NYSGA 2021
New York State Geological Association
92nd Annual Meeting
Field Trip Guidebook
Hosted by
Buffalo State College
Edited by
Gary S. Solar and David W. Valentino
Published by the
www.nysgaonline.org

A1 Marine Crisis Events and Fossils Of the Late Devonian Appalachian Basin Deltaic Sequence Of Western NY
Kimberly C. Meehan
University at Buffalo, Department of Geology
Buffalo, New York 14260
James T. Boyle
INTRODUCTION
The Devonian Period experienced many changes within the environmental and biological realms and terminated with one of the largest mass extinctions of the Phanerozoic. The Appalachian Basin of western New York contains several alternating successions of gray and black shale, many of which mark marine crises culmination in the end-Devonian mass extinction. The causes for the formation (e.g., anoxia, flooding, biological production changes) of the black shale sequences has long been debated within the basin. This period was characterized by major changes in both the terrestrial and marine biospheres and terminated with one of the largest mass extinctions of the Phanerozoic Era (Kaiser et al., 2016). Middle Devonian terrestrial environments saw tremendous increases in biomass and complexity with the evolution of vascular and seed-producing plants, trees, and the formation of deeply weathered and thicker soils (Beerbower et al., 1992). The Devonian marine realm has long been suspected to have been heavily affected by bottom water anoxia, enhanced organic carbon burial rates, dramatic shifts in primary production, and an extended biotic crisis. The biotic crises and related marine extinction events have been attributed to many factors including bolide impacts (McLaren, 1982), tectonism and climate change (Ettensohn et al., 1988), oceanic overturn and/or euxinic conditions (Kelly et al., 2019; Haddad et al., 2016; Boyer et al., 2021), cold water oceans and dysaerobic conditions (Copper, 1986), marine ecosystem collapse (McGhee, 2013), eustatic change (Johnson and Sandberg, 1988), and more recently linking the marine phenomena to coeval developments in the terrestrial realm (Algeo et al., 1995; Algeo and Scheckler, 1998; Algeo et al., 2000).
Algeo et al. (1995) presented the hypothesis that the Middle-to-Late Devonian marine biotic crisis and mass extinction of benthic communities were precipitated by the evolutionary development of vascular land plants; terrestrial floras appeared in the Middle Ordovician, and these land plants were small, either non-rooted or shallowly rooted, and ecologically limited to moist lowland habitats (Cascales-Miñana, 2016). Evolutionary innovations of these floras in the Devonian allowed them to interact with substrates and strongly influence weathering processes, hydrologic cycling that would have changed the amount of run-off and peak discharge (Schumm, 1977; Algeo and Scheckler, 1998), and has been suspected by some researchers to have resulted in geochemical fluxes and the formation of carbon-rich black shale beds within the Appalachian Basin. While flooding events in the Appalachian Basin have received much attention recently (Kelly et al., 2019; Haddad et al., 2016; Lash, 2019; Bartlett et al., 2021 (in press)), by no means is there a consensus on the causes of formation of black shale sequences and other major shifts in lithology during this global event (see Kaiser et al., 2016). Over 100 years of research of the Devonian Appalachian Basin has led to the construction of one of the most detailed litho-stratigraphic frameworks of a Paleozoic foreland system that has allowed for detailed interpretations of sea level history and shifts in sedimentation rates (Dana, 1894; Wanless, 1947; Brett and Baird, 1986; House and Kirchgasser, 1993; Brett, 1995; Ver Straeten and Brett, 1995; Brett et al., 2011; Ver Straeten et al., 2011). As a result, a tremendous amount of geochemical proxy data from these gray and black shale sequences has shown that the perception that the Devonian black shales were deposited under anoxic conditions holds true, thus far, for only one black shale unit (Werne et al., 2002), the Oatka Creek Shale, and that intervals of terrestrial fresh water flux were not as prevalent as previously thought and that primary production plays a strong role in many, if not all black shale beds of the Appalachian Basin (Arthur and Sageman, 2005). More recent research on intercalcated deposits described in ancient and modern marine settings (e.g., Cretaceous Western Interior Seaway and Eastern Atlantic Ocean, Pleistocene North Atlantic, Neogene Mediterranean, modern Black Sea) has focused on eutrophic conditions and the effects of organic input, climate variations, primary production changes and seasonal riverine input and has made clear that the formation of carbonaceous and organiccarbon- deficient layers is anything but straightforward. The same is true of investigations attempting to derive the mechanisms behind the gray and black sequences in the Devonian Appalachian Basin (Werne et al., 2002; Sageman et al., 2003; Arthur and Sageman, 2005; Ver Straeten et al., 2011; Wilson and Schieber, 2015; Kelly et al., 2019; Smith et al., 2019; Haddad et al., 2016; Lash, 2019; Boyer et al., 2021; Bartlett et al., 2021 (in press)).

