terrace on right is inset in an older alluvial fan which slopes toward the center of the valley from large gullies to the northeast.

STOP 3. Poland sand and clay pits.
Two exposures:
1) pit exposing outwash sands. Fluvial sand infilling early incision of the valley cut during fall in lake levels proceeding the Barneveld Readvance.
2) Clay Pit exposure of Phase II sediments.
Section: (similar to Sections 1 and 2 on Figure 3 and northwest end of West Canada Valley profile on Figure 7)
(top) |
6 ft. | oxidized varves (soil profile)
1 ft. | sediment flows
6 ft. | clayey dark gray till with high proportions of sandstone and Trenton Group limestone clasts (Norway till)
1 ft. | deformed lacustrine beds
4 ft. | thin varve couplets (less than 2 inches) containing a pink and tan clay component and red rain-out sediment (Oneida Sublobe provenance); flutes indicate paleocurrent flow to the southeast.
12 ft. | thick varve couplets (greater than 2 inches) with dark gray and drab colors and black rain-out sediment near base (Mohawk Sublobe provenance); couplets thicken downward; rib and furrow structures indicate paleocurrent flow to the northwest.
2 ft. | lacustrine sand and silt, oxidized at top and contain calcareous cement
25 ft. | rippled lacustrine sands with calcareous cemented layers and lenses; paleocurrent flow to the east
| (limit of exposure)
Note especially change from Mohawk to Oneida Sublobe provenance within the varve section accompanied by a change in paleocurrent directions from northwest to southeast.

Ice-marginal delta at the maximum position of the Barneveld Readvance.
Flat-topped hill to right with gravel pit excavations is capped by an ice-marginal delta at the maximum position of the Barneveld Readvance.

STOP 4. Cincinnati Creek sections (Figure 5).

Incised portion of a delta
The highway crosses an incised portion of a delta deposited during recession from the Hinckley Readvance.

Hinckley Moraine System
Hills on both sides of the highway are a part of the Hinckley Moraine System.

Exposure on the east side of the road
Exposure on the east side of the road contains calcareous western provenance gravel overlying older non-calcareous gravel of Adirondack provenance.

STOP 5. Dirt driveway leading to Trail's End bluff
Dirt driveway leading to Trail's End bluff exposure on Hinckley Reservoir (Figure 10). NOTE: This is private property.

STOP 6. Balley Hills delta.

Hummocky topography
On both sides of the road is hummocky topography resulting from stagnation of the Black River Sub lobe as it thinned over the Black River-West Canada Creek divide during recession from the Hinckley Readvance. The drift is composed of both stratified deposits and ablation till.

C11: STRUCTURE AND ROCK FABRIC WITHIN THE CENTRAL AND SOUTHERN ADIRONDACKS
James McLelland
Colgate University
Hamilton, NY
2011: This following trips are identical:

C11: STRUCTURE AND ROCK FABRIC WITHIN THE CENTRAL AND SOUTHERN ADIRONDACKS

STOP 1. Peck Lake Fm.
This exposure along Rt. 29A just north of Peck Lake is the type locality of the sillimanite-garnet-biotite-quartz-feldspar gneisses (kinzigites) of the Peck Lake Fm. In addition, there are exposed excellent minor folds of several generations. Note that the F2 folds rotate an earlier foliation.
The white quartzo-feldspathic layers in the kinzigites consist of quartz, two feldspars, and garnet and are believed to be anatectic. Note that fish-hook terminations on some of these suggest that they have been transposed. It is also clear that these anatectites have been folded by F2 indicating a pre-F2 metamorphic event(s). In a similar fashion some garnets in the rock appear to be flattened while others do not. It is believed that the anatectites formed at the muscovite-quartz reaction and are essentially in situ melts. Further anatexis did not take place due to absence of vapor.

STOP 2. Irving Pond Fm., .5 mile north of Nick Stoner's Inn, Canada Lake .
The outer portion of the Irving Pond Fm. is exposed in low cuts along the east side of Rt. 29A just prior to the crest in the road heading north.
At the southern end of the cut typical, massive quartzites of the Irving Pond are seen. Proceeding north the quartzites become "dirtier" until they are essentially quartzose sillimanite-garnet-biotite-feldspar gneisses (kinzigites).
At the northern end of the cut, and approximately on the Irving Pond/Canada Lake Fm. contact there occurs an excellent set of F2 minor folds. Polished slabs and thin sections demonstrate that these fold an earlier foliation defined by biotite flakes and flattened quartz grains.
The Irving Pond Fm. is the uppermost unit in the stratigraphy of the southern Adirondacks. Its present thickness is close to 1000 meters, and it is exposed across strike for approximately 4000 meters. Throughout this section massive quartzites dominate.

