The Outcrop at Crystal Rock, Margaretta Twp., Erie Co., Ohio, U.S.A. Is It An Example of Glaciotectonic Movement?

Michael James Norrocky

162 Duchess St., Vickery, Ohio, U.S.A.

mjnwlk@yahoo.com

Introduction

Glaciotectonics describes the movement of loose materials or solid land masses by either being shoved or carried by glaciers. It was first considered as a field of study in 1927 by George Slater who coined the term glacial tectonics which has been shortened to glaciotectonics. During the 1970's the study was revived by Asger Berthelsen (University Denmark). He developed the method of kineto-stratigraphy in which the main emphasis is placed on the study of the directional elements that reflect the movement patterns of former ice sheets. The field of glaciotectonics, although relatively new, has gained widespread recognition in the past 25 years (Aber & Ber 2007, Pg. 1). The renaissance in the study of glaciotectonism in North American was begun by A. R. Byers who demonstrated the development of the Dirt Hills and Cactus Hills in Saskatchewan, Canada through glaciotectonic activity. These are among the largest and best developed glaciotectonic hills in the world. The study area was expanded by Walter Kupsch to include ice-shoved hills in Alberta, Canada. An extensive bibliography by Dr. James Aber is available at: Bibliography of Glaciotectonic References: www.geospectra.net/glatec_biblio.htm

The Crystal Rock outcrop is located in the northwest part of Margaretta Twp., Erie Co., Ohio, U.S.A., 0.25 miles south of Sandusky Bay (41o 26' 35" N , 82o 50' 42"). It is ~118 acres and stands at ~625’ maximum elevation (Fig. 1). It is on the south end of a group of dolomite outcrops which include Catawba Island peninsula and South Bass Island (Fig. 2) The bedrock is Silurian dolomite of the Bass Island Group (Fig. 3), part of the Put-In-Bay dolomite series (For a detailed treatise see Sparling 1970. Several sinks of various sizes are scattered on the outcrop. A large depression on the west side is on property owned by Keith and Guy Miller (Fig. 4). Because of its size, it has been identified in the past as a quarry (Erie Soil & Water Survey 1971). It is currently believed to be a sink.

The Crystal Rock outcrop appears relatively smooth on the surface (Fig. 5). In 2008 Stephen Sabo made eleven transects at the Crystal Rock outcrop as part of his Master Thesis at Bowling Green State University using Earth Resistivy Graphic Imaging (ERGI). Two examples are seen in Figure 5. Steve’s results prove that the subsurface is very irregular, with voids over 30 feet, many clay

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filled (Fig. 5). During the last glacial epoch several lakes existed to an elevation of ~ 800” above sea level ~125’ above the Crystal Rock outcrop. While the area was covered by these lakes, clay was deposited and filled up many of the voids. The question is, what created the void in the bedrock. Was it subsidence into a void created by the dissolving of gypsum, erosion, removal by glacial activity, or some of each. Regardless of the cause, the irregularities would have provided places for a glacier to temporarily attach and move the outcrop.

Three caves are found on the outcrop, two of which are similar to caves found on South Bass Island (Verber & Stansbery 1953). Brewery Cave and Crystal Rock Cave had been developed and were open to the public in the past. These caves are at the edge of sinks as seen at Crystal Rock Cave (Fig. 6).

Fig. 1 Section of 1969 USGS 7.5 min. Castalia, Ohio Quadrangle showing Crystal Rock outcrop

(center) , Margaretta Twp., Erie County, Ohio.

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Fig. 2 Drawing showing relative positions of Crystal Rock, Catawba Peninsula, and

South Bass Island. These outcrops are all Put-In-Bay dolomite.

One difference between the Crystal Rock and South Bass Island caves is the changing of the water levels in the caves. Verber and Stansbery reported that the water level in some of the caves on South Bass Island fluctuated with the level of Lake Erie but with a two hour lag time. The author placed a Stevens Type F recorder in Perrys Cave, South Bass Island, for 24 hrs. The recorded level followed the lake level as reported at the Marblehead Coast Guard station with about a 2 hour lag as reported by Verber et al 1953, corroborating their conclusion. At Crystal Rock the water level is not affected by lake level, it changes in response to surface water and remains at a constant level between rain or snow melt events. (Norrocky 2011).

