NYSGA 1970
NEW YORK STATE GEOLOGICAL ASSOCIATION
42nd Annual Meeting May 1, 2, 3, 1970
FIELD TRIP GUIDEBOOK
William Graham Heaslip, Editor
Department of Geology
State University College at Cortland
Cortland, New York

A: BENTHIC COMMUNITIES OF THE GENESEE GROUP (UPPER DEVONIAN)
Jonathan W. Harrington
The University of Calgary
"The interest in a science such as geology must consist in the ability of making dead deposits represent living scenes." ---Hugh Miller
Introduction
The New York Devonian is unique in its completeness, fossil content, numerous outcrops, and relatively undisturbed nature. It is the standard reference section for North America and displays a classic example of facies transition. Stratigraphic and paleontologic investigation over the past century has resulted in a wealth of information. "Despite this, perhaps another century of rigorous study will be required before a thorough understanding of its paleontology, lithology, stratigraphy and paleoecology can be attained." (Rickard,1964).
It is doubly apropos that we examine the Genesee Group in the Cortland area. The rocks of this region and their organic remains are of considerable historical interest, having received attention since the earliest days of geological investigation in New York State. In fact, the presence of fossil shells in the Devonian rocks of New York was first noted in 1751 at a hillside outcrop in Cortland County by John Bartram, a member of Lewis Evans' Onondaga expedition (Wells, 1963).

STOP 1. Small quarry on West River Road
1. Small quarry on West River Road, just south of Bloggett Mills, Cortland Co.
This exposure in the Upper Ithaca formation (correlative with the Triphammer member in the Cayuga Lake meridian) consists of fine shales and siltstones of the Smethport depositional phase. The leptodesma biotope is represented by an abundant fauna, consisting of the spiriferid. Platyrachella,and Leptodesma, with numerous large pectinoid and mytiloid pelecypods. Most brachiopods, especially the rhynchonellids, are conspicuously absent.
2012: Guess at location.

STOP 2. Hillside quarry, 1 mile south of Cortland on Rte 90.
At this outcrop in the upper Ithaca the Big Bend phase is represented by a sequence of gray shales and siltstones. with some lenses of leached coquinite. An extremely varied benthic fauna is present. Especially abundant are Leiorhynchus mesacostale and "Pugnoides" solon.
2012: Guess at location. On topo map this route was also called 90...

STOP 3. Outcrop in Homer Gulf.
Ponticeras perlatum has been identified from exposures in Homer Gulf. This places the section in the lower portion of the Ithaca formation, probably correlative with the Renwick shale member. The lithology is extremely variable; consisting mainly of gray and reddish shales and siltstones. The fauna contains elements of both the Warrenella and Ithaca biotopes. Particularly common are: Conularia, Plumularia, Mucrospirifer, "Pugnoides", Cupularostrum eximia, Taxocrinus and linguloid brachiopods.

STOP 4. Fitzpatrick quarry ("Frozen Ocean"), north of Omro
This is the northernmost exposure of the Ithaca formation in this area. Here, a series of reddish brown and dark gray shales represents the lowermost Renwick member, and possibly part of the Cornell member of the Sherburne (Smith, 1935). The sparse fauna contains elements of the Naples and Warrenella biotopes. Especially abundant are well preserved specimens of Leiorhynchus mesacostale.

STOP 5. Fall Creek, Ithaca
This exposure, and that of adjacent gorges, constitutes the type section of the Ithaca formation. The sequence displays a complex inter-fingering of at least four of the biotopes that have been discussed.
The top of the Sherburne formation is marked by the presence of the Warrenella biotope (at the base of the falls). The commonest fossils are: Warrenella laevis, Palaeoneila filosa, Pterochaenia fragilis, Chonetes lepida, Taxocrinus ithacensis, Porcellia nias and Styliolina fissurella.
Above, in the lower vertical wall of the gorge is the Renwick member of the Ithaca, a reddish black fissile shale containing a sparse Naples fauna. Lingula complanata, Leiorhynchus mesacostale, Orbiculoidea lodensis and Styliolina fissurella are the commonest fossils.
In the upper portion of the vertical cliffs are gray shales and siltstones representing the Six Mile Creek member, containing a Tropidoleptus fauna with Platyrachella mesastrialis. Rhipidomella vanuxemi, Cyrtina hamiltonensis, Pleurotomaria capillaria and Cryptonella endora.
Above the falls the upper 300' of the Ithaca formation is represented by the Cascadilla and Triphammer members. At the base of the Cascadilla member the Ithaca biotope contains an abundant fauna, primarily of brachiopods. Especially common are: Leptostrophia, Cyrtina, Productella, Atrypa, Schizophoria, Leiorhynchus mesacostale, Cypricardella and Palaeoneilo.
The top of the Ithaca is marked by the recurrence of the Warrenella biotope, which is exposed at Forest Home, above the Cornell campus. Between these two zones are a sequence of virtually barren shales with a sparse Naples fauna, and at least one minor incursion of the Ithaca biotope.
2012: Guess at location.

STOP 6. Hubbard quarry.
This is one of the few places where the contact of the Geneseo black shale and the Sherburne formation can be seen.
The uppermost 6' of the Geneseo carry typical fossils of the Naples biotope: Barriosella spatulata, Orbiculoidea lodensis, Schizobolus truncatus, Leiorhynchus guadracostatum, Pterochaenia fragilis, Ponticeras perlatum, and fish and plant fragments .
In the lower Sherburne the following fossils occur: Chadochonus sp., Leiorhynchus guadracostatum, Loxonema noe, Palaeotrochus praecursor, Panenka sp., brevicone nautiloids and Ponticeras perlatum.
This fauna of mixed benthonic and pelagic types is similar to the "Naples fauna" of the West River shales further to the west. It seems to represent the environments of the Warrenella biotope.

STOP 7. Roadcut on Rte 13, just east of Dryden, Tompkins Co.
This exposure in the lower Triphammer member is one of the most richly fossiliferous outcrops of the Ithaca formation. It contains abundant encrusting epifauna representing the auloporid biotope, with minor incursions of the Ithaca biotope from the west and the Tropidoleptus from the east. Diversity is at a maximum, with maximum size development of Leiorhynchus mesacostale, Atrypa reticularis and Platyrachella mesastralis. Other common fossils are: "Pugnoides" solon, Porcellia nias, Mucrospirifer posterus and Cyrtina hamiltonensis.
2012: Guess at location.

B: UPPER DEVONIAN DELTAIC ENVIRONMENTS
Zeddie P. Bowen and Robert C. Sutton
University of Rochester
A. Lee McAlester and Donald C. Rhoads
Yale University
INTRODUCTION
The Upper Devonian of New York is composed of a lithologically and paleontologically diverse sequence of clastics that have played an historic role in the development of geological thought. Study of these strata resulted in the classical "facies" papers by Chadwick, Caster, Cooper and others in the 1920's and 1930's. In the years since 1940, most work has been concerned with detailed geologic mapping and more precise stratigraphic correlation. These studies have been summarized on the geologic map and Devonian correlation chart of New York State (Broughton and others, 1962; Rickard, 1964).
In New York State, the Upper Devonian marine strata crop out in a generally east-west belt over 200 miles long and extend from Lake Erie on the west to the Catskill Mountains in the east. These strata have been subdivided into seven groups, some of which are marked by thin, persistent black shales that enclose eastward-thickening rock wedges. Within each wedge diverse lithologies and faunas can be recognized and delineated. Moreover, similar lithologic and faunal associations can be recognized in each wedge forming the basis for the facies concept mentioned above. That portion of Rickard's Devonian Correlation Chart (formational and members names omitted) with which this field trip is concerned is shown in figure 1.
In 1965, the writers began an analysis of the Smethport or Chemung facies using both paleontological and sedimentological evidence to reconstruct its paleo-environments. The initial studies were confined to the Sonyea Croup in order to define a set of essentially contemporaneous environments that could be compared with those in modern deltas (Sutton, Bowen, and McAlester, in production). The second or current phase of research has dealt with the post-Sonyea Chemung facies in central and western New York.