STOP 3. Canada Lake Charnockite
These large roadcuts expose the type section of the Canada Lake charnockite. Lithologically the charnockite consists of 20-30% quartz, 40-50% mesoperthite, 20-30% oligoclase, and 5-10% mafics. The occurrence of orthopyroxene is sporadic. These exposures exhibit the olive-drab coloration that is typical of charnockites. Note the strong foliation in the rock.
Although no protolith is known with certainty for these rocks a metavolcanic history is suggested by their homogeneity and lateral continuity. Their bulk chemistry corresponds to dacites.

Canada Lake Store. Good exposures of Royal Mt. member of Green Lake Fill.

STOP 4. Rooster Hill megacrystic gneiss at the north end of Stoner Lake.
This distinctive unit is believed to be, in part, correlative with the Little Moose Mt. Fm. Here the unit consists of a monotonous series of unlayered to poorly layered gneisses characterized by large (1-4") megacrysts of perthite and microcline perthite. For the most part these megacrysts have been flattened in the plane of foliation as well as elongated in an E-W direction with concomitant developed of tails of grain-size reduced tails asymmetric to foliation. However, a few megacrysts are situated at high angles to the foliation. The groundmass consists of quartz, oligoclase, biotite, hornblende, garnet, and occasional orthopyroxene. An igneous rock analogue would be quartz-monzonite or granodiorite depending on concentration of K-feldspar.
The origin of the Rooster Hill is obscure. Its homogeneity over a thickness approaching 2.5 km suggests an igneous parentage. This conclusion gains support from the presence of localities where megacrysts appear to retain a random orientation, and from the occasional presence of what may be drawn out xenoliths of biotitic or amphibolitic gneisses. However, these features may be explained by other models. The contacts of the Rooster Hill are always conformable with enclosing units, and this suggests a metastratified (metavolcanic?) origin. However, the anorthosites of the region also show conformable contacts, and this may, in part, be due to tectonic flattening.
Recently Eckelmann (pers. comm.) has studied zircon population morphologies in the Rooster Hill and similar lithologies. His results strongly suggest an igneous plutonic origin. This would be consistent with the igneous origin assigned the Hermon granite of the northwest Adirondacks - a rock that is markedly similar to the Rooster Hill.

Low roadcut in kinzigites of Tomany Mt. Fm.

Long roadcuts of quartzo-feldspathic gneisses and metasediments
Long roadcuts of quartzo-feldspathic gneisses and metasediments of Lake Durant Fm. intruded by metagabbro and anorthositic metagabbro.

Roadcut of anorthositic metagabbro and metanorite.

Excellent examples of anorthositic gabbros
Roadcut on west side of highway shows excellent examples of anorthositic gabbros intrusive into layered pink and light green quartzo-feldspathic gneisses. The presence of pegmatites and cross-cutting granitic veins is attributed to anatexis of the quartzo-feldspathic gneisses by the anorthositic rocks.

Stop 5. Lake Durant and Sacandaga Fms.
Stop 5. Lake Durant and Sacandaga Fms. intruded by anorthositic gabbros and gabbroic anorthosites. These roadcuts are located on Rt. NY 10 just south of Shaker Place.
The northernmost roadcut consists of a variety of metasedimentary rocks. These lie directly above the Piseco anticline and are believed to be stratigraphically equivalent to the Sacandaga Formation. The outcrop displays at least two phases of folding and their related fabric elements. These are believed to be F2 and F3. A pre-F2 foliation is thought to be present. Both axial plane foliations are well developed here. Several examples of folded F2 closures are present and F2 foliations (parallel to layering) can be seen being folded about upright F3 axial planes.
Farther to the south, and overlooking a bend in the west branch of the Sacandaga River, there occurs a long roadcut consisting principally of pink and light green quartz-perthite gneiss belonging to the Lake Durant Fm. About half-way down this roadcut there occurs a large boudin of actinolitic and diopsidic gneiss. To the north of the boudin the quartzo-feldspathic gneisses are intruded pervasively by anorthositic gabbros, gabbroic anorthosites, and various other related igneous varieties. At the north end of the cut and prior to the metastratified sequences these intrusives can be seen folded by upright fold axes. They are crosscut by quartzo-feldspathic material.
Within this general region the Lake Durant Fm. and other quartzofeldspathic gneisses seem to have undergone substantial anatexis. This is suggested by the "nebular" aspect of the rocks. Good examples of this are seen in the manner in which green and pink portions of the quartzo-feldspathic gneisses mix. Note also the clearly cross-cutting relationships between quartzofeldspathic gneiss and mafic layers at the south end of the roadcut. Here it seems that mobilized Lake Durant is cross-cutting its own internal stratigraphy. Also note that the quantity of pegmatitic material is greater than usual. This increase in anatectic phenomena correlates closely with the appearance of extensive metagabbroic and metanorthositic rocks in this area. It is believed that these provided a substantial portion of the heat that resulted in partial fusion of the quartzo-feldspathic country rock.