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The Salinas dolomite occurs ~ 1 mile to the west of the outcrop and the contact with the Columbus limestone is ~2.5 miles to the east (Fig. 3). Bedrock on the north side ranges from a depth of 28' to ~37' near Sandusky Bay. Just to the west along Sandusky Bay, at Kugel's allotment, rock is ~45 feet deep, and to the east, on the Harkness property, bedrock depth is 20’ (Figs. 7 & 8). On the south the bedrock dips to 520', 65' below the surface, and then rises to ~620' as it approaches the Columbus cuesta, south and west of Castalia. The soils in the area of the outcrop are primarily marl due to the many springs found in the area (Sears 1967). (Fig. 8)

Fig. 3 Bedrock geology of the site region, modified from the ODNR, Geology Div.

overlaid on the 1969 USGS 7.5 min. Castalia, Ohio Quadrangle.

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Fig. 4 View to Northeast of sink on Miller property on west side of Crystal Rock

outcrop. The sink is ~180' to distant trees and then a ~50' section going to the right. The

site was called a quarry by Erie County Soils Engineers because they couldn't attribute it

to anything else (Personal Communication.). It is currently believed to be a sink. The dolomites and Columbus limestone are karst and John Tintera (Tintera 1980) discovered over 200 sinks in the Columbus limestone south of Castalia. Many springs are located in the karst north of the Columbus cuesta, north of Castalia (Fig. 7). Glaciotectonic features are frequently found in conjunction with subsurface aquifers (Aber et al 2004, pg. 167).

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Example 1.

Example 2.

Fig. 5 Two examples of contoured resistivity cross sections of eleven transects

performed at Crystal Rock outcrop by Steve Sabo during a 2008 study involving the

effectiveness of this method on different soils and bedrock. As can be seen the Crystal

Rock bedrock surface is very irregular and would have offered a surface that an glacier

could have attached to and allow it to be moved. Top of each example is the contoured

resistivity cross section obtained in the field and bottom drawing is the interpretation of

the cross section.

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Fig. 6 Opening to Crystal Rock Cave. Entrance excavated on edge of sink. Notice hand

rail along steps leading to cave.

In the dolomite, lens of gypsum can be found (Sparling 1970). About 1 mile to the east-southeast of Crystal Rock, where SR 6 and SR 269 intersect, on property owned by the Lippert family, a gypsum mine operated in the 1920’s. It was abandoned when they couldn't pump the water fast enough. Mr. Lippert told me that his father worked in the mine and they had two large pumps to keep the water level in the mine down enough for the workers. When they abandoned the mine, the pumps were not retrieved. The U.S. Gypsum Company mined gypsum for years on the north side of Sandusky Bay, ~3 miles north of the Crystal Rock outcrop. Five and three quarter miles to the southwest of the outcrop, in Sandusky County, near Vickery, the East Ohio Gas Company, drilled a test well (Haff #1) on the Haff property. The well log suggests much solutioning of gypsum south of Sandusky Bay (Sparling 1970, Pg.14).

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Fig. 7 Ohio Dept. of Geology map showing wells and bedrock depth determined from

well logs overlaid on Castalia 7.5 minute topographic quadrangle. Topo contour = 5 ft.

Bedrock contour interval is 20 feet.

The water in two springs south of Sandusky Bay, Miller Blue Hole south of Whites Landing and Troike Spring, ~1 mile southwest of Crystal Rock outcrop (Fig. 8) are cloudy suggesting solutioning of gypsum.

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Fig. 8 Drawing of Crystal Rock outcrop and area springs. Blue = terrestrial, red =

subaqueous. Many sinks occur in the area, especially to the south and southwest of

Castalia extending to Bellevue and Green Springs. About 200 sinks were found in the

area north of Bellevue, Ohio. (Tintera 1980).

Kihn (1988 Fig. 4 pg 19) diagrammed the possible course of the Erigan River running from the Columbus cuesta, southwest of Castalia, north then northwest to enter the present Sandusky Bay just east of White’s Landing (Fig. 9). These ancient channels influence glaciotectonic activities (Aber 2004 pg. 167). In the vicinity of Crystal Rock there are three wells which do not appear on the bedrock map (Fig. 7) but can be found on the Ohio Dept. of Nat. Res., Div. of Water website. These wells are recorded to Roy Ballah, Perry Mischler, and William McDougall (Fig. 10).

