HYDROGEOLOGIC FRAMEWORK OF THE

MIDWESTERN BASINS AND ARCHES REGION IN PARTS

OF INDIANA, OHIO, MICHIGAN, AND ILLINOIS

\

ILLINOIS

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1423-B
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Hydrogeologic Framework of the 

Midwestern Basins and Arches Region 

in Parts of Indiana, Ohio, Michigan, 

and Illinois

By GEORGE D. CASEY

REGIONAL AQUIFER-SYSTEM ANALYSIS MIDWESTERN BASINS AND ARCHES

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1423-B
U.S. DEPARTMENT OF THE INTERIOR 

BRUCE BABBITT, Secretary

U.S. GEOLOGICAL SURVEY 

Gordon P. Eaton, Director

Any use of trade, product, or firm names in this publication is for

descriptive purposes only and does not imply endorsement by the

U.S. Government.

Library of Congress Cataloging in Publication Data

Casey, George D.

Hydrogeologic framework of the midwestern basins and arches region in parts of Indiana, Ohio, Michigan, and Illinois / by 

George D. Casey

p. cm. -- (Regional aquifer-system analysis-midwestern basins and arches : B) (U.S. Geological Survey professional paper 

;1423)

Includes bibliographical references.

Supt. of Docs, no.: I 19.16:1423-B

1. Hydrogeology Middle West. 2. Aquifers-Middle West. 

I. Title. II. Series. III. Series: U.S. Geological Survey professional paper ; 1423. 

GB1017.C37 1996

551.49'0977~dc21 96-36377

CIP

For sale by the U.S. Geological Survey, Branch of Information Services, Box 25286,

Federal Center, Denver, CO 80225.

ISBN 0-607-86104-5
FOREWORD

THE REGIONAL AQUIFER-SYSTEM ANALYSIS PROGRAM

The Regional Aquifer-System Analysis (RASA) Program was started 

in 1978 following a congressional mandate to develop quantitative appraisals of the major ground-water systems of the United States. The RASA 

Program represents a systematic effort to study a number of the Nation's 

most important aquifer systems, which in aggregate underlie much of the 

country and which represent an important component of the Nation's total 

water supply. In general, the boundaries of these studies are identified by 

the hydrologic extent of each system and accordingly transcend the political 

subdivisions to which investigations have often arbitrarily been limited in 

the past. The broad objective for each study is to assemble geologic, 

hydrologic, and geochemical information, to analyze and develop an understanding of the system, and to develop predictive capabilities that will 

contribute to the effective management of the system. The use of computer 

simulation is an important element of the RASA studies, both to develop an 

understanding of the natural, undisturbed hydrologic system and the 

changes brought about in it by human activities, and to provide a means of 

predicting the regional effects of future pumping or other stresses.

The final interpretive results of the RASA Program are presented in 

a series of U.S. Geological Survey Professional Papers that describe the 

geology, hydrology, and geochemistry of each regional aquifer system. Each 

study within the RASA Program is assigned a single Professional Paper 

number, and where the volume of interpretive material warrants, separate 

topical chapters that consider the principal elements of the investigation 

may be published. The series of RASA interpretive reports begins with 

Professional Paper 1400 and thereafter will continue in numerical sequence 

as the interpretive products of subsequent studies become available.

Gordon P. Eaton 

Director

CONTENTS

Page

Foreword ........................................................................................ Ill

Abstract ...................................................................................... Bl

Introduction...................................................................................... 1

Purpose and Scope .................................................................... 1

Previous investigations ............................................................ 2

Acknowledgments ..................................................................... 3

Summary of Midwestern Basins and Arches Carbonate and 

Glacial Geology.......................................................................... 3

Regional Setting........................................................................ 3

Generalized Regional Geology................................................. 3

Relation of Stratigraphy and Hydrogeologic Units.............. 3

Stratigraphy ..................................................................................... 5

Ordovician Rocks....................................................................... 5

Silurian Rocks ........................................................................... 5

Stratigraphy Continued Pag<- 

Devonian Rocks ......................................................................... 9

Devonian and Mississippian Rocks ...................................... 13

Mississippian Rocks................................................................ 14

Glacial Deposits....................................................................... 14

Hydrogeologic Framework............................................................ 16

Glacial Deposits....................................................................... 17

Bedrock Aquifer andConfining Units................................... 19

Upper Confining Unit...................................................... 19

Carbonate-Rock Aquifer .................................................. 19

Basal Confining Unit....................................................... 24

Summary ....................................................................................... 26

Selected References ....................................................................... 28

ILLUSTRATIONS

[Plates are in pocket]

PLATE 1. Hydrogeologic section A-A', and map showing location of hydrogeologic sections in the Midwestern Basins

and Arches region

2. Map showing locations of hydrogeologic sections B-B', C-C', D-D', and E-E' in the Midwestern Basins 

and Arches region

Page

FIGURES 1-2. Maps showing:

1. Map showing location of data-collection and study areas in the Midwestern Basins and Arches region .................. 2

2. Map showing structural elements in the Midwestern Basins and Arches region.......................................................... 3

3. Generalized bedrock geologic map of the Midwestern Basins and Arches region ................................................................. 4

4. Chart showing time- and rock-stratigraphic framework and nomenclature for the Midwestern Basins

and Arches region ........................................................................................................................................................................... 6

5-9. Maps showing:

5. Approximate thickness and extent of the upper confining unit of the Silurian and Devonian carbonaterock aquifer system in the Midwestern Basins and Arches region ................................................................................. 8

6. Approximate altitude of the top of the upper confining unit of the Silurian and Devonian carbonaterock aquifer system in the Midwestern Basins and Arches region ................................................................................ 10

7. Location of Fort Wayne Bank and other contemporaneous bank-type deposits in the Midwestern Basins

and Arches region................................................................................................................................................................... 12

8. Generalized glacial deposits and location of Wisconsinan and maximum glacial limits in the

Midwestern Basins and Arches region ............................................................................................................................... 15

9. Generalized location of the Teays-Mahomet bedrock valley system in the Midwestern Basins

and Arches region................................................................................................................................................................... 16

10. Graph showing generalized responses of gamma-ray and electric logs to rock units in the Midwestern Basins

and Arches region......................................................................................................................................................................... 17

11-16. Maps showing:

11. Generalized thickness of glacial deposits in the Midwestern Basins and Arches region ........................................... 18

12. Approximate thickness and extent of the Silurian and Devonian carbonate-rock aquifer in the

Midwestern Basins and Arches region ............................................................................................................................... 21

13. Approximate altitude of the top of the Silurian and Devonian carbonate-rock aquifer in the Midwestern

Basins and Arches region...................................................................................................................................................... 22

14. Location of wells used to determine matrix permeability and porosity in the Midwestern Basins

and Arches region................................................................................................................................................................... 23

15. Approximate thickness and extent of the basal confining unit of the Silurian and Devonian carbonaterock aquifer system in the Midwestern Basins and Arches region ................................................................................ 25

16. Approximate altitude of the top of the basal confining unit of the Silurian and Devonian carbonaterock aquifer system in the Midwestern Basins and Arches region ................................................................................ 27
VI

CONTENTS

TABLES

Page

TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins

and Arches region ............................................................................................................................................................... 32

CONVERSION FACTORS AND DATUM

Factors for converting inch-pound units to the International System (SI) of units are given below:

Multiply By To obtain

foot (ft) 0.3048 meter

mile (mi) 1.609 kilometer

square mile (mi2 ) 2.590 square kilometer

foot per day (ft/d) 0.3048 meter per day

foot squared per day1 (ftVd) 0.0929 meter squared per day

^his unit is used to express transmissivity, the capacity of an aquifer to transmit water. Conceptually, transmissivity is cubic 

feet (of water) per day per square foot (of aquifer area) per foot (of aquifer thickness). In this report, the unit is reduced to its 

simplest form.

Sea Level: In this report, "sea level" refers to the National Geodetic Vertical Datum of 1929 (NGVD of 1929) a geodetic datum 

derived from a general adjustment of the first-order level nets of both the United States and Canada, formerly called Sea Level 

Datum of 1929.
REGIONAL AQUIFER-SYSTEM ANALYSIS-MID WE STERN BASINS AND ARCHES

HYDROGEOLOGIC FRAMEWORK OF THE

MIDWESTERN BASINS AND ARCHES REGION IN PARTS

OF INDIANA, OHIO, MICHIGAN, AND ILLINOIS

BY GEORGE D. CASEY

ABSTRACT

This report is a product of an extensive U.S. Geological Survey Regional-Aquifer Systems Analysis study 

undertaken to define the hydrology, geochemistry, and 

geologic framework of the Silurian and Devonian carbonate-rock aquifer system. The aquifer system underlies a 90,000-square-mile area in western Ohio; northern, central, and southeastern Indiana; and adjacent 

States and consists of Silurian and Devonian carbonate rock. Regionally, the carbonate-rock aquifer consists 

dominantly of limestones, dolomites plus subordinate 

amounts of terrigenous clastic rocks, and evaporites. 