Red-stained basal quartzo-feldspathic gneisses that have been faulted along NNE fractures.

Stop 6. Core rocks of the Piseco anticline.
Hinge line of Piseco anticline near domical culmination at Piseco Lake. The rocks here are typical basal quartzo-feldspathic gneisses such as occur in the Piseco anticline and in other large anticlinal structures, for example Snowy Mt. dome, Oregon dome.
The pink "granitic" gneisses of the Piseco anticline do not exhibit marked lithologic variation. Locally grain size is variable and in places megacrysts seem to have been grain size reduced and only a few small remnants of cores are seen. The open folds at this locality are minor folds of the F3 event. Their axes trend N70W and plunge 10-15° SE parallel to the Piseco anticline. Co-axial F2 isoclines are also present.
The most striking aspect of the gneisses in the Piseco anticline is their well-developed lineation. This is expressed by rodding and ribbon fabrics. These may consist of alternating ribbons of quartz, quartzo-feldspathic gneiss, and biotite-rich layers. In some instances the rods represent transposed layering on the highly attenuated limbs of early, isoclinal minor folds. Near the northeast end of the roadcut such minor folds are easily seen due to the presence of more massive layers in the rock. Slabbed and polished specimens from this and similar outcrops demonstrates that these early folds are exceedingly abundant in the Piseco anticline. Examination of these folds shows that the dominant foliation in the rock is axial planar to them.
The lineation in these outcrops is shown in Fig. 8a while slabbed sections are shown in Figs. 8b,c. Fig. 8b is cut perpendicular to foliation and both parallel to (left face) and perpendicular to (right face) lineation. As can be seen K-feldspar augen have been elongated in the direction of lineation. Together with elongated quartz aggregates, these grain size reduced minerals form the prominent mineral lineation that characterizes foliation surfaces (Fig. 8a). Note that the K-feldspar augen exhibit shapes closer to equant on the right hand face at perpendicular to lineation. This strongly suggests that the rock fabric is the result of rotational strain in the direction parallel to lineation, i.e., the lineation is an elongation, or stretching type. Fig. 9 shows a less deformed sample slabbed perpendicular to foliation and parallel to lineation. The development of tails on K-feldspar augen are clearly visible. These are the result of grain size reduction during ductile rotational strain. A sinistral (east over west) sense of motion is indicated. At more extreme conditions of strain the K-feldspar augen and quartz aggregates are drawn into ribbons as in the present outcrop. Long dimensions of 40-60 cm are common along with thicknesses of a millimeter, or less. Clearly strain has been extreme and elongations of 30-40 times are not unusual.
Ribbon gneiss origin by rotational strain is also suggested by the parallelism between lineation and F2, F3 fold axes. It is believed that these fold axes were drawn into parallelism with the lineation by ductile, rotational strain directed from east to west. The most satisfactory mechanism for this configuration is the stacking of thrust sheets and thrust nappes during plate collision. Thrusts have been recognized to the east of Lake George (Fig. 4) and others probably exist although the intense, ductile nature of the deformation has resulted in extremely subtle truncations that are difficult to recognize. Sheath folds (Fig. 10) with tube axes parallel to lineation are consistent with this model. Presumably crustal thickening during the Grenville Orogeny was caused by the stacking of these thrusts.