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Fig. 9 Drawing of Crystal Rock outcrop area showing accepted course of Erigan River

(modified from Kihn 1988, Fig. 4, Pg.19) and 3 wells (red dots) not on bedrock map, Fig.

7. The wells may define a tributary of the Erigan River.

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Fig. 10 Drawing of Crystal Rock outcrop area with Ballah, Mischler, and McDougall

wells. Depths and in some cases material in the wells are indicated. These data suggest a

deep channel on the west side of Northwest Road running northwest to Sandusky Bay

east of the course for the Erigan River indicated by Kihn 1988 (Fig. 9). The wells might

indicate a tributary of the Erigan River.

The log for Ballah records 79’ in basically clay, no bedrock. The well for McDougall has clay, then shale at 70’ and limestone at 86 feet. The unusual part of that record is sand from 10’ to 70’. Sand is usually associated with beaches which would have occurred as one or more of the post-glacial lakes were receding. The Mischler well is the deepest, with clay to 35', predominately gravel & clay to 110' with a thin layer of broken limestone, then shale at 114' to 115’. The logs of these wells define what appears to be a channel, possibly a tributary to the Erigan River. These channels can be associated with glaciotectonic activity (Aber et al 2004, pg. 167).

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In response to an inquiry, Rick Pavey of the Geology Div. of the ODNR wrote, “The valley shown in Kihn's Fig. 4 is actually a tributary to the classic Erigan, which follows the axis of Lake Erie. Our current interpretation of these valleys is that they are

probably not really pre-glacial stream valleys. The many ice advances eroded so much

bedrock that any pre-glacial topography has probably been removed. These shallow,

broad valleys are viewed as glacial scour channels, although they may have inherited

their location from former streams.” The apparent channel just west of Crystal Rock may not be an ancient channel but could have influenced the glaciotectonic movement of the outcrop (Aber et al 2004, pg. 167). Crystal Rock is on the south end of the string of dolomite outcrops on the east side of the Findlay Arch branch of the Cincinnati Anticline (Figs. 2 &11). The strata dips to the southeast at about 20’ to 40’ per mile (Herdendorf 1977, Kihn 1988).

Fig. 11 Drawing of Cincinnati Arch with branches Kankakee (Wabash Arch Hubbard, 1924) and

Findlay Arch. Modified from Kihn 1988 after Riggs 1960.

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Fig. 12 Drawing showing various strata on east side of Findlay arch in vicinity of South

Bass and Kelleys Islands in Lake Erie. The rock dips to the southeast producing a cuesta

on the west side of the islands. Drawing not to scale.

Carmen (1946 pg. 73) described the Bass Islands, Catawba Island peninsula and by extension, Crystal Rock as, “Both island belts are north-south cuesta ridges with steeper slopes on the west and gentler slopes to the east..”. Herdendorf (1977) describes the Bass Islands, Catawba Island Peninsula as having, “…high elevations and cliffs at their western shorelines; elevations generally decrease eastward …”. This is in direct contradiction to the situation at Crystal Rock where the greatest relief occurs on the east side (Fig. 14) and the west side is a gentle slope (Fig. 15).

Fig. 13 Cuesta on west side of South Bass Island. Photo courtesy of Dr. Ed Herdendorf.

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Fig. 14 Slope on east side of outcrop at Crystal Rock. Distance to level ground is 140'

and slope angle is ~10o resulting in a drop of ~25 feet to the level ground below.

On the east side the distance from the top of the slope to the level ground below is ~140' and the down slope angle is ~10.5o. Using the law of sins, the drop calculates to ~25'.

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Fig. 15 West side of outcrop at Crystal Rock. Distance to level ground ~500' (not visible

in this view. Slope ~2o.

The west side distance to flat ground is ~500' and the down slope angle is ~2o. Using the law of sins, the fall on the west side is 17'. Obviously the east side has the greater slope, unlike the Catawba Peninsula and South Bass outcrops. Crystal Rock does not conform to the pattern on Catawba or South Bass. Figure 16 is a ridge at Crystal Rock. It is ~ 100' wide on the northeast end. A cave, not of the sink type, opens facing north on the west end of the outcrop (Fig. 17). Large amounts of gypsum that dissolved from deposits in the area have formed sinks.