The carbonate-rock aquifer system is underlain by 

Ordovician shales and interbedded carbonate rocks of 

the Maquoketa Group and undifferentiated Cincinnatian rocks that are virtually impermeable and regionally extensive. These units collectively form a 

barrier to ground-water flow that effectively limits the 

transfer of significant quantities of water through the 

base of the Silurian and Devonian carbonate-rock aquifer. Near the edge of the study area, the carbonate-rock 

aquifer is confined above by Devonian and Mississippian shales and siltstones. Where the upper confining 

unit has been eroded away, the overlying glacial sediments partially confine the carbonate-rock aquifer. This 

relationship between the glacial sediments and the 

Silurian and Devonian carbonate rocks prevails 

throughout much of the study area, where the potentiometric surface of the Silurian and Devonian carbonate rocks is within the overlying glacial deposits.

Data for this study were collected and analyzed from 

July 1989 through June 1993. Natural-gamma and 

electric geophysical well-log data and stratigraphic 

test-well data were examined from more than 2,500 

wells in the Midwestern Basins and Arches region. 

From these 2,500 wells, more than 1,700 were selected 

to determine the hydrologic framework on the basis of 

location, depth of geophysical log or core, and quality

of the log. A series of maps, together with five 

hydrogeologic sections, depicts the geometry, lateral 

extent, and horizontal and vertical relationships between the carbonate-rock aquifer and confining units.

INTRODUCTION

The U.S. Geological Survey's (USGS) Regional Aquifer-System Analysis (RASA) Program, initiated in 1978, 

was designed to determine and assess the water resources of major aquifer systems on a regional scale 

(Sun, 1986; Sun and Johnston, 1994). In 1988, the 

USGS began an extensive regional investigation, as 

part of the RASA Program, to (1) define the hydrogeologic framework, (2) simulate current ground-water 

flow, and (3) define the water chemistry and the 

geochemical basis for that chemistry in the Midwestern Basins and Arches region (Bugliosi, 1990).

The Midwestern Basins and Arches RASA data-collection area spans approximately 90,000 mi2 in parts 

of Indiana, Ohio, Michigan, Illinois, and Kentucky, as 

well as a small part of Canada (fig. 1). This area, which 

is approximately 380 miles wide and 230 miles long, 

straddles a regional arch complex (Kankakee, Cincinnati, and Findlay Arches) and extends into three structural basins (Appalachian, Michigan, and Illinois Basins). The study area is approximately 44,000 mi2 and 

is contained within the data-collection area in parts of 

Indiana, Ohio, Michigan, and Illinois (fig. 1).

PURPOSE AND SCOPE

This report defines the regional extent and configuration of the hydrogeologic units (aquifers and confining units) that compose the regional aquifer system in 

the Midwestern Basins and Arches region in order to 

further the understanding of ground-water hydrology 

and subsurface geology there. The regional aquifer 

system is depicted in maps showing the altitude of the

Bi
B2 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

top of the hydrogeologic units and their thickness and 

extent, as well as hydrogeologic sections. The hydrogeologic units are described in terms of age, stratigraphic position, depositional environment, regional 

stratigraphic correlations, lithology, configuration, areal 

extent, and geophysical-log signatures.

PREVIOUS INVESTIGATIONS

Few reports of a regional scope have been published 

about the geology or ground-water resources of the

Midwestern Basins and Arches region. Stratigraphic 

relations within this region have been compiled and 

documented by Shaver (1985). In Ohio, a comprehensive 

study of the limestones and dolomites of western Ohio 

was completed by Stout (1941). Shaver and others 

(1986) compiled a compendium of Paleozoic rock-unit 

stratigraphy in Indiana, and Hull (1990) proposed a 

generalized column of bedrock units in Ohio. Larsen 

(1991) researched and documented the development of 

Silurian and Devonian lithostratigraphy in northwestern Ohio, and Janssens (1970, 1977) discussed the Silv WEST r> 

VIRGINIA

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

0 20 40 60 MILES

0 20 40 60 KILOMETERS

EXPLANATION 

Data-collection area

 Boundary of study area

FIGURE 1. Location of data-collection and study areas in the Midwestern Basins and Arches region.
SUMMARY OF MIDWESTERN BASINS AND ARCHES CARBONATE AND GLACIAL GEOLOGY B3

urian and Devonian rocks in the subsurface of northwestern Ohio. The paleogeography of the Midwestern 

Basins and Arches region has been described by Droste 

and others (1975) and Droste and Shaver (1983,1987). 

The regional carbonate reef or bank-type deposits have 

been studied by Doheny and others (1975), Briggs and 

others (1978), Shaver and others (1978), and Ault and 

others (1992).

The hydrogeology of the Midwestern Basins and 

Arches region has not been previously addressed other 

than in several reports that have considered subregional 

areas. The occurrence of water in the Silurian and Devonian carbonate-rock aquifer in western Ohio was 

described by the Ohio Department of Natural Resources, Division of Water (Walker and others, 1970), as 

well as by Norris and Spieker (1961), Norris and Fidler 

(1971; 1973), and Norris (1979). Ground-water resources 

of the Whitewater River and Kankakee River basins 

were studied by the Indiana Department of Natural 

Resources (1988, 1990). A statewide survey of existing 

hydrogeologic data for Indiana was compiled by Geosciences Research Associates Inc. (1982). A ground-water atlas of the State of Indiana was compiled by 

Fenelon and others (1994).

ACKNOWLEDGMENTS

The author gratefully acknowledges Norman Hester 

(Indiana State Geologist), John Rupp, and Robert 

Shaver of the Indiana Geological Survey; John Droste 

of the Department of Geosciences, Indiana University; 

and Thomas Berg (Ohio State Geologist), Dennis Hull, 

E. Mac Swinford, Gregory Schumacher, Lawrence 

Wickstrom, Glen Larsen, and Douglas Shrake of the 

Ohio Geological Survey for furnishing well information, 

geophysical logs, selected stratigraphic cores, and invaluable knowledge of the Silurian and Devonian carbonate rocks.

SUMMARY OF MIDWESTERN BASINS AND ARCHES 

CARBONATE AND GLACIAL GEOLOGY

REGIONAL SETTING

The Midwestern Basins and Arches region is in the 

Interior Lowlands of Eastern North America (P.B. King, 

1977), which cover the central part of the North American craton and extend from the Appalachian Mountains 

system west to the Colorado Plateaus. The study area 

of the Midwestern Basins and Arches RASA is in western Ohio; northern, central, and southeastern Indiana; 

southeastern Michigan; and a small part of northeastern Illinois. This area spans the Kankakee, Cincinnati, 

and Findlay Arches (fig. 2). The axes of the Cincinnati 

and Kankakee Arches trend west-northwest to southeast, whereas the axis of the Findlay Arch trends southwest to north-northeast. This structurally positive feature has been described as the Wabash Platform because of the sedimentary deposition that took place in 

this area (Shaver and others, 1978). The study area is 

bounded on the north by the Michigan Basin, on the 

east by the Appalachian Basin, and on the west by the 

Illinois Basin (fig. 2).

MICHIGAN If ? ONTARIO

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

0 40 80 MILES

I i-H '

0 40 80 KILOMETERS

EXPLANATION 

Approximate location of basin 

 Approximate location of arch

FIGURE 2. Structural elements in the Midwestern Basins 

and Arches region.

GENERALIZED REGIONAL GEOLOGY

The data-collection area is underlain by sedimentary 

rocks that range in age from Precambrian through 

Mississippian; however, only Ordovician (Cincinnatian) 

through Mississippian rocks crop out (fig. 3). The sedimentary rocks of primary interest range in age from 

Cincinnatian through Early Mississippian. These units 

dip away from the crests of the arches and thicken into 

the adjacent structural basins. The oldest sedimentary 

rocks are exposed along the crest of the Cincinnati Arch 

in southwestern Ohio and southeastern Indiana (figs. 

2 and 3) and are overlain by younger strata toward the 

center of the basins.

RELATION OF STRATIGRAPHY AND HYDROGEOLOGIC UNITS

The basal confining unit of the carbonate-rock aquifer system in the Midwestern Basins and Arches region
B4 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

20

I

40 60 MILES

_]______I

I__] Pennsylvanian 

HM Mississippian

i l I

20 40 60 KILOMETERS

EXPLANATION 

Geologic time units

[HI Devonian 

HI Silurian

Geology compiled and modified from Bownocker (1920). 