B: UPPER DEVONIAN DELTAIC ENVIRONMENTS

STOP 1. Open Shelf (Harford Mills)
Lithology and Structures:
Interbedded gray and dark gray shales, siltstones and mudstones. Small flute casts, groove casts, cross- laminae concretions, tracks and trails
Paleontology (only abundant forms listed)
Shelly fossils relatively rare. Tracks, trails, burrows (7 taxa found, all rare)

STOP 2. Prodelta (Berkshire)
Lithology and Structures:
Mudstone interbedded with siltstone and minor amounts of shale and sandstone. Groove casts, cross- laminations and cuspate ripples.
Paleontology (only abundant forms listed)
Leiorhynchus, Chonetes, Productella, Leptodesma, Ambocoelia Tracks, trails and burrows plus 9 other less common taxa

STOP 3. Platform (Smithboro)
Lithology and Structures:
Mudstone interbedded with sandstone, shale, siltstone, and coquinite. Cross-bedding, laminations, ball and pillow, cuspate ripples, load casts
Paleontology (only abundant forms listed):
Shelly fossil abundant. Atrypa, Cyrtospirifer, Productella, Crinoids, Douvillina, Auloporid corals, Ambocoelia, Cornellites, Schuchertella, Rugose corals, Tylothyris, Plant fragments plus 13 other less common taxa

STOP 4. Delta Front Sands (Glory Hill)
Mostly sandstone with small amounts of shale, mudstone, and coquinite. Cross-bedding, cross-laminations, current ripples, parting lineation, mud chips
Paleontology (only abundant forms listed)
Large shelly fossils abundant. Tracks, trails, and burrows. Productella, Thiemella, Atrypa Nervostroehia(?) Cyrtosperifer, Chonetes, Tylothyris, Crinoids, Douvillina, Auloporid corals, Ambocoelia, Plant fragments, Rhynchonellids, Cornellites plus 8 other less common taxa

STOP 5. Near Shore Facies: Channels, Lagoons, and Levees (Ingraham Hill Quarry)
Sandstone and shales with small amounts of shale-pebble conglomerate. Cross-bedding, linguoid ripples, groove casts
Shelly fossils uncommon. Plant fragments and tracks, trails and burrows abundant, plus 18 other less common taxa.

C: TRANSITIONAL SEDIMENTARY FACIES OF THE CATSKILL DELTAIC SYSTEM IN EASTERN NEW YORK STATE
Kenneth G. Johnson
Skidmore College
INTRODUCTION
One of the greatest thicknesses of Devonian rocks on the North American continent is at the northeastern end of the Allegheny Synclinorium in east-central Pennsylvania and southeastern New York. The sequence crops out along a north-facing escarpment extending from Lake Erie to the Catskill Mountains, a distance of some 300 miles. The escarpment continues south along the west side of the Hudson Valley into the Valley and Ridge physiographic province of the Appalachian highlands. The New York sequence is accepted as the standard for the Devonian System of North America. In the Catskills, although the top has been eroded, the Devonian is some 10,000 feet thick. It thins to about 2500 feet at the western edge of New York State and also thins toward the southwest. In northeastern New York Devonian rocks have been removed by erosion. In New York State the Devonian sequence was only slightly affected by the Appalachian Revolution; it was deformed into gently undulant folds. More intense tectonic forces to the southwest in Pennsylvania folded the same strata into elongate, plunging anticlines and synclines.
The upper Middle Devonian and Upper Devonian of eastern New York and Pennsylvania consist of a thick wedge of continental rocks that have a progradational relationship to marine formations farther west. These rocks have a deltaic character.
The deltaic wedge is composed of detritus derived from a source area east of the present-day Catskill Mountains which was being elevated by the first pulses of the Acadian Orogeny. At the base of the clastics is an interval of some 2500 feet of fossiliferous sandstones and shales (Hamilton Group) which thins toward the west and southwest. Penetrating eastward from the marine basin into the upper Hamilton clastics are two thin fossiliferous limestone beds (Centerfield and Portland Point) which were deposited during the time that the source terrain was in the beginning stages of uplift. The Tully Limestone, a transgressive carbonate tongue at the base of the Upper Devonian, represents the last significant limestone deposition in the New York Devonian prior to the overwhelming of the marine basin by clastic influx.
After deposition of the Tully, uplift apparently accelerated and continued on a large scale into the Mississippian. A thick wedge of clastic continental sediment (Catskill lithofacies) was deposited at the margin of the basin. The red and green-gray sandstones, shales, and conglomerates of this wedge inter-finger westward with littoral and shallow marine (Chemung lithofacies) sandstones and shales. These grade into dark-colored shales and siltstones (Portage lithofacies) farther west that are of deeper marine origin. The irregular, interfingering contact between the continental beds and the marine formations rises stratigraphically towards the west and the continental beds consequently have the appearance of over-riding the marine strata. This prograding relationship, the result of displacement of the late Devonian sea by the expanding clastic wedge, is shown in the cross-section along the N.Y. - Pa. border (Fig. C-l). Dunbar and Rodgers (1957, p. 137-140) give a concise description of the New York Middle and Upper Devonian from the paint of view of the facies concept. A correlation chart by Rickard (1964) shows the relationship of the depositional phases of the Devonian rocks in New York State.
Within the Tully Limestone and its eastern clastic correlatives are rocks that are representative of the spectrum of sedimentary environments that comprised the Catskill deltaic system during early Late Devonian Time. These were studied (Fig. C-2) in order to develop associations of criteria that will permit recognition of sedimentary environment elsewhere in the Catskill complex.

C: TRANSITIONAL SEDIMENTARY FACIES
OF THE
CATSKILL DELTAIC SYSTEM IN EASTERN NEW YORK STATE

Headwaters of Genegantslet Creek.
On right (S) swamp which forms headwaters of south flowing Genegantslet Creek.

On left (N) large outcrop of Chemung Lithofacies.

Cross Canasawacta Creek in South Plymouth

On right (S) large gravel pit in glacio-fluvial sedimentary deposit.

Cross Chenango River

Road cut in Catskill Lithofacies.
On left (N) excellent example of alluvial channel facies (cross-bedded, gray, graywacke) resting on over-bank facies (red shale),

Cross Unadilla River

Descend river terraces.

Center of Morris.
Note stone buildings constructed of Chemung lithofacies flagstone.

On left large gravel pit in glacio-fluvial deposit.

Ahead on left large gravel pit in Kame deposit.

Horizontal Chemung lithofacies
On left in used car lot adjacent to Nick's Diner horizontal, very thin bedded Chemung lithofacies containing abundant spiriferid brachiopods.