A1 Marine Crisis Events and Fossils Of the Late Devonian Appalachian Basin Deltaic Sequence Of Western NY

Meeting Point Burchfield Penny Art Center Parking lot Rockwell Road
Coordinates in Guidebook are not correct. Latitude should be 55', not 52'...

STOP A Eighteenmile Creek Access Site at the end of Basswood Drive, Lake View,
Regardless of creek level reaching this outcrop will require at least a brief dip into shallow water (usually less than a foot deep), so dress appropriately. This large amphitheater-style exposure stretches ~0.3 miles along the north side of the creek with the Tichenor limestone member of the Moscow Formation at the base providing a resistant platform to walk along. At this site members of the Hamilton (Tichenor, Windom), Genessee (North Evans, Genundewa, West River), and Soneya (Middlesex, Cashaqua) Groups can be observed. Large blocks of the more resistant North Evans, Genundewa, and Middlesex formations are common along the surface and can be readily examined. The underside of the North Evans is most accessible in situ at the upstream end of this outcrop where its unusual character is clearly visible.
There is a second exposure just upstream of where we will enter the creek but it is more difficult to view without crossing deeper water. However, for those interested this secondary location shows the full exposure of the Genundewa, West River, and Cashaqua units and even shows the lowest few meters of the Rhinestreet Formation at its top. The ubiquity of carbonate nodule bands in the Cashaqua is on full display at this exposure as well.

STOP B: Eighteenmile Creek Hobuck Flats at the end of Versailles Road, Derby
A short walk upstream there is an exceptional exposure of most of the Cashaqua and Rhinestreet Formations. There are numerous carbonate concretion layers accessible on foot from the Cashaqua and nodules originating from the Rhinestreet can often be found as talus along the base of the outcrop. Some of these nodules contain ammonite fossils and more rarely other macrofossils, such as placoderm fishes. There are also several soft pockets of organic matter within the upper Cashaqua that can often be spotted by their rusty weathering pattern. While the Rhinestreet is dominantly a black laminated shale there are also silty layers of grey shale within it that are visible at this locality.

STOP C Eighteenmile Creek at NY-20 (Southwestern Blvd), fisherman’s trail across from North Evans Cemetery.
Gravel path descent, may be washed out in places. Take caution on this foot path.
Uppermost Cashaqua Formation and beginning of the Rhinestreet Formation (Frasnian). This is the location where Lash found the 13C/TOC excursion for the punctata event and also at 20 and 40 cm below Cashaqua-Rhinestreet contact, at concretion layers, microtektites presumed to be from the Alamo event were found in macerated shale. Flooding event; hyperpycnal/monsoonal suspected. Some ammonoids and their casts have been found here, however, this location is mostly barren of macrofossils. Though there are abundant microfossils – not visible with naked eye.

Stop D: Preischel’s Farm. 2993 Belknap Road, Eden,
*** All wheel or 4x4 drive strongly suggested. By foot this is a 0.5 mile walk: Take dirt road next to tractor garage and milk silos on eastside of street. Last I was there the road was pretty washed out and steep, strongly recommend parking before the final drop off (you WILL see it), field with household appliances there for parking.
Rhinestreet and Angola Formation transitional zone, scraggy layer. Amazingly large concretions (average 1 m but can be as wide as >3m). This location contains geochemical signals and microfossils (charophytes, oogonia, antheridia), suggest seasonal to intermittent but regular flooding. Some macrofossils can be found but are rare. The Rhinestreet Formation is rich in methane/oil and contains a very distinct and strong odor.