Burger and others (1971), Gray (1972b), Gray and others 

(1972), Gray and others (1979), Grey and others (1987), 

Willman and others (1967), Milstein (1987)

[ J Ordovician 

 Contact

FIGURE 3. Generalized bedrock geologic map of the Midwestern Basins and Arches region.
STRATIGRAPHY B5

consists of shales and minor interbedded limestones of 

Ordovician age (fig. 4). The carbonate-rock aquifer consists of Silurian and Devonian limestones and dolomites. The rocks that compose the aquifer in Indiana 

can be grouped into four major stratigraphic units, 

whereas the equivalent rocks in Ohio have not been 

grouped into major stratigraphic units (fig. 4). The upper confining unit of the carbonate-rock aquifer system 

consists of upper Middle Devonian, Upper Devonian, 

and Lower Mississippian shales and siltstones (fig. 4). 

Where the shales and siltstones have been removed by 

erosion, the overlying glacial deposits function as a 

moderately permeable regional confining unit.

The basal confining unit thickens eastward from the 

western border of Indiana toward Ohio (pis. 1 and 2). 

The basal confining unit in Ohio gradually thickens as 

it dips into the Appalachian Basin (pi. 2). The basal 

confining unit thins where it crops out in southeastern 

Indiana and southwestern Ohio because of pre-Silurian 

erosion of the unit and post-Permian uplift and subsequent erosion along the crest of the Cincinnati Arch (pi. 

2).

In southeastern Indiana and southwestern Ohio, the 

Silurian and Devonian carbonate-rock aquifer increases 

in thickness from its contact with the underlying Ordovician shales (the updip edge of the carbonate-rock 

aquifer) as it is traced downdip into the various structural basins (pis. 1 and 2). Along the crests of the arches, 

in a structurally high position, the aquifer units crop out 

and have been subjected to several extensive periods of 

erosion. This erosion has resulted in the loss of entire 

sections of the carbonate-rock aquifer in the central part 

of the study area.

In Ohio and northern Indiana, the upper confining 

unit increases in thickness from its contact between the 

Middle Devonian carbonates and the updip edge of the 

Upper Devonian shales as it is followed downdip into 

the Appalachian and Michigan Basins (pis. 1 and 2). In 

central and southwestern Indiana, the upper confining 

unit increases in thickness from its contact between the 

Middle Devonian carbonates and the updip edge of the 

Middle and Upper Devonian shales as it is traced 

downdip toward the Illinois Basin (pis. 1 and 2).

Along the crests of the arches, in structurally high 

positions, the upper confining unit has been subjected 

to several extensive periods of erosion. This erosion has 

resulted in the loss of entire sections of the confining 

unit in the central part of the study area, with the exception of the so-called Bellefontaine outlier, which is 

approximately 50 miles northwest of Columbus, Ohio 

(figs. 5 and 6).

STRATIGRAPHY

ORDOVICIAN ROCKS

The nomenclature of the basal confining unit of the 

Silurian and Devonian carbonate-rock aquifer system 

depends largely on the geographic location. In Indiana, 

it is referred to as the Maquoketa Group, both in the 

subsurface and as a subcrop unit in southeastern Indiana near the Ordovician outcrop (Gray and others, 

1985). In Ohio terminology, the names of outcrop units 

are used to describe the Upper Ordovician rocks in 

southwestern Ohio; however, in the subsurface in northwestern Ohio, the Upper Ordovician unit is described 

as undifferentiated Cincinnatian shale and limestone 

(Hull, 1990). In order to minimize confusion and to 

maintain uniformity with the usage of the various State 

geological surveys, this RASA study has adopted the 

names "Maquoketa Group" in Indiana and "undifferentiated Cincinnatian rocks" in Ohio (Shaver, 1985) (fig. 

4). This naming convention follows the usage of the Ohio 

Geological Survey and the Indiana Geological Survey.

The Upper Ordovician units are present throughout 

the study area and unconformably overlie the Trenton 

Limestone in Indiana, except in southeastern Indiana 

where the Ordovician units conformably overlie the 

Kope Formation (Gray, 1972b; Droste and Shaver, 

1985). In northwestern and central Ohio, the undifferentiated Cincinnatian rocks unconformably overlie the 

Trenton Limestone (Janssens, 1977). The Upper Ordovician units are overlain unconformably by either the 

Sexton Creek Limestone or Brassfield Limestone and 

the Cataract Formation of Silurian age (LaFerriere and 

others, 1986).

The Maquoketa Group or the undifferentiated 

Cincinnatian rocks are a clastic wedge that extends 

across the study area from the west. The shale that 

predominates in these units is generally gray and calcareous, but a brown carbonaceous shale (100-300 ft 

thick) is present in the lowermost part of the unit. Approximately 20 percent of the basal confining unit is 

composed of limestone, predominantly in the uppermost 

part of the unit (Gray, 1972b).

SILURIAN ROCKS

The Silurian rocks that compose the carbonate-rock 

aquifer in Indiana and northeastern Illinois can be 

grouped into three major stratigraphic units: the 

equivalent units consisting of the Brassfield Limestone, 

Sexton Creek Limestone, or the Cataract Formation; the 

Salamonie Dolomite; and the Salina Group (fig. 4). The 

stratigraphic units in Ohio and southern Michigan have
B6 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

GENERALIZED GEOLOGIC UNITS

SYSTEM

QUATERNARY

 z. 

51

D_

MISSISS

DEVONIAN

z

EE

 1 

CO

y ORDOVICIAN

SERIES

PLEISTOCENE

LOWER

UPPER

MIDDLE

LOWER

CAYUGAN

NIAGARA

ALEXANDRIAN

CINCINNATIAN

"MIDDLE

Southeastern 

Indiana

Glacial 

deposits

Borden 

Group

Rockford LimestoneS: ; ; ;

New Albany 

Shale

Muscatatuck 

Group

;

; ; : Salina1 

; J; Group

} Salamonie1 

} Dolomite,^

Brassfield \ \ 

Limestone _Ni

Maquoketa1 

Group ,-,.- -

&

Northwestern 

to east-central 

Indiana

Glacial 

deposits

BordoV 

Group

Rockford Ls.

New 

Albany 

Shale

Musc< 

Gr

 i 

i

:

 ^Ellsworth 

Shale

Antrim 

Shale

ata

ou

tuck

3

Salina1 

Group

Salamo 

Dolom

Sexton"^. 

Creek Ls. 1 

Brassfield 

Limestone

Cataract * 5; 

Formation _

/'

Maquoketa1 

Group

^f

i

W \

ws* i

Northern 

Indiana

Glacial 

deposits

Northwestern 

Ohio and 

southeastern 

Michigan

Glacial 

deposits

; t

Coldwater Shale ~ \

\Suntury Sh.

Ellsworth Shale

Antrim Shale

Traverse 

Formation

Detroit 

River 

Formation

Group/ Muscatatuck 

Salina1 

Group

Salamo 

Dolom

Brassfield 

Limestone

nie1

tei 

+.

Ccc

L_

cc

0 '.C3

P

co iMaquoketa1 

Group

liijjljgjpig^te ft!

.* ».

^ fa

Bedford Shale

Antrim 

Shale

Traverse 

Formation

Dundee_Ls.jgelaware Ls. 

Columbus Limestone

Detroit River 

Formation

Lock 

Dolo

Salina 

Group

port 

mite

Rochester Shale equiv.

Brassfield 

.imestone

\m

; 

ftp> -

: H??" "

Cataract 

Formation

~ aunt

m% 

Wft: j

Central and 

western 

Ohio

Glacial 

deposits

f: '!

1 ;i

Ohio 

Shale

Olentangy Shale

Delaware

Columbus 

Limestone

Detroit River 

Group

Salina 

Group

e

i| D

juelph 

olomite2

^ § Goat Island 

o "o Dolomite2

 ' "-1 Gasport 

Dolomite2

Rochester Shale equiv.

'? ^"

Brassfield 

Limestone

^^^-*-

Cataract 

Formation

^_..

Mil*'"*" tone :

Southwestern 

Ohio

Glacial 

deposits

i: :«

' -3

Bedford Shale

Ohio 

Shale

oientangy&Taie

Hillsboro Sandstone

Salina Group

Lockport 

Dolomite

Rochester Shale equiv

Dayton Limestone

Brassfield Limestone

i ' ,>*" ~^U

GENERALIZED 

GEOHYDROLOGIC UNITS

Glacial aquifers and 

confining unit

Upper 

confining 

unit

Carbonate 

rock 

aquifer

Basal 

confining 

unit

 

. ~~~~ - s" 

SILURIAN CARBONATE-ROCK AND DEVONIAN AQUIFER SYSTEM

1 Follows usage of the Indiana Geological Survey (Gray and others, 1985) 

X

2 Follows usage of th Ohio Geological Suvery (Hull, 1990; Larsen 1991)

I Non-deposition or erosion

EXPLANATION 

Intervals not included in investigation

Geology modified from Bugliosi (1990) 

Unconformity

FIGURE 4. Stratigraphic chart showing time- and rock-stratigraphic framework and nomenclature for the Midwestern Basins

and Arches region.
STRATIGRAPHY B7

been subdivided more than those in Indiana. In Ohio 

and southeastern Michigan, the Silurian rocks that 

compose the carbonate-rock aquifer are the Brassfield 

Limestone or the Cataract Formation, the Dayton Limestone, the Rochester Shale equivalent, the Lockport 

Dolomite and its equivalent units, and the Salina Group 

(fig. 4).