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Fig. 16 A 100’ wide ridge on the northeast corner of the outcrop at Crystal Rock runs

southwest on the right to northeast on left. Herein referred to as the NE ridge.

Fig. 17 Cave at base of north side of NE ridge. This is example of cave not of the sink

type. Similar to some caves found on South Bass Island. This cave is on private property

and was never open to the public.

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Fig. 18 View from top of NE ridge at Crystal Rock. The depressions in the distance are

thought to be sinks due to the dissolving of gypsum.

Fig. 19 Southwest view of swale on south side of NE ridge at Crystal Rock outcrop.

Swale may be a sink caused by the dissolving of gypsum.

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Examples of the bedrock found along the ridge are presented in Figs. 20 to 22. No attempt to assign the various strata to a type due to the difficulty of identifying these (Forsyth and Kahle 1983).

Fig. 20 Massive bedrock on the south side and near east end of the NE ridge at Crystal

Rock..

Fig. 21 Brecciated bedrock on south side and near east end of swale. Pole in 1 ft.

increments.

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Fig. 22 Bedrock at the east end of the NE ridge at Crystal Rock. The pole is marked in 1

ft. increments. The layers of clast near the bottom may represent a contact between two

of the Bass Island dolomites.

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Scattered around the outcrop are granite erratics obviously dropped by one of the ice advances during the Illinoisan or Pleistocene periods. The following figures are examples of rock found on the surface unattached unless indicated otherwise.

Fig. 23 Eroded bedrock on top of NE ridge. Pole in 1 ft. increments.

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Fig. 24 Eroded bedrock near north end, in middle of Crystal Rock outcrop. Note leaves

for size comparison.

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Fig. 25 Seven inch long brecciated rock found at east end of NE ridge. Note calcite

crystals.

Fig. 26 Extremely brecciated rock found near north end in the middle of the Crystal Rock

outcrop.

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The lack of a cuesta on the west side makes Crystal Rock different from Catawba and South Bass Island (Fig. 13). If Crystal Rock was not simply rotated in place by glacial activity and has been transported, where did it come from? In searching ODNR Div. of Water well logs, I found records for wells along SR 163 (SR 163) aka East Harbor Road , aka Harbor Road E, Danbury Twp., Ottawa County. SR 163 is along the north side of Marblehead Peninsula near East Harbor which is a body of water just off Lake Erie (Figs. 27 & 28). I found several deep wells and gathered several well logs in an attempt to determine the size of the hole. Starting at Box 6154 SR 163, ~ 0.1 mile west of the Church Road-SR 163 intersection, Well Log (WL) # 667401, in the name of Gordon Wahles showed 68’ to “limestone”. [All references to limestone here should be dolomite]. At the intersection with Church Road, on the north side of the road at Box 6657 SR 163, the well log for Bass Haven Marina (WL #631403) has 108’ to limestone. Three tenths mile eastward on the north side , the well log (WL 394174) for Jack Tibbels, Box 6965 SR 163, has limestone from 94’ to 96’ and then coarse gravel to 100’. No further indication of solid rock was recorded. About 0.9 mi. east in Channel Groove, the log has boulders from 72’ to 86’ and solid rock at 86 feet. This location is very close to the dolomite / limestone contact (Figs. 28 & 29). Going south on Church Road from SR 163, well log #774873, issued to David Kihlken, 150 Church Road (Fig. 27), was filed on Sep. 02, 1993 by Tibboles Well Drilling, Inc., Bellevue, Ohio. The well log for the well reads as follows: YELLOW CLAY 0'-19', BLUE CLAY 19'-38', BLUE GRAVEL & CLAY 38'-52', BOULDERS 52'-54', GRAVEL & BOULDERS 54'-95', BLACK GRAVEL & SAND 95'-100', BLUE GRAVEL & CLAY 100'-105', GRAVEL 105'-118'. The well ends in gravel. South about 1.6 miles, near Bay Shore Road on the south side of the peninsula the rock is 34’ deep (Fig. 28). The dolomite/limestone contact occurs about half the length of Church Road .(Figs. 28 & 29). The wells along Church Road are near the Put-In-Bay dolomite and Columbus limestone contact (Fig. 28 & 29) which could facilitate the detachment of a landmass by a glacier (Aber et al 2004, pg. 167). If the Crystal Rock outcrop did come from the SR 163 location which is not on the present lake shore, it may not have been subject to the erosion seen on the west side of the Catawba Peninsula and South Bass Island (Fig. 13). This would account for the gentler slope found on the east side of Crystal Rock.