On right view of glacial deposits in mouth of Charlotte Valley.

On right across valley very large gravel pit in Kame terrace.

STOP 1. Flow rolls in Lithosome C.
This outcrop contains an example of the flow-rolls which are locally common in Lithosome C. The flow-rolls occur as beds of internally disturbed structure underlain and overlain by horizontal, well-bedded strata. Within the flow-roll beds are nodule-shaped, concentrically laminated masses of medium gray, very fine-grained sandstone enclosed in slightly darker colored siltstone. The laminar structure is due to concentric, extremely thin, dark laminae composed largely of very fine plant fragments. The enclosing siltstone commonly has a diapiric relationship to adjacent pillows. This outcrop is at the distal edge of the nearshore (bar and lagoon) facies.

Kame and Kettle topography.

Passing through Kame and Kettle topography.

On left well defined river terrace.

On right outcrop of dark Gilboa Formation shale.

Grand Gorge

STOP 2. Hardenburgh Falls
On right power sub-station. Park and walk down unsurfaced road across from power station.
The beds here are medium gray and olive gray, trough cross-bedded, fine to medium-grained, graywacke and medium gray, shaly siltstone of Lithosome C. Pebble and coquinoid conglomerate lenses, rich in plant fragments, are common. The strata are interpreted as being of tidal channel and tidal flat origin.

Kame (?) topography.

Cross Schoharie Creek.

On right sandstone ledges of Catskill lithofacies (Lithosome D).

On right more sandstone ledges of Catskill lithofacies.

STOP 3. Manor Kill Gorge
The beds exposed in the Manor Kill Gorge are within the upper part of the Hamilton Group. Those in the lower part of the section, adjacent to the Schoharie Reservoir, are trough cross-bedded, burrowed, medium-grained sandstone of Lithosome C assigned to the tidal channel facies. Some of these sandstones are rich in plant material and in a few places during low water stages of the reservoir fossil seed-fern stumps may be seen. The remainder of the section upstream consists of interbedded red and green shales, dark gray shales and medium gray, shallowly cross-bedded, fine-grained sandstone; interpreted, respectively, as distal alluvial plain, tidal flat and tidal channel facies. Walk down path on left (W) side of road to east bank of reservoir at mouth of Manor Kill to observe cross-bedded, burrowed sandstone.

On left Gilboa Dam constructed mainly of tidal channel (and bar?) sandstone of Lithosome C.

STOP 4 Display of Gilboa seed-ferns
Display of Gilboa seed-ferns taken from quarry (abandoned) a short distance back in woods. Over 200 such seed-fern stumps were taken from this quarry. They apparently represent a distal alluvial plain or tidal swamp which was buried by shifting tidal channel sands.

STOP 5. Graywacke
Park on right side of road opposite outcrops near base of steep hill. Outcrop consists of medium gray and olive gray, tabular and trough cross-bedded, fine to medium-grained, immature graywacke. The sandstone contains well-developed lag accumulations of large spiriferid brachiopods and a few large burrow structures. The sandstone is interpreted to represent a tidal channel deposit.

STOP 6. Lithosome D
Park on right opposite red beds.
Outcrop consists of grayish red, highly micaceous siltstone and silty, very fine-grained sandstone of the overbank alluvial facies (Lithosome D). Dark greenish gray mottles are common in these beds.
Resting in channel contact on the red beds is well cross-bedded, apparently unfossiliferous, medium gray, very fine-grained sandstone and olive-gray, fine-grained sandstone. Within this 30 foot sandstone interval is a well-developed compound channel that migrates to the right (SW) upward in the section.

D: PALEONTOLOGY, STRATIGRAPHY, AND PALEOECOLOGY OF THE LUDLOWVILLE AND MOSCOW FORMATIONS (UPPER HAMILTON GROUP), IN CENTRAL NEW YORK
Thomas X. Grasso
Monroe Community College
Rochester, New York
Introduction
The Middle Devonian Hamilton Group of New York State is structurally simple and highly fossiliferous, thereby lending itself to detailed stratigraphic and paleontologic studies.
The writer (1966) examined the Hamilton sequence in the Tully Valley to determine the sequence of lithologies and faunas. The zones thus determined were compared with those defined by Cleland (1903), who made a similar study of the Hamilton Group along the Cayuga Lake meridian, 30 miles west of the Tully Valley (Fig. D-1). A paleoecological interpretation of the Hamilton rocks of the Cayuga Lake region was made by Fernow (1961).
This trip was repeated as trip H.

D: PALEONTOLOGY, STRATIGRAPHY, AND PALEOECOLOGY OF THE LUDLOWVILLE AND MOSCOW FORMATIONS (UPPER HAMILTON GROUP), IN CENTRAL NEW YORK

Roadcut on east side of 1-81 is in the Upper Dev Ithaca Fm.

STOP 1. Roadcut on east side of U.S. Rt.11
Elevation 1280': .3 miles north of the junction of N.Y. Rts. 80 and 11 (Tully Quad.).
Exposed thickness: Windom Member 35'
The top of this exposure is stratigraphically below the Windom outcrop on Kingsley Road (STOP 5). The Windom at this locality (STOP 1) is approximately 100 feet below the base of the Tully Ls and is fossiliferous.

STOP 2. Roadcut, on west side of LaFayette Rd
Elevation 1330': Roadcut, on west side of LaFayette Rd. just before the bend in this road, about .4 miles northwest of LaFayette (Jamesville Quad.).
Exposed thickness: Otisco Member 30'
This exposure of the Otisco is stratigraphically above the Joshua Submember and below the Ivy Point. It is extremely fossiliferous. Mucrospirifer mucronatus, Spinocyrtic granulosa, Athyris spiriferodes, Megastrophia cava are some of the brachiopods, Cornellites flabella, Modiomorpha mytiloides, Pseudaviculopecten princeps, Paleoneilo constricta, Cypricardella bellistriata are some of the pelecypods found here.

STOP 3. Base of WSYR TV Tower on Miller Hill
Elevation 1400'; Base of WSYR TV Tower on Miller Hill, .3 miles southwest of the intersection of Sentinel Heights Road and Bull Hill Roads (Jamesville Quad.).
Exposed thickness: Joshua Submember 15.5'
Numerous solitary rugose corals occur here such as Cystiphylloides, Siphonophrentis, and Heterophrentis. The colonial rugose coral Eridophyllum sabcaespitosum is also abundant.

STOP 4. Lords Hill, on N.Y.80
Elevation 1380': Lords Hill, on N.Y.80, south of the junction with U.S.20 (South Onondaga Quad.).
Name | Exposed Thickness | Elevation | Notes
Portland Point Member | 10' | |
Owasco Member | 2' | Elev. 1380' |
Spafford Member | 2' | |
Ivy Point Member | -not measured | | -small exposures on both sides of road
Joshua Submember | -70' (projected) | Elev. of top 1280' | (Oliver, 1951)
Joshua corals are found in the regolith on both sides of the road. The Owasco contains an abundance of Allanella tullius and Mucrospirifer mucronatus. The basal crinoidal layer of the Portland Point nests directly on top of the Owasco Member. This is succeeded by 9 feet of interbedded shales and thin limestones.