During Alexandrian and early Niagaran time, tectonic 

events in the Great Lakes region were continuing to be 

affected by the Taconic orogeny. In northwestern Ohio, 

northeastern Indiana, and southern Michigan, the accumulation of Alexandrian and lower Niagaran carbonates was affected by depositional environments that 

were restricted to the Michigan Basin. This resulted in 

the deposition of the Cataract Formation, which is 

mostly a dolomite in the lower one-third of the formation and an impure and argillaceous dolomite in the 

upper two-thirds (Shaver and others, 1986). The Cataract Formation is conformably overlain in the extreme 

northwestern part of Indiana by the Salamonie Dolomite, and in this area, the basal section of the 

Salamonie Dolomite is in a facies relation with the 

upper part of the Cataract Formation (Rexroad and 

Droste, 1982). In most of the region, the Cataract Formation is unconformably overlain by either the 

Salamonie Dolomite or the Dayton Limestone.

In southeastern Indiana and southwestern Ohio, carbonate-sediment accumulation during Alexandrian and 

early Niagaran time was affected by the depositional 

environments within the Illinois and Appalachian Basins. This resulted in the deposition of the Brassfield 

Limestone, a medium- to coarse-grained fossiliferous 

limestone that is locally dolomitized and contains thin, 

noncontinuous stringers of shale (Shaver and others, 

1986; Stout, 1941). The Brassfield Limestone is 

unconformably overlain by either the Salamonie Dolomite or the Dayton Limestone.

In the western one-half of Indiana, the accumulation 

of Alexandrian and lower Niagaran carbonate sediments was affected by the depositional environments 

within the Illinois Basin, which resulted in the deposition of the Sexton Creek Limestone, a very cherty, impure limestone or dolomite. In northwestern Indiana 

and northeastern Illinois, the lowest section of this unit 

is an argillaceous dolomite or a dolomitic shale (Rexroad 

and Droste, 1982; Shaver and others, 1986). The Sexton Creek Limestone is unconformably overlain by the 

Salamonie Dolomite in the western one-half of Indiana, 

with the exception of a small part of northwestern Indiana where the Salamonie Dolomite conformably overlies the Sexton Creek Limestone (Rexroad and Droste, 

1982).

During middle Niagaran time, the Great Lakes region 

underwent a period of relative tectonic quiescence, as

compared to Alexandrian and early Niagaran time, and 

was accompanied by a marine transgression (Shaver 

and others, 1986). In western Ohio, this transgression 

resulted in the deposition of the Dayton Limestone and 

the Rochester Shale equivalent rocks. The Dayton Limestone is a saccharoidal, coarsely crystalline, mediumbedded dolomite (Stout, 1941; Ausich, 1987). The name 

Rochester Shale equivalent refers to several members 

that have been described as containing soft calcareous 

clay shale and thin layers of dolomite (Stout, 1941; Hull, 

1990). These stratigraphic units are comparable in character to the lowest part of the Salamonie Dolomite in 

southeastern Indiana and the highest part of the Cataract Formation in northern and east-central Indiana 

(Shaver and others, 1986).

The Salamonie Dolomite consists of two distinct 

lithologies. The basal part generally is a fine-grained, 

impure, argillaceous limestone, dolomitic limestone, and 

shale (Shaver and others, 1986). This basal part is correlative to the Dayton Limestone and the Rochester 

Shale equivalent in Ohio as described above. The upper 

part of the Salamonie Dolomite is generally a uniform, 

pure, white to light-gray dolomite that has a coarsegrained, bioclastic, vuggy texture (Shaver and others, 

1986). In Ohio, the correlative unit of the upper part of 

the Salamonie Dolomite is the lower and middle part of 

the Lockport Dolomite.

The Lockport Dolomite conformably overlies the Rochester Shale equivalent and is conformably overlain, with 

minor local unconformities near reef-bank facies 

(Shaver, 1991), by the Salina Group, where the Salina 

has not been eroded from above the Lockport Dolomite. 

In central and western Ohio, the Lockport Dolomite 

interval has been subdivided into the Gasport Dolomite, 

the Goat Island Dolomite, and the Guelph Dolomite 

(Janssens, 1977). The Gasport Dolomite is a microcrystalline to coarsely crystalline, medium- to dark-gray 

dolomite. The Goat Island Dolomite is a microcrystalline to finely crystalline, light-brown to light-gray-brown 

dolomite. The Guelph Dolomite is a fossiliferous, predominantly coarsely crystalline, vuggy, white to lightgray dolomite. The term "undifferentiated Lockport 

Dolomite" is used in Ohio only for areas where a distinct 

lithology cannot be determined for the Goat Island Dolomite; therefore, the Lockport Dolomite includes the 

Gasport and Goat Island Dolomite equivalent rocks and 

the Guelph Dolomite (Janssens, 1977).

Droste and Shaver (1976) described the Salamonie 

Dolomite as a laterally extensive, blanketlike deposit of 

carbonate rocks that covered the entire State of Indiana 

before the multiple post-Silurian periods of erosion. This 

description can be extended to the correlative Lockport 

Dolomite of Ohio. The pre-Devonian erosion resulted in 

the removal of not only the Salamonie and the Lockport
B8 REGIONAL AQUIFER-SYSTEM ANALYSIS-MID WESTERN BASINS AND ARCHES

Dolomites but also the Silurian strata below these units 

in the south-central part of the study area.

During late Niagaran time, the Great Lakes region 

underwent a series of marine regressions and transgressions as the result of a combination of tectonic forces

exerted by (1) deposition within the structural basins, 

(2) emplacement of an overthrust on the eastern margin of the North American Craton in the present-day 

Middle Atlantic States, and (3) possible eustatic sealevel changes (Beaumont and others, 1988; Shaver and

Lake 

 A Michigan

" iChicago

38° -j

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

0 20 40 60 KILOMETERS

EXPLANATION

Lines of equal thickness of the upper confining unit from Casey (in press) 

Geology compiled and modified from Bownocker (1920), Burger and 

others (1971), Gray (1972b), Gray and others (1972), Gray and others 

(1979), Grey and others (1987), Willman and others (1967), Milstein (1987) 

Data on location and extent of faults compiled from Bassett and 

Hasenmueller (1979), VanWagner (1988)

200 

 400 

 800 

-1,000 

Approximate thickness of the 

upper confining unit Lines of 

equal thickness dashed where infered. 

Interval 200 feet. Darker colors indicate 

greater thickness

P I Subcrop of Silurian and Devonian carbonate rocks

[::::::;:;:j Subcrop of Ordovician shales

 Location of the Bowling Green fault zone

T i r Fault Hachures on downthrown side

FIGURE 5. Approximate thickness and extent of the upper confining unit of the Silurian and Devonian carbonate-rock aquifer system

in the Midwestern Basins and Arches Region.
STRATIGRAPHY B9

Sunderman, 1983; Onasch and Kahle, 1991). The Salina 

Group conformably and unconformably overlies the 

Salamonie Dolomite and the Lockport Dolomite. The 

unconformities are considered to be minor local 

unconformities near the reef-bank facies (Shaver, 1991). 

The upper contact of the Salina Group is a regionally 

extensive unconformity. The overlying Devonian rocks, 

where present, range in age from Early to Middle Devonian (Droste and Shaver, 1982; Hull, 1990).

In Indiana, the Salina Group includes a diverse assemblage of dominantly carbonate rocks that range from 

fine-grained argillaceous rocks to a pure carbonate mud. 

The Salina Group also includes a coarse-grained, 

bioclastic, vuggy, and fossiliferous facies that consist of 

reef-framework rocks (Shaver and others, 1986). In 

Indiana, south of a paleogeographic feature named the 

"Fort Wayne Bank" (fig. 7), the lower one-half of the 

Salina Group contains three distinct facies (Pinsak and 

Shaver, 1964). These facies consist of a micritic to finegrained and sucrosic dolomite; an argillaceous to shaly, 

fine-grained, thin-bedded dolomite; and a reef facies. 

The reef facies grades from a fully mature reef rock to 

what has been described as an incipient reef rock 

(Shaver and others, 1986). North of the Fort Wayne 

Bank, the reef facies generally is absent. Instead, the 

dolomites that compose the lower one-half of the Salina 

Group north of the Fort Wayne Bank consist of a darkbrown, micritic to fine-grained, partially laminated 

dolomite and a lighter colored, granular, vuggy dolomite 

(Shaver and others, 1986).