STOP E US- 219 and Zimmerman Road overpass (broad shoulder for parking).
Park on wide shoulder near Zimmerman overpass.
*** be mindful of oncoming traffic. Speed limit is 65 mph, use due diligence should you cross the highway. It is strongly recommended that you use proper exit/entrance ramps to view the east side of the outcrops.
Angola, Pipe Creek (1m thick), and Hanover Formations on the west, middle, and east side shoulders. Oldest to youngest trending north to south along the highway. Pipe Creek marks the Lower Kellwasser Event.
Uppermost Hanover marks the Upper Kellwasser Event. Pipe Creek finger concretions 13C bear evidence of short-lived flow – disputed as to whether microbial, hydrates, or mud volcano … nonetheless, methane was discharged either due to common weather related mechanical dissociation.

A2 Eighteen Mile Creek - South Branch to Lakeshore - Middle to Upper Devonian Shales
Paul A. Agle
Department of Atmospheric and Geological Sciences
SUNY Oswego
INTRODUCTION
For logistical purposes, we will run this trip “backwards” in geologic time. We will start at the headwaters of Eighteen Mile Creek South Branch on the Appalachian Plateau. We will then begin to descend the plateau as the creek incises into the Upper Devonian shales. In these exposures, we will be able to observe important markers within the Late Devonian, including both the Lower and Upper Kellwasser extinction horizons. As we journey further back into geologic time, we will observe shales deposited during times of less environmental stress and, finally, we will end at the Lake Erie shoreline which provides excellent fossil collection opportunities. This morning trip serves as a companion trip to the afternoon “Penn Dixie Fossil Park & Nature Reserve: A Window into the Devonian Period of western New York” and the final portion of the road log will take us to the quarry where that trip will begin. Eighteen Mile Creek is named not for its length, but for its distance along the Lake Erie shoreline from the mouth of the Niagara River. The mouth of the Buffalo River, which would eventually become the terminus of the Erie Canal is about 2miles closer. These major navigable waterways were vital to the indigenous peoples, later colonial communities, and the industrial history of the area. On this trip, we will be visiting the locations of two of the earliest mills along the creek (Stops 2 & 3). In addition to powering mills, Eighteen Mile Creek and its valleys and floodplains provide fertile soils which continue to support a vibrant agricultural industry, particularly sweet corn, which is celebrated annually during Eden’s Corn Festival (1st weekend in August). The lower gorge and lakeshore sections have been a popular site for previous NYSGA field trips. These trips mostly sought to analyze a specific stratigraphic section (e.g., Zambito and Mitchell, 2006 – Wanakah Member; Lash and Blood, 2006 – Rhinestreet Member) or to address specific geological / paleontological problems (e.g., Over et al., 1999 – Disconformities; Baird et al., 2006 – Geologic and Biotic Event horizons). This trip is meant to serve as a comprehensive overview of the creek itself, primarily the South Branch, but it also provides some optional stops along the main (northern) branch. The Eighteen Mile Creek gorge can be intimidating and may seem unapproachable at first. This trip will highlight areas that provide relatively easy accessibility for other researchers and students who may wish to study these intervals in more detail. For this purpose, the trip also provides a broad sampling of the stratigraphy (ranging from Middle Devonian (Givetian) Wanakah Member up through the Late Devonian (Famennian) Dunkirk Member. From a paleontological perspective, we will see fossil communities thriving along the lakeshore section (and later at Penn Dixie Fossil Park in a separate afternoon trip) and higher in the section, we will explore outcrops surrounding the Kellwasser Events, where these fauna were stressed or eliminated.