STOP 5. Roadcut. on both sides of Kingsley Road
Elevation 1500': Roadcut. on both sides of Kingsley Road just west of the intersection of Hitchings Rd. (South Onondaga Quad.)
Exposed thickness: Windom Member 28'
The top of this exposure is about 20 feet below the base of the Tully Limestone. The Windom here is unfossiliferous.

STOP 6. Peppermill Gulf
Elevation 1050': Peppermill Gulf, parallel to and just east of Hogsback Rd., 1.3 miles west of the junction of U.S.20 and N.Y. 8O (South Onondaga Quad.).
Exposed Thickness: Centerfield Member 30'
Butternut Member --
A waterfall just north of U.S.20 exposes approximately 30 feet of Centerfield. The Butternut - Centerfield contact is gradational - is therefore difficult to establish. The Centerfield is a coarse siltstone at this locality. Fossils are difficult to extract because of the lack of good bedding plane exposures.

STOP 7. Moonshine Falls on Paines Creek
Elevation 475' : Moonshine Falls on Paines Creek, 1 mile south of Aurora (Sheldrake Quad.). Unnamed gravel road on right leading downhill to a bridge over Paines Creek -Walk down road to Paines Creek and then downstream
Exposed thickness: Ledyard Member --
Centerfield Member 25'
Centerfield at this locality is abundantly fossiliferous with numerous species of brachiopods, pelecypods, corals, and bryozoans. The Ledyard Member sharply overlies the Centerfield and carries a fauna of small, thin shelled pelecypods and brachiopods. The contact between these 2 units occurs just upstream from the waterfall.
2012: Bridge was visible in 1995 image.

STOP 8. Black Rock on Paines Creek
Elevation 720': (Sheldrake Quad.).
| | Exposed thickness:
| Dense fossiliferous shale | 28"
Portland Point Member | Blue-gray fossiliferous shale | 8"
| Basal crinoidal layer | 16 -20"
King Ferry Member | | 8'
The lip of the falls is 8 feet lower than the base of the crinoidal limestone, therefore the uppermost King Ferry is accessible here. The Portland Point is very fossiliferous containing numerous brachiopods, pelecypods, ostracodes, crinoids and trilobites.

STOP 9.Portland Point Quarry on east lip of Cayuga Trough
Elevation 620': (Ludlowyille Quad.).
Exposed thickness: |
Geneseo Black Shale | 15'
Tully Limestone | 16'
Windom Member | 5'
This locality is one of the most fossiliferous exposures along the Cayuga Lake meridian. Numerous corals, bryozoa, crinoids, brachiopods, pelecypods, trilobites, and gastropods are found in the upper 5 feet of the Windom. (see Guidebook -31st Annual Meeting N.Y.S.G.A. 1959 Ithaca, N.Y.)
At the south end of the quarry a thrust fault overthrust to the northwest occurs in the Tully Limestone and has drag folded the upper Windom at this locality.
On the east side of the quarry an alnoite dike about 1 foot thick occurs in one of the N-S joints.

STOP 10. Roadside quarry on Portland Point Road
Elevation 460': (Ludlowville Quad.),
Exposed thickness:
King Ferry Member --
The King Ferry Member exposed here is about 20 feet below the Portland Point Member.

E: MINERAL INDUSTRIES IN PARTS OF ONONDAGA, CORTLAND AND TOMPKINS COUNTIES
Newton E. Chute
Syracuse University
Central New York has had important production of industrial minerals and rocks for many years. In 1967 (Minerals Yearbook) the order of value of these products in Onondaga County was as follows:
1st Salt
2nd Lime
3rd Stone (also 3rd county in state)
4th Cement
5th Sand and gravel
6th Clays
Industrial minerals and rocks now being produced in the field trip area are described briefly. Those formerly produced are discussed in the following section.
Repeated as Trip I

STOP 1. Finger Lakes Stone Company's sandstone quarry
The quarry is in the upper part of the Enfield Formation which is about 650 feet thick in the Ithaca area. Layers of sandstone alternate with layers of shale in the quarry. Slabs of sandstone are obtained without blasting by drilling holes on seams and separating them with wedges. The slabs are cut to the required sizes in the mill by diamond and wire saws. Pieces with good joint surfaces are used for seam face stone. Those with sole markings on bedding surfaces are used for special surface effects. The stone is laid in various patterns with different finishes, as illustrated by the exterior of the company's office at the quarry.

STOP 2. Quarry of the Cayuga Crushed Stone Company
This is the old quarry in the Tully Limestone and the Geneseo Shale that was worked by the Penn.-Dixie Cement Company until 1948. The quarry is on the crest of the Portland Point anticline above the Cayuga Rock Salt Company's mine. The Cayuga Crushed Stone Company reopened the quarry and has worked it for a number of years.
The Tully Limestone, which is 16 to 18 feet thick at the quarry, is underlain by fossiliferous Moscow Shale of Middle Devonian age and is overlain by unfossiliferous Geneseo Shale of Upper Devonian age.
Two peridotite dikes have been known in this quarry for many years. They are marked on a map in the guidebook for the 31st annual meeting of the N.Y.S.G.A. sponsored by Cornell University in 1959. One is shown to extend for about 1700 feet across the southeastern part of the quarry.
A dike, 1'5" thick, is presently exposed in the southern part of the quarry face and for about 100 feet on the quarry floor. It diminishes in thickness to about 6 inches near the south end of the exposure. The dike is vertical and strikes N 5 to 10 degrees W parallel to a prominent set of joints about at right angles to the axis of the Portland Point anticline .
The first description of a peridotite dike in this quarry was by Sheldon in 1921. Other descriptions are by Martens (1924) and Broughton (1950).
A cluster of six or seven dikes each 6" to 8" thick was observed recently in the middle part of the quarry face by J.J.Prucha. He also knows of at least eight peridotite dikes in the salt mine below the quarry (personal communication, April 1970). Martens (1924) described this dike rock as kimberlite or alnoite depending upon the presence of melilite, an essential constituent of alnoite. Broughton (1950) did not observe any melilite in the thin sections he examined and called the rock kimberlite .
Of particular interest at this quarry is the unusual thickness of glacial overburden and shale that it is economical to strip to quarry the limestone. At the south end of the quarry in particular, the depth of the stripping is several times greater than the thickness of the limestone quarried. The favorable location of the quarry for marketing stone in the southern part of the state is an important factor in making the unusual depth of stripping possible. Small quarries have been worked in the Tully Limestone in various places in central New York in the past, but this is the only one worked in recent years.

STOP 3. Salt mine shaft and Cement Plant
The Cayuga Rock Salt Company's mine shaft and the former plant of the Penn.-Dixie Portland Cement Company.
A brief stop will be made to observe the headframe of the Cayuga Rock Salt Company's mine and the remains of the old cement plant on the lake shore.

STOP 4. Brine well field
Brine well field of the Solvay Process Division of the Allied Chemical Corporation.
Brine is obtained from wells about 1100 to 1200 feet deep that penetrate salt beds in the Syracuse Formation of the Salina Group. The brine is piped to the company's plant at Solvay for the manufacture of soda ash and chemicals.
A tour of the brine field will be conducted by Mr. Michael Slexak who is a geological engineer with the Solvay Process Division.
2012: Location is uncertain.