The upper one-half of the Salina Group in Indiana was 

deposited during latest Niagaran to earliest Cayugan 

time. These rocks contain several lithologies that grade 

into one another across the western one-half of the 

study area (Shaver and others, 1986). The lithologies of 

these rocks include dense to fine-grained, calcareous, 

silty dolomite; dolomitic, silty limestone; fine-grained, 

light-colored limestone; dolomitic limestone; and dolomite. Also included are micritic to fine-grained, thinly 

laminated limestone; granular, vuggy dolomite; and 

carbonate mudstones that are contained within the 

bank, reef, reef-detrital, and biohermal deposits.

The upper part of the Salina Group has been subjected 

to post-Cayugan, pre-Middle Devonian subaerial exposure and erosion. This is apparent where the uppermost 

part of the Salina Group is exposed within quarries. At 

several locations in Indiana where the Cayugan carbonate rocks have not been removed by erosion, paleokarst 

features are evident. The paleokarst features consist of 

caves, grykes (solution-widened fissures), solution-widened bedding joints, and fractures derived from the 

settling of reef-flank deposits (Shaver, 1989). The 

paleokarst features are filled with a whitish quartz sand 

and a shaly material, which are cave breakdown that

consists of the local host rock, and what appears to be 

pisolites. As evidence of the age of these features in 

relation to the overlying sediment, Shaver (1989) described a calcareous shaly material that fills a cave and 

contains Devonian conodonts.

In Ohio, the Salina Group consists of a diverse assemblage of carbonate and evaporate deposits. This group 

ranges from an argillaceous, microcrystalline dolomite, 

which includes a stromatolitic dolomite representing a 

biohermal facies, to a saccharoidal, medium-grained 

dolomite and bedded evaporate deposits (Janssens, 

1977).

In northwestern Ohio, the Salina Group contains 

lithologies that also vary with the location. In the western one-half of northwestern Ohio, the Salina Group 

contains the following dominant lithologies: (1) a stromatolitic brown dolomite, (2) a partly argillaceous, silty, 

microcrystalline dolomite that contains some shale, (3) 

a microcrystalline dolomite that is partially laminated, 

argillaceous, and pelletal and that locally contains secondarily deposited gypsum (Janssens, 1977), and (4) a 

karst facies that contains mud cracks, as well as caverns that are believed to contain secondary fillings of 

Devonian sediments (G.E. Larsen, Ohio Geological Survey, oral commun., 1992).

A facies change has been noted within the Salina 

Group of northwestern Ohio east of the Bowling Green 

Fault Zone (fig. 5), where it contains dolomite, bedded 

anhydrite, very argillaceous dolomite, and shale. 

Janssens (1977, p. 23) described it as "an important 

updip facies of the salt-bearing Salina rocks of eastern 

Ohio". This facies change in northwestern Ohio could be 

the result of several periods of movement along the 

Bowling Green Fault Zone and their effect on depositional environments, coupled with subsidence in the 

Michigan Basin during this depositional episode 

(Onasch and Kahle, 1991).

In southwestern Ohio, the Salina Group has been 

subjected to a greater amount of post-Cayugan, preMiddle Devonian erosion than in northwestern Ohio. 

Ulteig (1964, p. 34) suggested that the "Upper Silurian 

units under cover of the Devonian carbonates are truncated in a southwesterly direction". This erosion of the 

upper section of the Salina Group in southwestern Ohio 

leaves only the basal section, which consists of a pure 

crystalline dolomite that exhibits medium to massive 

bedding and has a sucrosic texture; an argillaceous to 

shaly dolomite; and a dolomite that has a reeflike character (Stout, 1941).

DEVONIAN ROCKS

The Devonian rocks that compose the carbonate-rock 

aquifer in Indiana can be grouped into two major strati-
BIO REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

graphic units, the Detroit River and Traverse Formations, which together make up the Muscatatuck Group 

(fig. 4). The stratigraphic units in Ohio and southeastern Michigan have been subdivided more than those in 

Indiana. In Ohio and southeastern Michigan, the Devonian rocks that compose the carbonate-rock aquifer are 

the Hillsboro Sandstone, the Detroit River Group or 

Formation, the Columbus Limestone, the Delaware 

Limestone or the Dundee Limestone, and the Traverse 

Formation (fig. 4).

38° -,

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

20 40 60 MILES

0 20 40 60 KILOMETERS

EXPLANATION

Altitude of top of the upper confining unit from Caseyfin press) 

Geology compiled and modified from Bownocker (1920), Burger and 

others (1971), Gray (1972b), Gray and others (1972), Gray and others 

(1979), Grey and others (1987), Willman and others (1967), Milstein (1987) 

Data on location and extent of faults compiled from Bassett and 

Hasenmueller (1979), VanWagner (1988)

1,200-1

 1,000--

 800 

 BOO 

 400 

 200 

SEA LEVEL- 0 

 200 

 tOO 

 -600 

 -800 

 1,000 

 1,200 

 1,400-*

Approximate altitude of the top of the 

upper confining unit Contour interval 

200 feet. Dashed where inferred. Datum 

is sea level. Darker greens indicate greater 

elevation above sea level; darker blues 

indicate greater depth below sea level

[ ~] Subcrop of Silurian and Devonian carbonate rocks

Subcrop of Ordovician shales 

 Location of the Bowling Green fault zone 

T i r Fault Hachures on downthrown side

FIGURE 6. Approximate altitude of the top of the upper confining unit of the Silurian and Devonian carbonate-rock aquifer system

in the Midwestern Basins and Arches region.
STRATIGRAPHY Bll

The Antrim Shale and the Ellsworth Shale are the 

upper Middle Devonian and Upper Devonian shales 

that make up the upper confining unit of the Silurian 

and Devonian carbonate-rock aquifer system north of 

the Kankakee and Findlay Arches in northern Indiana, 

southeastern Michigan, and northwestern Ohio. South 

and west of the Kankakee and Cincinnati Arches in 

southeastern, northwestern, and east-central Indiana, 

the equivalent lithologic unit to the Antrim Shale is the 

New Albany Shale (fig. 4) (Lineback, 1970; Shaver and 

others, 1986). East of the Cincinnati Arch and south of 

the Findlay Arch in central-western and southwestern 

Ohio, the equivalent lithologic unit is the Olentangy 

Shale, Ohio Shale, and the lower part of the Bedford 

Shale (fig. 4).

After the post-Cayugan, pre-Middle Devonian erosional event, the Great Lakes region was again a site 

of carbonate and evaporite deposition. The controlling 

tectonic forces of this depositional event were the 

Acadian orogeny and a major subsidence episode in the 

Michigan and Illinois Basins (Droste and Shaver, 1983; 

Beaumont and others, 1988). The late Niagaran and 

Cayugan Fort Wayne Bank (fig. 7) also is thought to 

have played a large role in the deposition of the Middle 

Devonian carbonate rocks. As a resistant carbonate reefbank facies, it may have functioned as a barrier or a sill 

during the early deposition of the Detroit River Group 

or the Detroit River Formation of the Muscatatuck 

Group (Doheny and others, 1975). Some investigators 

(Doheny and others, 1975; Briggs and others, 1978) 

have proposed that the Fort Wayne Bank was a continuous feature that extended from northwestern Indiana 

to northwestern Ohio (fig. 7). The Fort Wayne Bank, in 

conjunction with another carbonate bank in southern 

Michigan (proposed by Briggs, 1959), formed a restricted evaporite basin in northern Indiana, northwestern Ohio, and southern Michigan (Mesolella and others, 

1974).

In northern Indiana, northwestern Ohio, and southern Michigan, the Detroit River Formation was deposited during late Early Devonian and Middle Devonian 

time. This stratigraphic unit unconformably overlies 

rocks of the Salina Group that become progressively 

younger from the Wabash Platform into the Michigan 

Basin. In northern Indiana, the Detroit River Formation is unconformably overlain by the Traverse Formation. In northwestern Ohio, the Detroit River Formation 

is conformably overlain by a thin section of the Columbus Limestone. The Detroit River Formation was described by Janssens (1970) and Shaver and others 

(1986) as having several distinct facies. The basal unit 

consists of a sandy dolomicrite that grades to a fine- to 

medium-grained sandstone, which is cemented by dolomite and contains thin lenses of dolomicrite. This

basal unit grades upward into a fine-grained, laminated 

dolomite, dolomicrite, and dolosiltite that contains anhydrite and gypsum nodules (Janssens, 1970; Shaver 

and others, 1986).

In central and western Ohio, southeast of the eastern 

extension of the Fort Wayne Bank, the Detroit River 

Group was described by Stout (1941) as a true dolomite 

that grades into a calcareous dolomite. This limy dolomite is finely crystalline, light to brownish gray, and 

finely banded and contains no evaporites. The absence 

of evaporites can be explained by the presence of a more 

open, nonrestricted depositional environment south and 

east of the eastern extension of the Fort Wayne Bank 

in central and western Ohio (fig. 7).