A2: Eighteen Mile Creek: South Branch to Lakeshore; Middle to Upper Devonian Shales

Meeting Point: Francis Danter Memorial Park in New Oregon

Kern 1 well (National Fuel Gas).
Kern 1 well (National Fuel Gas), penetrates to Queenston producing out of
Medina SS. Outcrop of Canadaway Group in creek behind well with small
waterfall

Shear road cut exposure of Canadaway Group.
Shear road cut exposure of Canadaway Group. Shoulder is often VERY soft

Bridge over creek with some decent outcrop

Cement driveway bridge across creek
Cement driveway bridge across creek with easy access to pavement
outcrops of Canadaway Group

Would be Stop1, but bridge is out. We will detour around and visit as Stop2

STOP1: New Oregon Rd Bridge, Upper Kellwasser Bed: Frasnian-Famennian boundary
Park on right shoulder in front of garden, just before the New Oregon
Rd bridge over Eighteen Mile Creek South Branch.
At this location, we will examine the Upper Kellwasser horizon in outcrop. The interval is visible in the cutbank just to the NW of the New Oregon Rd bridge as the creek makes a turn towards the NE and heads towards Sisson Highway. This location is Stop7 of Baird and others (2006) and they provide an indepth review of the interval, including a measured section, which is reproduced herein (Figure6B). The Upper Kellwasser Bed lies 2.4m below the abrupt contact between the Hanover Member and the overlying black shales of the Dunkirk Member (which we will also see at Stop2). This bed within the upper Hanover marks the Frasnian-Famennian boundary and a major faunal disturbance.

There is a small tributary on the right with a series of small waterfalls

STOP2: Clarksburg Country Club, Dunkirk Shale
Clarksburg Country Club. Turn right into driveway (just before bridge)
and park along the wood fence near the green bathroom buildings
Unfortunately, the Clarksburg Rd Bridge is out which will force us to detour around. The locals informed me that a propane tanker truck lost its brakes coming down the hill and the driver was forced to bail out before the truck hit the bridge. Fortunately, there were no major injuries aside from the bridge as the engine block tore through the plate steel. The falls here mark the historic location of Simeon Clark’s Mill (circa 1820) for whom the town is named. The face of the falls is composed entirely of highly fissile, organic-rich, black shales of the Dunkirk Member.

Bridge over creek with nice pavement outcrop and small waterfall in creek
bed

STOP3: Kromer’s Falls, Lower Kellwasser Bed (Pipe Creek Member)
Drive past the two private residences and park at the
end of the driveway in front of the out-buildings near No Trespassing signs
The falls here also powered an historic mill and the area around it was referred to as Toad Hollow. Kromer’s sawmill operated here into the 1980s when the roof collapsed during a winter storm. The foundations of the mill are still visible. This location is Stop6 of Baird and others (2006) and they provide an in-depth review and stratigraphic column which is reproduced herein (Figure6A). Most of the face of the falls is composed of gray silty, bioturbated shales of the Angola Member, but the falls is capped by the well-jointed black shale of the Pipe Creek Member. Bioturbation diminishes upward within the Pipe Creek and it is laminated at the top of the falls, indicative of the major faunal disturbance associated with the Lower Kellwasser Event.

Bridge over small tributary that exposes some section in a series of small
waterfalls up Schintzius Hill

Eden Valley Mills
Where Mill Rd intersects with Bley Rd, there is an access road on the right that will bring you to the site of Eden Valley Mills (still standing), one of the historic mill locations along the creek. The creek bed is mostly covered through the relatively low-relief Eden Valley.