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

STOP 6. Limestone quarry
Limestone quarry of the Solvay Process Division of the Allied Chemical Corporation, located on the north side of the Seneca Turnpike just east of Jamesville.
This is one of the largest limestone quarries in the state and provides a good illustration of selective quarrying. The rock units quarried are as follows:
Onondaga Limestone Formation
Moorehouse Member
Nedrow Member
Edgecliff Member with several feet of sandstone at the bottom
Manlius Limestone Formation
Pools Brook Member
Jamesville Member
Clark Reservation Member
the quarry floor is at the top of the Elmwood Member below the Clark Reservation Member
The Clark Reservation, Jamesville, Pools Brook, and the noncherty part of the Edgecliff member have the highest purity, and they are quarried for use by the Solvay Process Division for kiln stone and for cement manufacture by the Alpha Portland Cement Co. The Onondaga Limestone above the Edgecliff Member is quarried for crushed stone. The sandstone at the base of the Edgecliff Member and the cherty part of the Edgecliff are stripped separately and wasted.
The Tioga Metabentonite, which is about 8" thick, overlies the Moorehouse Member and separates it from the Seneca Member above. The metabentonite is unsatisfactory in crushed stone and is stripped along with some of the Seneca Member where they occur at the south edge of the quarry.
Two reverse faults that strike about N 70 degrees W and dip southward offset the beds in the quarry a few tens of feet. Fluorite and calcite crystals have been found in fractures along the fault zones.
Additional points of interest to be seen on this quarry property are an old lime kiln, an old quarry worked for Elmwood argillaceous dolomite used for natural cement manufacture, and part of an old gypsum quarry in the Forge Hollow Formation of the Bertie Group.

STOP 7. Split Rock quarry
STOP 7. Split Rock quarry located at the west end of Split Rock Gulf Road about 0.7 mile southwest of the junction of Route 173 and Onondaga Blvd.
This quarry illustrates the influence of the unconformity at the base of the Onondaga Limestone on the amount of limestone available for quarrying. Here the Edgecliff Member of the Onondaga overlies Elmwood A unit of the Elmwood Member. The Clark Reservation, Jamesville and Pools Brook limestones, seen at the Solvay Process Division's quarry, were eroded prior to the deposition of the Onondaga Limestone.
Most of the floor of the bottom part of the quarry is on the top of the Rondout dolomite, about 33 feet of Olney and Thacher Limestone overlie the Rondout. Two or three stromatolite zones and a dolomite bed are present in the lower part of the Thacher. The upper part of the Thacher and the Olney are mainly the "drab and blue" type of alternating thin beds of dolomitic brownish weathering and purer gray weathering limestone. The Edgecliff Limestone at the top of the south side of the quarry contains some small coral reefs a few feet to a few tens of feet in diameter.

STOP 8. Syracuse Pottery Company plant and clay pit.
The plant is on the west side of Pottery Road about 0.9 mile north of its junction with Route 173 and 2.2 miles east of Warners.
This company, which manufactures mainly flower pots and urns from glacial clay dug a short distance west of the plant, has been operating nearly continuously since about 1875. The clay is dug to a depth of 8 feet after stripping 6 to 10 inches of topsoil. The part of the clay bed under a swamp has different firing characteristics from the part on higher ground. The part under the higher ground has been partly leached of calcium carbonate and this apparently causes the clay to burn redder and to shrink more than the clay from below the swampy area. These two types of clay are blended to obtain the desired firing characteristics.
After the flower pots are molded by presses, they are fired in a tunnel kiln at a temperature of 1800 degrees F. Some of the pots are glazed and some are coated with colored enamel.

STOP 9. Old portland cement plant and marl pits
The old portland cement plant of the Empire Cement Company and the marl pits. Ruins of the old cement plant can be seen on the north side of the old Erie canal a few hundred feet west of Newport Road at Warners. The water-filled marl pits are west of the plant between the canal and Canal Road.
This cement plant is historically significant, because it was one of the early portland cement plants and because marl was used as a source of calcium carbonate. The plant was first built in 1886, and operated until about 1908. Depletion of the supply of marl suitable for cement manufacture may have been a factor in the plant closing. Two other cement plants that used marl were operated for a short time in this region. One was the American Cement Company's plant about 5 and 1/2 miles west of Warners and the other was at Montezuma north of Cayuga Lake.

STOP 10. Plant of the Onondaga Lightweight Aggregate Corporation
Plant of the Onondaga Lightweight Aggregate Corporation located about 0.6 mile east of Warners on the north side of the railroad.
Lightweight aggregate has been produced here since 1954. Some years previously the plant was used by the Onondaga Brick Corporation for the manufacture of building brick. The raw material is Vernon Shale obtained from an old quarry about half 8 mile north of the plant (Stop 11). After crushing the shale is sized, mixed with coal, and sintered on a sintering machine at 2400 degrees F. The sintered chunks are crushed and screened to four sizes for marketing. This plant is said to be one of the first lightweight aggregate plants in New York State. The product is marketed widely, especially in the central part of the state.

STOP 11. Vernon Shale quarry
Vernon Shale quarry of the Onondaga Lightweight Aggregate Corporation located in the hillside on the north side of Brickyard Road about half a mile northeast of Canton Street in Warners.
The quarry, which probably is in the upper part of the Vernon, exposes 25 to 30 feet of red and greenish gray shale. Gypsum nodules are present in the shale in places and also some small shiny black crystals of specular hematite. Usually the hematite crystals are associated with cavities that probably contained gypsum or salt. Some of the cavities are molds of salt hopper crystals. In places the red shale contains very irregular patches of the green shale suggesting partial decolorization of the red shale.
This quarry is one of the few places in central New York where more than a few feet of the Vernon are well exposed for examination.

STOP 12 . Gravel pit
Gravel pit on the south side of Lake Road, opposite the south end of Green Lake, about a mile west of Tully.
The pit is close to the Valley Heads moraine near Tully and has some interesting features. The gravel in the pit appears to have come from two different sources. probably because of diversion around the ice block that stood in the position of Green Lake. The gravel in the western half of the pit came from the northwest and is much lower in shale than the gravel in the eastern half which cross bedding and imbricate structure show came from the northeast. Shale is abundant in a layer 2 to 4 feet thick near the middle of the face on the east side.

STOP 13. Alluvial Fan at Preble
Stop on Route 281 at Preble to view the alluvial fan built in the main valley at the mouth of Otisco Valley.

STOP 14. Gravel pit operated by the Cortland Ready Mix Company.
This pit is on the west side of Route 11 about a mile north of the Homer city line. Entrance to the pit is opposite the end of Health Camp Road.
This pit, and the pit of the Concrete Materials Corporation nearby on the east side of Route 11, illustrate the kind of gravel available in this part of the valley of the West Branch of the Tioughnioga River. Gravel and sand are dug to a depth of about 40 feet below which is a thick deposit of silt and clay. Most of the gravel is dug from below water and is not weathered.

STOP 15. Gravel pit in a kame
Gravel pit in a kame on the northwest side of the valley of the east branch of the Tioughnioga River, about a mile northeast of Route 81. This pit provides a good illustration of the Olean type of gravel which is characterized by much local shale and siltstone. This type of gravel is of very poor quality and is usable mainly for fill. Varved clay exposed on the side of the kame may indicate the presence of a lake in the valley after the kames formed.