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Fig. 27 View north along Church Rd., Danbury Twp., Ottawa Co., Ohio near intersection

with SR 163. Kihlken house (Well log #774873) is on left. House in distance faces SR

163. East Harbor, just off Lake Erie, can be seen in the distance, frozen and snow

covered. A mobile home can be seen in Bass Haven South mobile home park on east side

of road.

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Fig. 28 Google maps view of portion of Marblehead Peninsula, Danbury Twp., Ottawa

Co., Ohio. showing depth to rock from well logs. Dashed line is approximate location of

Bass Island dolomite / Columbus limestone contact. East Harbor, a body of water just off

Lake Erie, is at top.

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It is obvious that the hole near and north of SR 163 is extensive. Bedrock was not reached in 2 of the wells even though they were over 100 feet. It is ~1.3 miles from the Wahles well at 6294 SR 163 (WL 667401) on the west to the 86’ well (WL 183786) at Channel Grove on the east. From the 108’ well at Bass Haven to the 69’ Boyce well it is ~0.58 miles. The area enclosed by this rectangle is 0.75 square miles. On the east the rock at Englebeck Road is in the Columbus Limestone and does not approach the depth found to the west (Fig. 28). For this reason the enclosed area is calculated on a diagonal from Channel Grove to the Boyce well along Church Road. This yields about half the area, or ~0.38 square miles. Since the deepest wells are near East Harbor it is reasonable to assume there are more deep holes under this body of water.

Fig. 29 Ohio Dept. of Geology map showing the boundary of the contact for the Bass Is.

dolomite and Columbus limestone in Danbury Twp., Ottawa Co., Ohio. The David

Kihlken well is near the junction of Church Road and SR 163. The wells locations are

near the dolomite – limestone contact on the south and East Harbor on the north.

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The information from the logs for 4 wells near SR 163 are listed in Table 1. The presence of the boulders encountered during drilling suggest that the voids were created during the glacial period, the hole(s) being gouged out and then boulders being carried by subsequent ice and being dropped or pushed into the voids.

Table 1 Select well logs from along SR 163, Danbury Twp., Ottawa Co., Ohio First 3

wells north of SR 163, 1 from 150 Church Road. Well Log

# Name Address Material Depth

ft.

631403 Bass

Haven SR 163 at Church

Rd. Yellow clay 0-15

Blue Clay 15-60

Clay/Gravel/Boulders 60-108

Limestone 108-112

394174 J. Tibbels 6965 SR 163 Yellow Clay 0-15

Blue Clay 15-69

Blue Gravel & Clay 69-85

Fill Material 85-90

Coarse Gravel 90-94

Limestone 94-96

Coarse Gravel 96-100

Water at 100

183786 J. Martin Channel Grove Mud 66

Gravel 66-72

Boulders 72-86

Solid Rock 96-104

774873 D. Kihlken 150 Church Rd. Yellow Clay 0-19

Blue Clay 19-38

Blue Gravel & Clay 38-52

Boulders 52-54

Gravel & Boulders 54-95

Black Gravel & Sand 95-100

Blue Gravel & Clay 100-105

Gravel 105-118

Gravel 118

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Crystal Rock outcrop is basically a rectangle ~ 1000’ wide and 4200’ long (Fig. 30) or ~0.15 square miles, less than half of the area enclosing the deeper wells on Marblehead. Artesian wells and springs that are high in sulfur and iron are found from the Sandusky Bay just north and east of the outcrop (Fig. 30), south through Castalia to the Columbus cuesta then southwest along the Lake

Fig. 30 Google photo of Crystal Rock Outcrop area. The Outcrop is surrounded by

artesian wells and springs.