STOP4: The Forks @ Eighteen Mile Creek Park, Rhinestreet Member
The road winds along the rim of the gorge. After a sign that says
"Slides" and a 20mph left bend sign, park facing the "wrong" way on the left
shoulder (wider and paved) just as the road starts to bend towards the North.
Across the road, there is a very small gap in the retaining barrier that leads to a
footpath down to the main branch of Eighteen Mile Creek.
The footpath provides a relatively easy descent into the gorge with outcrop in the path itself and along the right-hand side. This is the best opportunity to examine the Rhinestreet Member up close as the gorge walls here are quite steep and inaccessible. Near the bottom of the path, an ephemeral waterfall on a small tributary exposes some large septarian carbonate concretions within the black shales. Lash and Blood (2006) provide an in-depth analysis of this interval, the concretions, and a detailed stratigraphic section that is provided herein (Figure 5). Once you are at creek level, if you walk upstream you will come to The Forks (the confluence between the main branch and the South Branch of Eighteen Mile Creek.) In this area, there are several large concretions that have weathered out of the banks and now rest among the talus and alluvium. This land is currently being developed into Eighteen Mile Creek Park with footpaths providing easy access both upstream and downstream from this location.
**Alternate stops (upstream on main branch of Eighteen Mile Creek)** If you’d prefer to work your way up the main branch of Eighteen Mile Creek rather than proceed downsection to the lake shore, there are a few interesting stops along the way.
If you continue eastward on North Creek Rd you will continue to parallel the gorge, but access from above is very difficult. Make the first possible left (Lakeview Rd) and then turn right onto Lakeview Rd. The Town of Hamburg Recreation Center is near this intersection and there is a moth-balled Cold War Era Nike Missile Base (BU-52) on its grounds. According to the Hamburg Historical Society website, this missile base (and others) protected the Buffalo population center and the steel and iron industries of the area.
The intersection of Lakeview Rd and Old Lakeview Rd is directly across from the Recreation Center. If you take Old Lakeview Rd to the intersection with Smith Rd there is a sharp meander in the creek. Turn right onto the onto South Creek Rd bridge (42.7117°N, -78.8695°W) and to your right you can see a cable stretched across the creek with Posted signs strung across it. Beneath the cable on the SW wall of the gorge, there is a small tunnel (barely high enough to stand) that goes entirely through the meander (do not enter without permission!) at creek level. This tunnel is another callback to the industrial history of the area as it served as the upstream head race that powered a grist mill and the tail race comes out downstream of the falls on the other side. According to the nearby historical marker, this mill was erected in 1806 by John Cummings and was the first grist mill south of Buffalo. Upstream from this location, towards the town of Hamburg, the gorge becomes shallower and much less steep. The creek is readily accessed from Woodview Park (Woodview Ave) and from Centennial Gardens Park (corner of Main St and Buffalo St). The creek continues behind Eighteen Mile Creek Golf Course and even across Rt219, but outcrop is limited.

This road parallels the gorge with a few areas where access is possible (but mostly difficult)

Go to right to descend to creek level to Hobuck
Flats parking area
If you turn right on Versailles Rd, you will descend to creek level to Hobuck
Flats parking area. There is a footbridge across the creek, easy access to creek
level, and a short hike (stay on lower path) to a waterfall on a small tributary.

Creek access
We will go under a set of railroad tracks. The creek can be accessed from
near the railroad bridge, but it is not recommended

Creek Access
There is a way down to creek level at the Rt5 bridge, but this is also not recommended

This location should absolutely not be accessed without prior permission from the residents

STOP5: Lake Erie Shoreline, Wanakah Member
Group). This interval is examined in detail by Over and others (1999) near the mouth of Eighteen Mile Creek, which lies just north of this location. Their map of the stratigraphic contacts along the creek and accompanying stratigraphic section are reproduced herein (Figure4). The lowest stratigraphic member exposed at this location (and often covered by shifting talus) is a light gray, shaly limestone of the Wanakah Member which contains abundant (and often complete) Eldredgeops trilobite fossils. This is likely the upper “Trilobite Bed” as described by Grabau (1898), which can also be observed at the mouth of the creek. Above that are more typical shales of the Wanakah and a thin, but laterally continuous band of chocolate brown shaly limestone that is largely unfossiliferous. Above that is more typical shale and then the upper contact with the Moscow Formation (Tichenor Member). The Tichenor forms a prominent ledge in the cliff face and numerous large blocks of limestone with its characteristic pyrite and rust-staining are strewn across the beach. This rock is used as a building stone in many local buildings, including Frank Lloyd Wright’s Graycliff which sits just above the cliff. The rusted steel remnant of the stair tower, which used to provide “easy” access down to lake level, is still standing along the shoreline. It is difficult to examine the stratigraphically higher units (Windom Member) of the cliff at this location, but I encourage you to use the directions below and join us for Philip Stokes and Holly Schreiber’s guided tour of the Penn Dixie Fossil Park & Nature Reserve in the afternoon where they will examine these units in detail.