Stop 7. Blue Mt. Lake Fm. exposed in roadcuts on both sides of highway.
The Blue Mt. Lake Fm. is exposed in roadcuts on both sides of the highway. These exposures show typical examples of the extreme ductility of the carbonate-rich units. The south wall of the roadcut is particularly striking, for here relatively brittle layers of garnetiferous amphibolite have been intensely boudinaged and broken. The marbles, on the other hand, have yielded plastically and flowed with ease during the deformation. As a result the marble-amphibolite relationships are similar to those that would be expected between magma and country rock. Numerous rotated, angular blocks of amphibolite are scattered throughout the marble in the fashion of xenolith, in igneous intrusions. At the eastern end of the outcrop tight isoclinal folds of amphibolite and metapelitic gneisses have been broken apart and rotated. The isolated fold noses that rema in "floating" in the marble have been aptly termed "tectonic fish." The early, isoclinal folds rotate on earlier fo1iation.
Near the west end of the outcrop a deformed layer of charnockite is well exposed. In other places the charnockite-marble interlayering occurs on the scale of one to two inches.
Exposed at several places in the roadcut are cross-cutting veins of tourmaline and quartz displaying a symplectic type of intergrowth. Other veins include hornblende and sphene bearing pegmatites.
Commonly included in the Blue Mt. lake Fm., but not exposed here, are quartzites, kinzigites; sillimanite rich, garnetiferous quartz-microcline gneisses; and fine grained garnetiferous leucogneisses identical to those characterizing the Sacandaga Fm. These lithologies may be seen in roadcuts .5 mile to the south.
Almost certainly these marbles are of inorganic origin. No calcium carbonate secreting organisms appear to have existed during the time in which these carbonates were deposited (> 1 b.y. ago). Presumably the graphite represents remains of stromatolite-like binding algae that operated in shallow water, intertidal zones. If so, the other roadcut lithologies formed in this environment as well. This seems reasonable enough for the clearly metasedimentary units such as the quartzites and kinzigites. The shallow water environment is much more interesting when applied to the charnockitic and amphibolite layers. The fine scale layering, and ubiquitous conformity of these, strongly suggests that they do not have an intrusive origin. Perhaps they represent the metamorphosed products of volcanic material in a shelf like environment. Such intercalation is now occurring in many island arc areas where shallow water sediments cover, and in turn are covered by, ash and lava. Alternatively they may represent metasediments. A large lumber of minerals are developed within these outcrops. Both calcite and minor dolomite are present in the carbonate horizons. These are accompanied by green diopside and serpentinized forsterite as well as by tourmaline, graphite, and various sulfides. In calcsilicate horizons phlogopite, diopside (white), and tremolite occur. Wollastonite is locally present. The presence of tremolite and wollastonite is believed to be a function of the relative concentration of CO2 and H2O in the vapor phase Valley et al., 1983).

Extensive roadcuts in lower part of Blue Mt. Lake Fm.
Quartzites, kinzigites, and leucogneisses dominate. Minor marble and calcsilicate rock is present.

Large roadcuts in lower Lake Durant Fm.
Pink, well-layered quartzo-feldspathic gneisses with subordinate amphibolite and calcsilicate rock.

Stop 8. Intermediate Adirondack anorthositic gneiss
On the west side of the road small roadcut exposes an excellent example of Adirondack anorthositic gneiss intermediate in character between the so-called Marcy type (coarse) and the Whiteface type (fine grained). About 50% of the rock consists of fine grained crystals of andesine plagioclase. Some of these crystals appear to have measured from 6-8" prior to grain size reduction. Excellent moonstone sheen can be seen in most crystals. In places ophitic to subophitic texture has been preserved with the mafic phase being represented by orthopyroxene.
In addition to the anorthosite there exists a clearly crosscutting set of late iron-rich orthopyroxene rich dikes containing xenoliths of coarse grained anorthosite. The latter may represent a late mafic differentiate related to cotectic liquids responsible for the ophitic intracrystalline rest magma. This would be consistent with the iron enrichment trend characteristic of Adirondack igneous differentiation.
Near road level there can be found several inclusions of calcsilicate within the anorthositic rocks. These are believed to have been derived from the Cedar River Fm. and are consistent with a non-basement status for the anorthosite.
The upper, weathered surface of the outcrop affords the best vantage point for studying the textures and mineralogy of the anorthositic rocks. In several places there can be seen excellent examples of garnet coronas of the type that are common throughout Adirondack anorthosites. These coronas are characterized by garnet rims developed around iron-titanium oxides and pyroxenes. Recently McLelland and Whitney (1977) have succeeded in describing the development of these coronas according to the following generalized reaction:
Orthopyroxene + Plagioclase + Fe-bearing oxide + quartz = garnet + clinopyroxene.
This reaction is similar to one proposed by de Waard (1965) but includes Fe-oxide and quartz as necessary reactant phases. The products are typomorphic of the garnet-clinopyroxene subfacies of the granulite facies (de Waard 1965). The application of various geothermometers to the phases present suggests that the P,T conditions of metamorphism were approximately 8 Kb and 700 ± 50°C respectively.

Cedar River Fm. Minor marble, amphibolite, and calcsilicate rock.
Predominantly very light colored sillimanite-garnet-quartz-K-feldspar leucogneisses.

Leucogneisses of the Blue Mt. Lake Fm.
To the west of the intersection are roadcuts in leucogneisses of the Blue Mt. Lake Fm. A large NNE normal fault passes through here and fault breccias may be found in the roadcut and the woods beyond.