F: DEGLACIATION OF THE EASTERN FINGER LAKES REGION
James Kirkland
State University of New York at Binghamton
Acknowledgments
The writer is indebted to Dr. James Bugh at the State University of New York College at Cortland and Or. Donald Coates at the State University of New York at Binghamton for their encouragement and criticism.
Regional Setting
The field trip area is located in central New York State and comprises parts of the Tully, Otisco Valley, Truxton, Homer, Sempronius, and Cortland 7.5 minute U.S.G.S. topographic quadrangles. This region consists predominately of gently southward dipping Devonian shales with an east-west system of broad anticlines and synclines (Tarr, 1909).
There is wide disagreement in the literature concerning residuals from preglacial erosion.
Durham (1954) described three erosion surfaces in the surrounding region, the highest or Schooley Peneplain at 1600 to 1999 feet, the next between 1500 and 1700 feet, and the lowest between 1100 and 1300 feet. He further considers only the Schooley Peneplain to be a true peneplain and the others to be the result of structural control by resistant strata.
Denny (1956) concluded that remnants of former peneplanation have been reduced.
Muller (1965) stated that summit accordance is valid only if summit reduction by glaciation is light and that " ... summit contours generalized to a six mile grid give an impression of imperfect summit accordance." (1966)
Clayton (1965) stated: "... the whole of the relief near the Finger Lakes is the work of ice, and is quite independent of the form of the preglacial landscape. The destruction of that earlier landscape is almost complete, ... "
The present form of the topography is probably the result of multiple cycles of glaciations and interglacials (Coates, 1966) with erosion by late Wisconsinan glaciation contributing little to the present bedrock form of the topography.

F: DEGLACIATION OF THE EASTERN FINGER LAKES REGION

State University College at Cortland
The campus of the State University College at Cortland is situated on a bedrock hill or umlaufberg which rises 110 feet above the surrounding outwash plain. The knob represents an extension of the ridge extending northeast from Cortland. Muller (1966) attributes the formation of the knob to ... "Concentrated glacial scour at the south end of the Tully-Cortland trough effected the reducing and isolating of the knob. Aggrading valley fill completed separation of knob from upland."
Query: How many cycles does the formation of the knob represent and what effect have fluvial processes had in its formation?
The valley fill underlying Route 13 is composed of two gravel units, each approximately 50 feet thick, separated by 100 feet of sand and silt. The intermediate unit presumably represents conditions of low gradient and restricted drainage south across the Tioughnioga col. The upper gravel relates to deposition of coarse outwash aggrading east-north eastward from the Valley Heads moraine just west of South Cortland.

Crossing South Cortland outwash plain
Proceed past Munsons Corners crossing South Cortland outwash plain, rising southwest at about 20 feet/mile. Several streamlets from the till slope to south disappear into this permeable coarse gravel plain.

STOP 1. South Cortland Kames
Active borrow pits in kame complex on south flank of valley expose structure of ice disintegration deposits comprising a linear ridge which is relatively smooth on the distal slope but with massive kame-like aspect to the northwest. Lateral variability of sorting and coarseness is characteristic. The gravels are characterized by crystalline-carbonate-clastic relationship of about 5:15:80 which is representative of through valley drift in this area. The kame complex contains sections of highly cemented gravels. What does this indicate about carbonate leaching and ground water conditions?

Ice contact face of kame terrace
Descend sharply on ice contact face of kame terrace, into complex of ice disintegration deposits marking stagnant toe of north-eastward trending Valley Heads ice tongue.

Continue north through Gracie across ice disintegration complex.

Cross abandoned meltwater channel
Cross abandoned meltwater channel cut by stream flowing from melting ice blocks responsible for the Fish Hatchery kettles.

Post glacial lake
Cross Otter Creek. Note lake of post glacial modification of outwash plain.

Alluvial fan of Dry Creek.
Turn left (W) onto Kinney Gulf Road built largely across alluvial fan of Dry Creek.

Start of Kinney Gulf
Dry Creek and road pass through narrow rock-walled gorge which shortly opens out to form Kinney Gulf.

Valley Heads moraine
Rise across outwash to well-defined Valley Heads valley-stopper moraine which forms divide between Dry Creek (Susquehanna drainage) and headwaters of Fall Creek (St. Lawrence drainage).

Glacial striae oriented S45W
Carney (1909) reported glacial striae to be oriented S45W on summit of west Hill to north of intersection.

Glacial striae oriented S71E
On summit of southeast end of Summer Hill west of route, Carney (1909) reported glacial striae to be oriented S71E, indicating opposing directions of ice flow during late Wisconsin Stage.

Cross small tributary of Fall Creek which drains Lake Como.

Intermorainal Basin
To northwest (left ahead) the valley floor opens out as an inter-morainal basin, part of which is occupied by Lake Como. Lower slopes enclosing the basin on north and east are marked by strong kame and kettle development.

Start of Homer Gulf
Proceed across nose of stagnant ice deposits at drainage divide, before entering Homer Gulf, a canyon incised 300 to 500 feet deep.

STOP 2. Homer Gulf
Post-glacial modification of the upper part of the Gulf is minor, and latest gorge-cutting relates to Valley Heads glaciation.
Note the fan deposited by water from Homer Gulf in the Skaneateles trough.
Query: Is this gulf a product of a single episode of gorge-cutting? Is the moraine position on the divide co-incidental?

Skaneateles trough
Proceed north over outwash and postglacial alluvial fan deposits of Skaneateles trough.

Cross Valley Heads terminal moraine.
Road follows an open, irregular channel cut by meltwater during wasting of stagnant toe of the Skaneateles ice tongue.

STOP 3. Ripley Hill Summit
At elevation of 1986 feet above sea level Ripley Hill is one of the highest points in Onondaga County and representative of the heavily scoured but relatively unreduced remnants of an essentially accordant preglacial summit surface. If pre-glacial summit accordance is accepted, the present departure from summit accordance affords a measure of summit reduction by glacial scour. Elongation of ridges commonly relates to ice-flow. Through valleys, long interpreted as showing a pattern inherited from pre-glacial stream systems, have recently been referred to as "intrusive troughs" implying only minor dependence on inherited pre-glacial controls.

Road parallels Cold Brook
The road parallels Cold Brook, a southward draining stream tributary to the Tioughnioga River.

STOP 4. Dwyer Park Gravel Pit
The upper 3 feet of stratified outwash has been interpreted on the basis of heavy mineral studies to represent the last or Valley Heads phase of Wisconsinan Glaciation while the lower approximately 8 feet of gravel represents the earlier Binghamton phase.

Mount Toppin
On the west side of the valley is Mount Toppin, which Von Engeln (1921) refers to as a truncated spur, the result of glacial scour. Holmes (1939) accounts for the over steepened appearance of
the east facing valley wall by differential insolation and therefore greater deposition on the east side of the valley .

STOP 5. Otisco Valley fan.
South of Preble is evidence that the ice tongue in Otisco Valley was active for a longer time than the ice in the Tully-Cortland trough. A fan was deposited by waters from Otisco Valley over the outwash from the Tully Moraine. Note that the southern part of the fan is a collapsed surface. Buried ice must have extended into the valley with melting and collapse in progress as glacial water was distributing the fan material.

Outwash materials of the Tully-Cortland trough
Continue north on Route 281 on the outwash materials of the Tully-Cortland trough. The road trends to the east side of the valley to skirt the Tully Lakes kame and kettle complex on the west side of the valley.