Penn Dixie Fossil Park and Nature Reserve

B1 Salamanca Conglomerate A Record Of Storms, Floods, And Tides in Deltaic-Coastal Deposits Of the Upper Devonian Cattaraugus Formation
A version of the following article was prepared after a brief field season for the 2017 New York State Geological Association fall meeting ( http://www.nysga-online.net/ ). Ongoing fieldwork has continued over the last four years and the use of DEMs/GIS has located and correlated Salamanca (and other conglomerates) outcrops over an area of 2000 km2. The overall interpretation (prograding delta - flood dominated with wave & tide-influence) is the same with some refinements for the type section (“Little Rock City”) and near-field areas (Rock City State Forest).

B1 Salamanca Conglomerate A Record Of Storms, Floods, And Tides in Deltaic-Coastal Deposits Of the Upper Devonian Cattaraugus Formation

Meeting Point: Rock City State Forest
Little Rock City Rd. at the DEC sign/State Forest
boundary

STOP 1. The “Sentinels”
STOP 1. The “Sentinels” - obvious from the first crest of Little Rock City Rd.; well visited but respect private property. Wellweathered, isolated blocks; interpreted as tidal flats and shoals.

STOP 2. The "North Face"
The highest outcrops (+10 m; which includes 3-4 m of marine strata) – shoreface/foreshore/channels; see Figs. 18, 19 & 20)..

STOP 3. NW corner of outcrop belt
NW corner of outcrop belt and points S on the Rim Trail, interpreted as a deltaic channelbelt w/shoreface, mouth bar, channels/point bars.

STOP 4. Just east of the first rise (escarpment) on Little Rock City
Rd. within RCSF.
Some point bars (lateral accretion deposits) and channel fills and large x-beds and capped by beds of very large (> 7m) pebbly hummocky cross-strata (HCS). Interpreted as part of the deltaic sequence with some tidal deposits and storm intrusions

STOP 5. A series of linear outcrops extend south for 100s of meters
A few 100 meters south of #4, east side of the road, just inside treeline, a series of linear outcrops extend south for 100s of meters. Roughly 2 m exposed, mostly HCS, some wave xlamination, occ. channels/x-beds; very large and pebbly HCS subjacent to caprock; above cap, a thin-bedded fossiliferous sandstone. Interpreted as intense storms then quiescent shallow marine conditions; a distinct change in wave climate perhaps best explained by a relatively rapid change in relative sea level/apparent transgression.

STOP 6. Perhaps the most interesting (confusing?) outcrop area.
STOP 6. East of first campsite/shelter, follow white (NCT) blazes; perhaps the most interesting (confusing?) outcrop area. A large channel complex overlying fine-grained wave-rippled sandstone (delta interpretation) with adjoining cross-strata of all scales.

STOP 7. Large-scale (3-5 m) cross-strata, then HCS and channel deposits
STOP 7. The NCT joins outcrop area #6 with #7 and following it south (white blazes) through Little Rock City provides a representative sampling of large-scale (3-5 m) cross-strata (tidal dune field) followed by HCS (dune beheading by waves), then a smattering of channel deposits (tidal or fluvial), then the caprock (a final leveling by waves).

B2 Escarpment to Escarpment to Escarpment - Three Vistas Reflecting the Subsurface
Structure of Western NY
Paul R. Nevergold
984 Parkside Avenue
Buffalo, NY 14216
Joseph A. Butch
202 North Linden St.
Amherst, NY 14221
INTRODUCTION
This trip, designed for Earth Science teachers, and the general public, presents a non-technical overview of the structural geology of western New York State. It includes stops at each of the three major escarpments, a brief hike, sampling of the escarpment capping lithologies, “snapshots” of geologic features, guided discussions, and includes historical geology interpretations.