The carbonate rocks that are present in southwestern 

Ohio were subjected to a large amount of erosion after 

early Cayugan and during Middle Devonian time. Locally, where it has not been eroded, the Hillsboro Sandstone unconformably overlies the Salina Group and is 

unconformably overlain by the Olentangy Shale, which 

makes up the lowest part of the upper confining unit. 

The Hillsboro Sandstone is said to be a clean, very pure, 

well-sorted, angular silicious sand (Orton, 1888).

In northwestern, east-central, and southeastern Indiana, the entire Middle Devonian carbonate-rock sequence is classified as the Muscatatuck Group (Shaver, 

1974). The Muscatatuck Group unconformably overlies 

the Salina Group strata that become progressively 

younger from the Kankakee Arch into the Illinois Basin. In southeastern Indiana, the Muscatatuck Group 

is unconformably overlain by the New Albany Shale, 

which makes up the upper confining unit. In northwestern and east-central Indiana, the New Albany or Antrim 

Shale contact with the Muscatatuck Group generally is 

unconformable, but in places, the contact is conformable 

(fig. 4) (Shaver and others, 1986).

In northern Indiana, the Muscatatuck Group is divided into the Detroit River and Traverse Formations 

(Shaver and others, 1986). Several dominant carbonate 

lithologies are present in the Muscatatuck Group. The 

lowest part consists of a sandy, fine-grained, quartz-rich 

dolomite or a dolomitic quartz sandstone overlain by a 

granular, vuggy dolomite. These basal units are overlain 

by shaly to pure, granular limestone and dense, lithographic to fine-grained, typically laminated dolomites 

and dolomitic limestones (Becker, 1974; Shaver and 

others, 1986). Certain coarsely granular and fibrous 

anhydrite and gypsum deposits within the Muscatatuck 

Group correlate with the Detroit River Formation in 

northern Indiana (Becker, 1974; Shaver and others, 

1986).

In central and western Ohio, the Columbus Limestone 

unconformably overlies the Detroit River Group (where 

the Detroit River Group is recognized) and is uncon-
B12 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

formably overlain by the Delaware Limestone (Hall and 

Alkire, 1956; Dow, 1962; Hull, 1990; Larsen, 1991). The 

Columbus Limestone consists of a basal brown, highly 

crystalline and porous dolomite or dolomitic limestone 

overlain by a massive, gray, fossiliferous limestone that 

locally contains some chert (Westgate, 1926; Stout, 

1941; Hall and Alkire, 1956).

In northwestern Ohio, the Detroit River Formation is 

conformably overlain by a thin section of the Columbus 

Limestone (Shaver, 1985). The Columbus Limestone is

unconformably overlain by the Dundee and Delaware 

Limestones (fig. 4), which are laterally equivalent. The 

Dundee Limestone is a saccharoidal, sandy, fine- and 

medium-grained crystalline dolomitic limestone or dolomite that contains nodular chert (Janssens, 1970). The 

Delaware Limestone is a fine-grained, argillaceous and 

fossiliferous limestone (Janssens, 1968). The Dundee 

and Delaware Limestones are unconformably overlain 

by the Traverse Formation (fig. 4).

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

0 20 40 60 MILES

I i-h H '

0 20 40 60 KILOMETERS

EXPLANATION 

I Carbonate reef bank deposits

I Eroded Silurian and Devonian 

carbonate rock

FIGURE 7. Location of Fort Wayne Bank and other contemporaneous bank-type deposits in the Midwestern Basins and Arches region.
STRATIGRAPHY B13

The Traverse Formation in northwestern Ohio contains two major lithologies. The basal part of the 

Traverse is a fine- to coarse-grained, argillaceous and 

fossiliferous limestone interbedded with calcareous 

shale. The upper part consists of a dense to mediumgrained crystalline dolomite that contains lenticular and 

nodular chert and minor interbedded shaly dolomite 

and shale (Janssens, 1970). The Traverse Formation 

unconformably overlies the Dundee and Delaware Limestones and is unconformably overlain by the Antrim 

Shale (Janssens, 1970; Hull, 1990; Larsen, 1991). The 

Antrim Shale makes up the lowest part of the upper 

confining unit of the Silurian and Devonian carbonaterock aquifer system in northwestern Ohio.

The Traverse Formation in northern Indiana is lithologically similar to the strata of the same name in Ohio. 

In Indiana, the Traverse Formation contains the following distinct lithologies: (1) a basal dense, micritic, fossiliferous limestone; (2) a highly fossiliferous, lithographic and sublithographic limestone that grades from 

northwestern to northeastern Indiana into a fossiliferous calcareous shale and an argillaceous limestone; and 

(3) a cherty, dense to medium-grained dolomite that 

overlies both of these units (Shaver and others, 1986). 

The Traverse Formation unconformably overlies the 

Detroit River Formation. The Traverse Formation overlies progressively younger parts of the Detroit River 

Formation updip from the Michigan Basin onto the 

Wabash Platform (Shaver and others, 1986). The 

Traverse Formation is overlain conformably and 

unconformably by the Antrim Shale (Shaver and others, 

1986). In northern Indiana, the Antrim Shale is the 

lowest part of the upper confining unit of the carbonaterock aquifer system.

In central and western Ohio, the Delaware Limestone 

unconformably overlies the Columbus Limestone and is 

unconformably overlain by the Olentangy Shale 

(Shaver, 1985; Hull, 1990; Larsen, 1991). The Olentangy 

Shale is the basal part of the upper confining unit of the 

Silurian and Devonian carbonate-rock aquifer system in 

central and western Ohio. The Delaware Limestone 

consists of a basal section of thinly bedded limestone 

that contains nodules of chert and thin layers of shale. 

This basal section grades into an argillaceous limestone, 

which contains beds of chert, and a massive limestone 

unit (Hall and Alkire, 1956; Dow, 1962; Janssens, 1968).

During late Middle Devonian and Late Devonian time, 

the Acadian orogeny caused the formation of the 

Catskill delta complex, which spread from the northeastern Appalachian Basin south along the trend of the 

basin and west onto contiguous sections of the craton. 

The Acadian Mountains were uplifted along the eastern 

margin of the craton and were a source area for the 

sediments that were shed into the Appalachian Basin

(Ettensohn and Barron, 1981). The Catskill delta complex had a widespread distribution that ranged from the 

source area near the cratonic margin, across the Appalachian Basin onto the Cincinnati, Findlay, and 

Kankakee Arches, and into the east- and north-central 

midcontinent area of Illinois and eastern Iowa to the 

northwest (Ettensohn and Barron, 1981; Devera and 

Hasenmueller, 1991).

In central and western Ohio, the Olentangy Shale 

unconformably overlies the Delaware Limestone and is 

unconformably overlain by the Ohio Shale (Hoover, 

1960; Larsen, 1991). In southwestern Ohio, the 

Olentangy Shale unconformably overlies the Hillsboro 

Sandstone (Devonian) and is unconformably overlain by 

the Ohio Shale (Hull, 1990; Larsen, 1991). The Olentangy shale is a bluish-gray to greenish-gray, clay-rich 

shale that has black, fissile shale beds in the upper part 

of the unit; these black shale beds are more numerous 

in southwestern Ohio (Hoover, 1960).

The Ohio Shale in central, western, and southwestern 

Ohio unconformably overlies the Olentangy Shale. The 

Ohio Shale crops out beneath glacial sediments in central and western Ohio, and the Ohio Shale is conformably overlain by the Bedford Shale in southwestern 

Ohio. The Ohio Shale is a grayish-black, fissile shale 

that contains some gray argillaceous layers, thin sheets 

of micaceous sandstone, and pyrite (Hoover, 1960). The 

Ohio Shale and its equivalents constitute a carbon-rich 

or petroliferous shale sequence that has produced moderate quantities of natural gas (Janssens and de Witt, 

1976). The Ohio Shale in central, western, and southwestern Ohio is equivalent to the Antrim Shale in northwestern Ohio and northern and northwestern Indiana, 

north of the Findlay and Kankakee Arches (Shaver, 

1985).

DEVONIAN AND MISSISSIPPIAN ROCKS

The Antrim Shale in northwestern Ohio and southeastern Michigan unconformably overlies the Traverse 

Formation and is conformably overlain by the Bedford 

Shale; it is buried by glacial sediments where it crops 

out at the bedrock surface (fig. 4) (Shaver, 1985; Hull, 

1990; Larsen, 1991). The Antrim Shale was described 

by Janssens (1970) as a black and dark-brown, fissile 

shale, of which the basal 30 ft is interbedded with minor dark-brown dolomitic layers.