Tully Moraine
Proceed west onto the Tully Moraine, parallel to steep slope marking the proximal border of the moraine. Kettles are to be seen on both sides of the road.

STOP 6. Solvay Gravel Pit
Steep-walled gravel pit exposes materials composing major part of Tully moraine, showing it to be largely a product of outwash deposition from a stationary to narrowly oscillating ice margin. Exotic component in this through valley gravel is high with crystalline-carbonate-clastic ratios on the order of 10:40:50. The "bright" character of the gravels results from proximity to carbonate sources, attrition of diluting shale fraction from the lake plain, and effectiveness of glacial transport in a major through valley.
Query: How can we account for this ratio in view of the 5:15:80 ratio found at the Cortland kames?

Choker moraine
About 0.5 mile east of Tully cross low, smoothed valley choker moraine, convex eastward. This moraine may correlate with the "advance Valley Heads" position defined in Tully Valley by the outer border of the Tully Lakes area. If so, the smoothed nature of this ridge is puzzling, but may relate to impounding at the ice margin.

Valley Heads moraine
Near Markham Hollow Road enter Valley Heads moraine complex of Butternut trough. Proximal margin of moraine is less sharply defined than in Tully Valley. "Main Valley Heads" position is south of Apulia Station.

The Apulia-Fabius trough
The Apulia-Fabius trough extends eastward for several miles. Although segmented by drift deposits that define the heads of several drainage basins, this valley has the continuity suggestive of origin as part of a south-westward draining pre-glacial stream system.

Cross moraine ridge.
Cross moraine ridge. Toward axis of north-south through valley this ridge separates into three small but well-defined ridges marking recession of "advance Valley Heads" ice. The road follows a marginal meltwater channel between moraine ridge and valley wall.

Labrador Pond
Meltwater channel widens, opening onto outwash plain upon which shallow Labrador Pond is located. valley floor is less than 0.5 mile wide between 750 foot walls which converge southward as though toward a bedrock col. Labrador Pond, however drains southward by Labrador Creek on gradient developed by outwash deposition.
Query: How does the transverse relationship of the Apulia-Fabius trough and the Butternut-Labrador trough clarify the relative importance of inherited valley system as opposed to glacier scour in determining the through valley pattern of this part of the plateau?

Cross Shackham Brook.
State reforestation area and experimental drainage basin to east of route. Kame complex developed in valley wall re-entrant where Shackham Brook debouches into Labrador trough.

STOP 7. Truxton town highway department borrow pit.
Stratified sand and silt, with foreset beds and collapse structure. Dominance of shale in gravel, with small percent of crystallines and carbonates indicates dilution by uptake of local rock material. Rapid attrition of such material with fluvio-glacial sorting might within a few miles of through valley transportation "brighten" even this drab gravel, giving it a Binghamton-type lithology.

Truxton, birthplace of J.J McGraw
Truxton, birthplace of J.J McGraw, for 30 years manager of the New York Giants.

East Homer
Continue southwest through East Homer settled by Revolutionary War veteran John Albright in 1827. Route 13 lies along valley of East Branch Tioughnioga Creek, apparently a major tributary of the pre-glacial drainage line inferred to have extended west from Cortland toward Cayuga trough.

Kame terrace
Continue southwest past East River, on Route 13 toward Cortland. Coarse kame terrace gravels exposed in several pits in next three miles.
Note that the East Branch Tioughnioga Creek is diverted to the south side of the valley by the alluvial deposits of the south flowing tributaries. Since the recent floodplain deposits are generally less than eleven feet thick, the fan-shaped deposits are now being eroded and there is a general lack of new fan deposition, the East Branch Tioughnioga Creek must have been diverted by these fans shortly after the ice melted from the valley,

Esker parallels Route 13
Esker parallels Route 13 south of Light House Road where John Miller built first cabin in 1792.
Note that the East Branch Tioughnioga Creek is diverted to the south side of the valley by the alluvial deposits of the south flowing tributaries. Since the recent floodplain deposits are generally less than eleven feet thick, the fan-shaped deposits are now being eroded and there is a general lack of new fan deposition, the East Branch Tioughnioga Creek must have been diverted by these fans shortly after the ice melted from the valley,

STOP 8. Gravel pit in coarse till.
The till was part water-laid and there is outwash material at the south end of the cut.
Continue southwestward on Route 13 passing gravel pit with well stratified sediments on the right (N) in 0.9 miles.

West Branch of Tioughnioga Creek.
Draining the Tully-Horner-Cortland trough, this creek joins the East Branch of Tioughnioga Creek 0.5 miles east. The combined discharge drains south in a through valley with converging walls indicative of a pre-glacial divide a few
miles south of Cortland.

G: PALEONTOLOGY OF THE CORTLAND AREA
Jonathan W. Harrington
The University of Calgary
All of the exposures visited on this trip are in the Ithaca formation. The participant is referred to the discussion on benthic communities of the Geneseo Group (Trip A).

STOP 1. Roadcut on Rte 81, 3 miles south of Cortland
This exposure represents the Grammysia biotope in the Smethport depositional phase. Lithology is highly variable with shales, and ripple-marked and cross-laminated siltstones and fine sandstones. Coquinite lenses, especially with Cupularostrum, are frequent and usually show distinct size-sorting and differential accumulation of valves. Areas of high currents are dominated by the infaunal filter-feeder, Grammysia, and the byssally attached bivalve, Goniophora. Occasional vertical burrows may be seen.
Sheltered areas support an abundant epifauna of crinoids (Decadocrinus and Acanthocrinus) and occasional brachiopods. This environment is characterized by the accumulation of plant fragments and orthoconic cephalopods, and by the scavengers - the gastropods, Pleurotomaria several asteroids (Urasterella, Lepidasterella) and ophiuroids.
The orientation of many of the smaller crinoid calices (inverted with free arms outspread) indicates very slight water agitation. However the preservation of fragile specimens such as asteroids and the scyphomedusa, Plectodiscus cortlandensis, requires periodic rapid sedimentation. Fecal material is occasionally found at this outcrop. It has tentatively been identified as Tomaculum problematicum, a form not previously reported in North America.

STOP 2. Outcrop in Homer Gulf on Rte 41A.
Ponticeras perlatum has been identified from exposures in Homer Gulf. This places the section in the lower portion of the Ithaca format1on, probably correlative with the Renwick shale member in the Cayuga Lake meridian.
Lithology is extremely variable; consisting mainly of gray and reddish shales and siltstones. The fauna contains elements of both the Warrenella and Ithaca biotopes. Particularly common are: Conularia, Plumularia, Mucrospirifer, "Pugnoides", Cupularostrum eximia, Taxocrinus and linguloid brachiopods.

STOP 3. Small outcrop
Small outcrop on the west side of Cosmos Hill, 1 1/2 miles northwest of Cortland.
At this outcrop shales and fine siltstones of the Smethport phase are exposed. The fauna is that of the Leptodesma biotope, with abundant epifaunal filter-feeding faunas.