B2 Escarpment to Escarpment to Escarpment - Three Vistas Reflecting the Subsurface
Structure of Western NY

Meeting Point: East side of the Science Bldg.

STOP 1: Chestnut Ridge Park parking lot
Hike to Falls of the Eternal Flame (If, perchance, the eternal flame is out, we will light it and not tell anyone.) You will lose and then gain about 80 feet of altitude on the hike. The trail is rugged and should not be taken unless you are sure you can get back up. Hiking boots best, sturdy sneakers second, sandals or flip-flops forbidden. You will be following a stream bed and may get your feet wet. You should have extra socks. It will take 25 minutes down, and 30 minutes back.
Interesting sedimentary features for photos and samples can be taken. We will be hiking through outcrops of the Upper Devonian Arkwright group’s Canadaway formation. The rock formation making up the sides of the small canyon we will be hiking up is the Canadaway formation, the Gawanda member to be specific. The lithology is described as gray and black shale, thin and thick bedded siltstone and occasional limestone concretions and layers. The black shale is highly petroliferous, the likely source of the gas for the “eternal flame” and on calm days can be smelled near the falls. We will point out and discuss sedimentary, topographic, and structural features along the hike.

STOP 2: Chestnut Ridge Park view from the edge of the Portage
Escarpment
The view from the edge of the Portage Escarpment will open our discussion on the three topographic vistas of western New York. Looking north you can see UB (South Campus) and the Vet’s Hospital on the horizon which is located on the Onondaga Escarpment. If you look a little west (left) of Buffalo, you can see Niagara Falls on a clear day about 30 miles.

STOP 3: New Enterprise Stone and Lime Company
We will meet at 11:am at the quarry gates. All visitors will be required to sign a permission slip before entering the quarry. During the tour, we will stay together as a group and follow all quarry rules.
The quarried area is about one square mile. The rock layer quarried is the Nedrow member of the Onondaga Limestone which is middle Devonian in age. Quarried Onondaga was used as “dimensional stone in most of the bridge abutments of the old railroad bridges in WNY. It was considered strong and resistant enough to be used in the abutments of the Brooklyn Bridge. It outcrops from Lake Huron and the NW shore of Lake Eri to The Hudson valley. The Nedrow member contains a lot of flint that was used by indigenous peoples for weapons and tools. In Erie County, there are three active quarries on the Onondaga and quite a few abandoned quarries.

STOP 4: outcrop south of Clarence Town Park
We will take a close look at an outcrop south of Clarence Town Park. We will discuss the nature of the outcrop, collect flint, discuss the weathering process, and interpret how the features observed could have been formed.
Discussion questions:
How does the bedrock outcropping at this stop differ in appearance from the bedrock visible at the New Enterprise Stone and Lime Co. quarry? How would you explain this? The calcium carbonate in the limestone is stable in an alkaline environment and rapidly decomposes in an acidic environment. The silica in the chert nodules contained in the limestone is stable in an acidic environment. How might a cherty limestone have been formed?

STOP 5: Airport Road in Akron, NY
A stop along Airport Road in Akron NY affords a view from the Onondaga escarpment and an opportunity to discuss physical geogrphy. The first draft of this field guide instructs us to “take pictures, sing & dance.” The geologic processes forming this escarpment have produced an east-west string of waterfalls across New York State including Williamsville Falls, Akron Falls, Indian Falls, Buttermilk Falls and others.

STOP 6: Outwater Park, 125 Outwater Drive, Lockport, NY
Outwater Park in Lockport New York provides an excellent safe view of Lake Ontario Lowlands. Discuss glacial Lake Iroquois and the carving of the Lake Ontario basin. On a clear day you can see Toronto about 50 miles away.
Since we will be not able to park and walk around at Stop 7, we can take time to discuss this outcrop while we are assembled here.