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Warren beach ridge through Clyde to Green Springs, Ohio in Seneca County. From there the springs occur northward to and under the Sandusky Bay east to Crystal Rock. The water in the caves at Crystal Rock have little iron or sulfur. The static level of the water in the Crystal Rock cave is ~590’ or about the level of the surrounding ground (Norrocky 2011). With artesian wells surrounding but not affecting the water, it is obvious there is no connection between the aquifers. If the artesian aquifer had developed around the outcrop it would seem that the aquifers would affect each other. If the outcrop was placed on the artesian aquifer after it had developed, the aquifers could remain separate. The Marblehead void is ~ 0.38 square miles, Crystal Rock is 0.15 square miles so it could have come from Marblehead. The proposed channel just west of Crystal Rock (Fig. 9) could have influenced the deposition of a glaciotectonic structure. The outcrop is not too large to have been transported (Moran et al 1980). The slopes found at Crystal Rock Outcrop are definitely anomalous. The facts presented here lead toward the possibility that Crystal Rock outcrop is a glaciotectonic feature that could have originated along SR 163, east and south along Church Road, Danbury Twp., Ottawa County, Ohio.

ACKNOWLEDGEMENTS

I would like to thank the following people: 1) Jeral McMillan for help in the field, 2) Jim Keegan, Tom Bauman, Judy Terry, Keith and Guy Miller for access to their property; Dr. Ed Herdendorf, Ohio State Univ. for helpful suggestions, Dr. Stierman, Univ. Toledo for the seismic evaluation; Doug Aden ODNR Geology Dept. for his contributions and I would especially like to thank my sister, Mary Anne Lenhart for putting this and other articles on the web at Weebly.com

Bibliography

Aber J.S., & Ber A., 2007 – Glaciotectonism, Developments in Quaternary Sciences Volume 6: Elsevier, Amsterdam, 246 p. Byers, A.R. 1959. Deformation of the Whitemud and eastend Formations near Claybank, Saskatchewan. Transactions Royal Society Canada 53, series 3, sect. 4, p. 1-11. Carman, J. Ernest 1946 The Geologic Interpretation of Scenic Features in Ohio. Ohio Journal of Sci. V46(5) pgs. 241-283 Erie County Ohio Soil Survey, 1971 U.S. Dept. of Agriculture, Ohio Dept. of Nat. pp. 166 16 maps Forsyth, Jane L. and Kahle, C. F. 1983, Cruising the Columbus Cuesta. Ohio Association of Sedimentologists Field Guide. 7 pp.

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Herdendorf, Charles and Ronald Stuckey 1977 Lake Erie and the Islands Clear Technical Report No. 74 Hubbard, George D., 1924 Dimensions of the Cincinnati Anticline. Ohio Jour. Sci. V24(3): 161-168 Kihn, Gary E. 1988 Hydrogeology of the Bellevue-Castalia Area, North-Central Ohio, With an Emphasis on Seneca Caverns. 163 pp. 3 plates. Moran, S.R., Clayton, L., Hooke, R.LeB., Fenton, M.M. and Andriashek, L.D. 1980. Glacier-bed landforms of the Prairie region of North America. Journal Glaciology 25, p. 457-476. Norrocky, M. J. 2011 Determining the source of the water in Crystal Rock and Brewery Caves, northwest Margaretta Twp., Erie County, Ohio, U.S.A. 18 pgs. Published on Weebly.com Ohio Div. Of Geological Survey, 1997 Preliminary Bedrock Geology of the Castalia, Ohio quadrangle. Digital Map Series BG-2 Castalia. Riggs, E. A. 1960 Major Basins and Structural Features in the United States: The Geographical Press, New Jersey, 1 map. Sabo, Stephen 2008, Sabo, Stephen 2008, Evaluation of Capacitively - Coupled Electrical Resistivity For Locating Solution Cavities Overlain By Clay-Rich Soils. Masters Thesis pp. 50. Sears, Paul B. 1967. The Castalia Prairie. The Ohio Journal of Science 67(2): 79-88. ---------- 1926. The Natural Vegetation of Ohio, II. The Prairies The Ohio Journal of Science 26(3): 128-146. Sparling, Dale R., 1970 The Bass Islands Formation In Its Type Region. The Ohio Journal Science 70(1) pp. 1-32 Tintera, John J., 1980, The identification and interpretation of karst features in the Bellevue-Castalia region of Ohio. [Master's Thesis]: Bowling Green State University, Bowling Green, Ohio, 110 p. Verber, J. L. and Stansbery, D. H., 1953, Caves in the Lake Erie's Islands. Ohio Journal of Science, 53(6): 358-362.