STOP 4. Roadcut on Rte 81 at Homer, Cortland Co.
The sequence here consists of alternating dark shales and fine siltstones, occasionally ripple-marked. The sparce fauna, representing the Leptodesma or Grammysia biotope, consists of rare brachiopods and occasional crinoids (Acanthocrinus). At several horizons are colonies of the hexactinellid sponge, Actinodictya placenta. These fragile forms were almost certainly preserved in situ.
Small hillside quarries immediately north of this exposure have yielded Ponticeras perlatum. Thus, indicating a correlation with the lower portion of the Ithaca (Renwick or Six Mile Creek Members) in the Ithaca meridian.

J: PROGLACIAL LAKE SEQUENCE IN THE TULLY VALLEY, ONONDAGA COUNTY
Thomas X. Grasso
Monroe Community College
Rochester, New York
Introduction
Few locations in the New York State display as varied an array of geological features as does the Tully Valley.
The Tully Valley is a glacially scoured trough carved into the northern margin of the Appalachian (Allegheny) Plateau (von Engeln, 1921). The glacial erosional and depositional features found here have been the subject of a number of theses and publications (Fairchild, 1909, 1932; von Engeln, 1921, 1959; Brainerd, 1922; Faltyn, 1957; Durham, 1958; Muller, 1964) .
Most of the valley lies within the outcrop belt of the Middle Devonian Hamilton Group. Unlike similar steep-sided troughs to the west, the Tully Valley does not now contain a finger lake. Because of the relatively low temporary base level, due to the absence of a lake, tributary streams have opened excellent exposures even in the lower formations of the Hamilton Group. East-west tributaries, in hanging valleys have carved deep, post-glacial, bedrock gorges, wherein the extremely fossiliferous Hamilton rocks are easily accessible. Therefore, the Tully Valley is also a highly stimulating region for the paleontologist and stratigrapher.
The purpose of this narrative is to outline the proglacial lake sequence of the Tully Valley as indicated by correlating the elevations of the delta masses deposited in these lakes with those of the abandoned outlet channels southeast of Syracuse.
This report is a compilation based mostly on the work of previous investigators and the examination of topographic maps. It should not be misconstrued as the final authoritative explanation of the apparently simple, but actually complex late Pleistocene history of the Tully Valley.

J: PROGLACIAL LAKE SEQUENCE IN THE
TULLY VALLEY, ONONDAGA COUNTY

Kettles more numerous on west side.
Notice along the route that kettles are more numerous on the west side of the valley where a narrow bench can also be seen. Greater insolation and melting occurred along the east sides of valleys at the time of final deglaciation. The ice remained longer along the west valley wall where it was protected from the afternoon sun. Here the relatively thicker ice masses were finally buried to form Little York Lake, Crooked Lake and Song Lake.

Fan from Otisco Valley
In the Preble region, Interstate 81 crosses a fan deposited by a stream from Otisco Valley . Deposition of the fan crowded the West Branch Tioughnioga River against the east wall of the valley. These factors suggest that ice was active longer in Otisco Valley than in Onondaga Valley. Buried ice still existed in the valley so that melting and collapse were occurring while deposition continued from the northwest source.

STOP 1. Gravel Pit in Tully Moraine
Gatehouse Pond and Solvay Gravel Pit. Steep-walled gravel pit exposes materials composing major part of Tully moraine, showing it to be largely a product of outwash deposition from a stationary to narrowly oscillating ice margin. Exotic component in this through valley gravel is high with crystalline-carbonate-clastic ratios on the order of 10:40:50. The "bright" character of the gravels results from proximity to carbonate sources, attrition of diluting shale fraction from the lake plain, and effectiveness of glacial transport in a major through valley.

Cross Onondaga Creek
Cross Onondaga Creek which drops at Fellows Falls with hanging and barbed juncture into Onondaqa trough, in this area called Tully Valley. Ahead (NE), local relief exceeds 1250 ft. from upland to trough floor on proximal (northern) flank of massive Tully (Valley Heads) Moraine. The abrupt proximal border and gently graded distal slope of this moraine is characteristic of valley blocking moraine loops of this system on divides and northward opening valleys of central New York.
Seismic refraction profiles suggest that the unconsolidated valley fill in mid-trough opposite Fellows Falls may be 400 to 500 ft. thick, with the bedrock floor at 300 to 400 ft. msl. Northward, in the vicinity of Syracuse the bedrock floor of the trough lies below sea level. Southward the rock floor rises to 975 ft. above sea level in the col at Tully Lake.

Third Delta
Now riding over the surface of the third delta (el. 610') built into a lake whose outlet was the Rock Cut Channel.

Head of minor meltwater channel
Southwest of Joshua Corners note level swampy area at head of minor meltwater channel which deposited a delta complex into a predecessor of Otisco Lake, 3 miles to the southwest.

Cross Smith Hollow (Navarino Channel).
With threshold at 1005 ft. about one mile north of Rte. 20, the Navarino Channel developed as an outflow or overflow from Pumpkin Hollow (Lake Cedarvale) into Lake Marietta in Otisco trough

Four small marginal meltwater channels
Four small marginal meltwater channels notch the nose of Slate Hill to the west.

Pumpkin Hollow
Observe Pumpkin Hollow to the east (right). Cut sharply through Hamilton Shale section and floored on Onondaga Limestone. This is one of the largest of the cross channels which carried drainage eastward along the plateau margin. Pumpkin Hollow is about 0.25 miles wide and as much as 400 feet deep. Three miles east of Marcellus it widens abruptly to nearly a mile.

Head of Otisco Valley to Tully Valley channel
This is the head of the channel that carried the meltwaters from the Otisco Valley eastward into the Tully Valley. It becomes progressively wider eastward (downstream).

STOP 2. Sudden widening of valley
The sudden widening of the valley at this point, plus the absence of bedrock exposures in this area has led Krall (1966) to suspect that this is a buried pre-glacial or interglacial valley.

STOP 3. Gravel Pit Entrance.
This pit is being excavated in the second series of deltas (elev. approx. 700'). Shale pebbles occur frequently in the gravel and crossbedding is conspicuous.

Break in Slope on Makyes Road (S. Onondaga Hill Road)

STOP 4. Gravel Pit Entrance.
Gravel pit is in the second delta terrace. (Fairchild's Middle Terrace)

STOP 5. Base of tower.
Looking west can view the Tully Valley deltas just traversed. Also Joshua Coral Bed (Ludlowville Fm.) is exposed here.

Meltwater channel - Smoky Hollow with horseshoe shaped loop

Floor of Smoky Hollow meltwater channel (elev. 790').
East Syracuse reservoir on left.
Smoky Hollow, with bedrock floor just below 800 feet, is sharply incised in Hamilton Shales. This outlet may have controlled drainage of impounded waters in the Onondaga trough at the highest delta level in Cedarvale Channel (seen at STOP 3). Descend from drumlinized Hamilton upland onto channeled Onondaga bench.

STOP 6. Parking Area. Clarke Reservation Channel observed here.
Erosion by glacial meltwater, solution by underground water and joint control responsible for the features. Green Lake occupies the plunge basin cut into the Onondaga Limestone and underlying beds by waterfalls fed by glacial meltwater.

Entering Rock Cut Channel.
This steep-walled, flat-bottomed channel is floored by the Fiddlers Green Dolomite, with threshold at 550 feet at the west end and average eastward gradient of less than 10 feet per mile. The size of this channel and the configuration of the south wall suggest glacial advance south of Rock Cut Channel after the channel had attained essentially its present dimensions.

Note features in south wall (left side) of channel.