North of the Kankakee Arch, in northern and northwestern Indiana, the Antrim Shale paraconformably 

overlies the Traverse Formation (Muscatatuck Group) 

and is laterally equivalent to parts of the Ellsworth 

Shale (fig. 4) (Shaver and others, 1986; Gutschick and 

Sandberg, 1991). The Antrim Shale was described by 

Lineback (1970) as a mostly brownish black shale that
B14 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

includes a greenish-gray shale in the basal section of the 

unit.

South and west of the Kankakee and Cincinnati 

Arches in southeastern, northwestern, and east-central 

Indiana, the lithologic unit equivalent to the Antrim 

Shale is the New Albany Shale (Lineback, 1970; Shaver 

and others, 1986). The New Albany Shale is a brownish-black, carbon-rich shale and a greenish-gray shale 

containing minor dolomite and dolomitic quartz sandstone layers (Lineback, 1970). The New Albany Shale 

unconformably overlies the Muscatatuck Group. Locally, 

the New Albany Shale is conformably overlain by the 

Rockford Limestone, which represents a thin Mississippian limestone interval (less than 10 ft thick); in places, 

the New Albany Shale is unconformably overlain by the 

Borden Group, a Mississippian shale and siltstone.

The Bedford Shale in southwestern Ohio conformably 

overlies the Ohio Shale and is conformably overlain by 

Mississippian sandstone that was not considered within 

the scope of this study. The Bedford Shale grades from 

a soft, clay-rich shale in the lower part of the formation 

to a siltstone containing gray, silty shale layers in the 

upper part of the formation (Hoover, 1960). North of the 

Findlay Arch in northwestern Ohio and southeastern 

Michigan, the Bedford Shale is a soft to hard siliceous 

shale (J.M. King, 1977). The Bedford Shale conformably 

overlies the Antrim Shale and is conformably overlain 

by a Mississippian sandstone that was not considered 

within the scope of this study.

North of the Kankakee Arch in northern, northwestern, and east-central Indiana, the Ellsworth Shale conformably overlies the Antrim Shale. In northern Indiana, the Ellsworth Shale is laterally equivalent to the 

Sunbury Shale and is conformably overlain by the 

Coldwater Shale (Shaver and others, 1986). The Ellsworth Shale crops out at the bedrock surface in northern Indiana, where it is covered by glacial deposits. The 

Ellsworth Shale consists of alternating beds of graygreen shale and brownish-black shale in the lower part 

and grayish-green shale in the upper part (Hasenmueller and Woodard, 1981).

MISSISSIPPIAN ROCKS

In northern Indiana, the Sunbury Shale conformably 

overlies and is laterally equivalent to the Ellsworth 

Shale (Shaver and others, 1986) (fig. 4). Hasenmueller 

and Woodard (1981) describe the Sunbury Shale as a 

brownish-black, carbonaceous shale. The Sunbury and 

Ellsworth Shales are conformably overlain by the 

Coldwater Shale (fig. 4) (Shaver and others, 1986), 

which crops out at the bedrock surface in northern Indiana, where it is deeply buried by glacial deposits 

(Johnson and Keller, 1972). Shaver and others (1986)

describe the Coldwater Shale as a gray to greenish-gray, 

silty shale that has red stringers in the lower part of the 

unit.

South and west of the Kankakee and Cincinnati 

Arches in parts of southeastern, northwestern, and central Indiana, the Borden Group conformably overlies the 

Rockford Limestone, which represents a thin Mississippian limestone interval (less than 10 ft thick); in other 

areas, the Borden Group unconformably overlies the 

New Albany Shale (fig. 4). The Borden Group is described as a dominantly gray, argillaceous siltstone and 

shale that contains some fine-grained sandstone and 

interbedded, discontinuous limestone lenses (Shaver 

and others, 1986).

GLACIAL DEPOSITS

Approximately 80 percent of the study area is covered 

by Pleistocene deposits (fig. 8); most are of Wisconsinan 

age and represent three major stages: early, middle, and 

late Wisconsinan. Advances by the late Wisconsinan 

Laurentide Ice Sheet removed evidence of earlier glaciations in most places by eroding the surficial materials and incorporating older deposits with those transported by the glacier. In many places, the ice sheets 

overrode and deposited sediments on top of older deposits (Mickelson and others, 1983). The resulting landforms are a composite of unconsolidated deposits from 

multiple glacial advances and retreats.

The composition of till in the glacial deposits depends 

on glacial-flow paths and local geology. Most of the mineral composition of a till is representative of the local 

bedrock (Strobel and Faure, 1987). Many of the till units 

in the study area are rich in clay because of the composition of the bedrock (the Devonian and Mississippian 

shales) and its low resistance to glacial erosion. In addition, the Wisconsinan glacial deposits have a till composition that is determined by the inclusion of older 

glacial and interstadial material during the final ice 

advance. The direction of flow, as determined from erosional and depositional features, indicates that ice advances during late Wisconsinan time crossed the Lake 

Erie basin and other interstadial lakes (Whillans, 1985). 

These lakes provided clay-rich lacustrine sediments that 

have been included in the upper Wisconsinan tills as 

well.

A system of buried river valleys, filled with various 

lacustrine, alluvial, and glacial deposits, is present 

throughout the Silurian and Devonian carbonate-rock 

aquifer system. These buried river valleys have been 

referred to by several different names based on location 

and origin, but in this report they are referred to as the 

"Teays-Mahomet bedrock valley system" (fig. 9). These 

valleys were formed as a result of several continental
STRATIGRAPHY B15

38°

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

Geology from Bennison (1978)

0 20 40 60 KILOMETERS

EXPLANATION 

Glacial deposits

End moraine 

Ground moraine 

Lacustrine 

Outwash 

ll Bedrock

 Extent of Wisconsin glaciation

 Maximum extent of glaciation

FIGURE 8. Generalized glacial deposits and location of Wisconsinan and maximum glacial limits in the Midwestern Basins

and Arches region.
B16 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

glaciations that took place during the Pleistocene Epoch, although evidence exists that a preglacial river 

system followed a similar course (Fullerton, 1986; 

Goldthwait, 1991). As the ice margin retreated north 

ward, sediment-laden rivers incised the bedrock of western Ohio and eastern Indiana, altering the preglacial 

valleys and later depositing valley-fill material (Gray, 

1991). The hydrologic characteristics of these buried 

valleys vary with the type of materials deposited in 

them and the depth of incision into the bedrock.

HYDROGEOLOGIC FRAMEWORK

The correlation of the hydrogeologic units was based 

primarily on the interpretation of natural-gamma logs, 

drill-core descriptions, and a small number of electric 

logs and drillers' logs. Regional subsurface nomenclature and geologic mapping in the Midwestern Basins 

and Arches region was based on the Ohio and Indiana 

State Geological Surveys' formal geologic (rock-stratigraphic) and chronologic (time-stratigraphic) units. 

These units have been defined by location, lithology, and 

biostratigraphy from well cuttings, drill cores, and outcrop locations. The description and correlation of the 

various stratigraphic units that compose the Silurian 

and Devonian carbonate-rock aquifer system in this 

area are necessary because different names are used for

38° -

Base from U.S. Geological Survey digital data, 

1:2,000.000.1972

0 40 80 MILES I r-h '

0 40 80 KILOMETERS

EXPLANATION

Modified from Goldthwait (1991)

 Trace of Teays-Mahomet bedrock valley system

Figure 9. Generalized location of the Teays-Mahomet bedrock 

valley system in the Midwestern Basins and Arches region.

similar stratigraphic units in the various States. The 

geologic nomenclature and stratigraphic relations and 

the hydrogeologic nomenclature used by the Midwestern Basins and Arches RASA project are shown in figure 4.

Geophysical logs, descriptions of drill core, and geologists' or drillers' logs for more than 1,000 sites were 

considered for use in the delineation of the hydrogeologic sections. Of these sites, 221 were selected for evaluation on the basis of their location, the quality and 

length of the geophysical log, and the availability of drill 

core or drillers logs (table 1, on p. 32). Natural-gamma 

logs were used because they exhibit distinctive patterns, 

or signatures, that correspond to geologic contacts between the aquifer units and the confining units.

The typical response of natural-gamma-ray and spontaneous-potential electric logs to different lithologies in 

the Midwestern Basins and Arches region is illustrated 

in figure 10. Natural-gamma logs are obtained by lowering an instrument and recording the resulting response at the surface from a detector that measures the 

natural radioactive properties of the rock (Keys, 1990). 

The natural-gamma log can be run on a borehole that 

has been cased or uncased, and the presence of fluid in 

the borehole is not required. The type of electric log used 

in this report was the spontaneous-potential (SP or selfpotential) curve. The electric log is obtained by lowering an electrode into an uncased, fluid-filled borehole 

and recording the resulting electrical response at the 

surface (Telford and others, 1976).

A natural-gamma log is a plot of the changes that take 

place with depth in the natural-gamma radiation emitted from the strata that are penetrated by the borehole. 