Entering Little Moose Mt. Fm.
Entering Little Moose Mt. Fm. on northern limb of the Glens Falls syncline. Note that dips of foliation are to the south.

Downdropped block of lower Paleozoic sediments.
Entering town of Wells which is situated on a downdropped block of lower Paleozoic sediments. The minimum displacement along the NNE border faults has been determined to be at least 1000 meters.

Silver Bells ski area to the east.
The slopes of the ski hill are underlain by coarse anorthositic gabbro intrusive into the Blue Mt. Lake Fm.

Lake Durant Fm
On the north side of NY Rt. 30 are quartzo-feldspathic gneisses and calcsilicate rocks of the Lake Durant Fm. An F1 recumbent fold trends subparallel to the outcrop and along its hinge line dips become vertical.

Gabbro and anorthositic gabbro.

Stop 9. Pumpkin Hollow.
Large roadcuts on the east side of Rt. 30 expose excellent examples of the Sacandaga Fm. At the northern end of the outcrop typical two pyroxene-plagioclase granulites can be seen. The central part of the outcrop contains good light colored sillimanite-garnet-microcline-quartz gneisses (leucogneisses). Although the weathered surface of these rocks are often dark due to staining, fresh samples display the typical light color of the Sacandaga Fm. The characteristic excellent layering of the Sacandaga Fm. is clearly developed. Note the strong flattening parallel to layering and the lineation developed on many foliation surfaces. These gneisses are similar to so-called straight gneisses found in proximity to ductile shear zones. The Sacandaga Fm. may represent mylonitic rocks of this type and its layering may, in fact, be tectonic.
Towards the southern end of the outcrop calc-silicates and marbles make their entrance into the section. At one fresh surface a thin layer of diopsidic marble is exposed. NO HAMMERING PLEASE. Many "punky" weathering layers in the outcrop contain calc-silicates and carbonates.
At the far southern end of the roadcut there exists an exposure of the contact between the quartzo-feldspathic gneisses of the Piseco anticline and the overlying Sacandaga Fm. The hills to the south are composed of homogeneous quartzofeldspathic gneisses coring the Piseco anticline (note how ruggedly this massive unit weathers). The Sacandaga Fm. here has a northerly dip off the northern flank of the Piseco anticline and begins its descent into the southern limb of the Glens Falls syncline.
No angular discordance or other indications of unconformity can be discerned at the base of the Sacandaga Fm. However, this does not preclude the prior existence of an angular discordance which may have been swept into pseudo-conformity by tectonism.
Along most of the roadcut there can be found excellent examples of faults and associated pegmatite veins. Note that the drag on several of the faults gives conflicting senses of displacement. The cause of this is not known to the author. Also note the drag folds which indicate tectonic transport towards the hinge line of the Piseco anticline.

Core of the Piseco anticline.
All exposures are within the basal quartzo-feldspathic gneisses at the core of the Piseco anticline.

Re-enter the Sacandaga Fm. Dips are now southerly.

Southerly dipping quartzo-feldspathic gneisses of Lake Durant Fm.
In long roadcuts of southerly dipping quartzo-feldspathic gneisses of Lake Durant Fm.

C12: GROUNDWATER CONTAMINATION FROM A SANITARY LANDFILL: INVESTIGATIONS, REMEDIAL ACTION AND ENERGY RECOVERY AS A POSSIBLE SOLUTION
Kenneth Jeffrey Goldstein
Environmental / Water Resource Planner
Oneida County Planning and Environmental Management Council
Utica, New York
PURPOSE
The purpose of this field trip is to view the adverse impacts resulting from the improper disposal of solid and hazardous wastes. A tour of the Rome Sanitary Landfill will reveal the impacts on the environment resulting from hazardous waste landfill leachate. Leachate can be seen at the landfill and in nearby streams. The participants will be able to view the remedial measures being conducted at the site, including, the construction of a barrier cap, gas vents and monitoring wells. A discussion on the elements of the site investigation and remedial actions utilized will be conducted while touring the facility. Questions are encouraged! Later in the day the participants will tour the Oneida County Energy Recovery Facility in Rome, N.Y. This facility, which will not be operational at the time of the field trip, is one of Oneida County's solutions to the land burial of industrial and municipal solid waste. Although the facility will not be operational, all equipment will be on-line and will be reviewed.
No Road Log

C13: SEISMICITY IN THE CENTRAL ADIRONDACKS WITH EMPHASIS ON THE GOODNOW, 10/7/84 EPICENTRAL ZONE AND ITS GEOLOGY
Lamont-Doherty Geological Observatory
of Columbia University
Palisades, New York, 10964
No Road Log