These naturally occurring emissions of gamma rays are 

products of small amounts of uranium, thorium, and 

potassium contained within the strata (Telford and others, 1976). Carbonate rock, sandstone, and unconsolidated deposits that have a low clay content all have a 

low natural-gamma-ray activity. This low activity results in a deflection to the left on a natural-gamma log 

trace, which indicates a decrease in natural-gamma 

radiation. Shale, siltstone, and unconsolidated deposits 

that have a high clay content all have a high naturalgamma activity because of the presence of small 

amounts of naturally occurring uranium, thorium, and 

potassium in the clay. These radioactive elements are 

concentrated by way of ion exchange and adsorption by 

the clay minerals. This concentration of naturalgamma-ray emitters results in a deflection to the right 

on a natural-gamma-log trace, which indicates an increase of natural-gamma radiation.

The spontaneous-potential curve is a plot of small 

changes in voltage that vary with depth between the 

fluid in the borehole and the strata penetrated by the
HYDROGEOLOGIC FRAMEWORK B17

SPONTANEOUS GAMMA-RAY

POETENTIAL LOG

- Millivolts + Radiation increases

LITHOLOGY

i o

 200

 400

600

 800

 1,000

 1,100

Glacial deposits

Devonian shale

Devonian limestone 

or dolomite

Silurian limestone 

or dolomite

Ordovician shale

FIGURE 10. Graph showing generalized responses of natural

gamma-ray and spontaneous-potential electric logs to rock units

in the Midwestern Basins and Arches region.

borehole, measured in ohms (Keys, 1990). These naturally occurring, spontaneous potentials are caused by 

electrochemical reactions between the fluid in the borehole and the surrounding strata (Telford and others, 

1976). In general, carbonate, sandstone, and unconsolidated deposits that have a low clay content are more 

resistant to the flow of an electrical current and cause 

a negative deflection of the spontaneous potential to the 

left. Shale, siltstone, and unconsolidated deposits that 

have a high clay content are less resistant to the flow 

of an electrical current and cause a positive deflection 

to the right. Where water in the borehole is more saline 

than water in the formation, the deflection is reversed 

(Keys, 1990).

The composition of the strata that constitute the carbonate-rock aquifer system in the Midwestern Basins 

and Arches region makes the use of electric and natural-gamma logs ideal for lithologic correlation. The use 

of the geophysical logs combined with the drill cores, 

drill-hole sample cuttings, and drillers' logs allow for a 

reasonable amount of certainty when making correlations across such a large area. Detailed information 

about borehole geophysics can be found in Telford and 

others (1976); information on the application of borehole

geophysics to a water-resources investigation can be 

found in Keys (1990).

GLACIAL DEPOSITS

The thickness of the glacial deposits in the Midwestern Basins and Arches region ranges from 100 ft near 

the limit of glaciation to more than 400 ft in northeastern Indiana and along the course of the ancient TeaysMahomet bedrock valley system (figs. 11 and 9). In 

northwestern Ohio, the glacial deposits generally are 

less than 100 ft thick, except for the northwesternmost 

part of the State where thicknesses increase to more 

than 300 ft. The increase in the thickness of the glacial 

deposits in this part of Ohio is due to the area's 

interlobate position during the Wisconsinan glaciation 

(Soller, 1986). In central Ohio near the eastern limit of 

glaciation, the glacial deposits thicken to approximately 

200 ft and then abruptly thin near the limit of glaciation. Soller (1986) describes this increase in thickness 

east of Columbus, Ohio, to be a result of the concentration of glacial materials between a glacial lobe and bedrock uplands (fig. 8).

Glacial deposits range from 200 to more than 400 ft 

thick in northeastern Indiana, north of the Eel River. 

The northeastern part of Indiana was between two glacial lobes and was covered by large quantities of glacial 

materials (Wayne, 1956). In northeastern Indiana, the 

glacial deposits range in thickness from less than 100 

ft to more than 300 ft; the increases in thickness of the 

glacial deposits were controlled by the location and 

depth of preglacial bedrock valleys (Wayne, 1956). In 

central Indiana, south of the Iroquois, Wabash, and Eel 

Rivers, the thickness of the glacial deposits ranges from 

less than 100 ft to more than 400 ft. Generally, the thickness of the glacial deposits is less than 200 ft, except 

where the ancient Teays-Mahomet bedrock valley system (fig. 9) deeply incised the bedrock and controlled the 

thickness of the glacial deposits.

The major feature that affects the thickness of the 

glacial deposits in the Midwestern Basins and Arches 

region is the ancient Teays-Mahomet bedrock valley 

system (fig. 9). The system entered the study area from 

near the confluence of the Scioto River and the Ohio 

River, then trended northward from the Ohio River, 

flowed northwestward just south of Columbus, Ohio, 

toward Indiana, and crossed the Ohio-Indiana State 

line in an east-west orientation (Goldthwait, 1991). The 

ancient Teays-Mahomet bedrock valley system flowed 

westward across Indiana in a sinuous channel and left 

the study area, crossing the Indiana-Illinois State line 

from the west-central part of Indiana (Burns and others, 1985a, b, c; Bleuer, 1991; Gray, 1991).
B18 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

Hydrologic data for the glacial deposits in the Midwestern Basins and Arches region have been compiled 

by Joseph and Eberts (1994). Transmissivities reported 

for the glacial deposits, as determined from aquifer

tests, range from 1.5 to 69,700 ft2/d; storage coefficients 

range from 0.00002 to 0.2 (Joseph and Eberts, 1994). 

Where the upper confining unit has been eroded, the 

overlying glacial sediments partially confine the carbonBase from U.S. Geological Survey digital data, 

1:2,000,000,1972 l I l l 0 20 40 60 KILOMETERS

EXPLANATION 

Thickness in feet

Less than 100 feet 

100 to 200 feet

HI 2C)1 to 40° feet

H Greater than 400 feet

 Maximum extent of glaciation

FIGURE 11. Generalized thickness of glacial deposits in the Midwestern Basins and Arches region.

Geology compiled and modified from 

Gray (1983) and Seller (1986)
HYDROGEOLOGIC FRAMEWORK B19

ate-rock aquifer (S.M. Eberts, U.S. Geological Survey, 

written commun., 1992).

BEDROCK AQUIFER AND CONFINING UNITS

Data used to compute the thickness and altitude of the 

top of the carbonate-rock aquifer and the confining units 

were obtained primarily from the Indiana and the Ohio 

Geological Surveys in the form of geophysical logs and 

drillers logs. Supplemental information on the thickness 

and altitude of the carbonate-rock aquifer and the confining units was obtained from the Petroleum Information Corporation's data base, and deep-test-well data 

were obtained from the USGS's Ground-Water Site Inventory (GWSI) data base.

UPPER CONFINING UNIT

In Ohio and Indiana, the upper confining unit has 

been subjected to several extensive periods of erosion. 

This erosion has resulted in the removal of the upper 

confining unit in the central part of the study area. The 

only exception is the Bellefontaine outlier, which is 

approximately 50 mi northwest of Columbus, Ohio 

(fig. 5).

In Ohio and northern Indiana, the upper confining 

unit increases in thickness from the contact between the 

Devonian carbonate rocks and the updip edge of the 

Devonian shales as it is followed downdip into the Appalachian and Michigan Basins (figs. 2 and 5). The 

approximate thickness of the upper confining unit 

ranges from zero at the contact with the Devonian carbonate rocks to more than 1,000 ft on the western flank 

of the Appalachian Basin and the southern flank of the 

Michigan Basin (Casey, in press, b). In central and 

southwestern Indiana, the upper confining unit increases in thickness from zero at the contact between 

the Devonian carbonate rocks and the updip edge of the 

Devonian shales to more than 600 ft downdip into the 

Illinois Basin; however, in southwestern Indiana, the 

upper confining unit thins to less than 400 ft because 

of its proximity to the edge of the Catskill delta, which 

was described in the section on "Devonian Rocks" 

(Kammer and others, 1983).

The upper confining unit is cut by one major fault in 

Indiana, the Mt. Carmel Fault (fig. 5). This fault is located along the eastern edge of the Illinois Basin and 

is thought to represent movement during Mississippian 

and Pennsylvanian time (Melhorn and Smith, 1959; 

Shaver and Austin, 1972). Vertical displacement on this 

fault is generally thought to be less than 200 ft; therefore, the confining unit does not appear to be completely 

offset along the Mt. Carmel Fault.

The approximate altitude and configuration of the top 

of the upper confining unit are shown in figure 6. Along 

the eastern flank of the Cincinnati and Findlay Arches, 

the slope (the change in altitude over distance) of the 

top of the upper confining unit is fairly flat (less than 

10 ft/mi) near the updip edge of the Devonian shales. 

The slope increases (to greater than 20 ft/mi) as the 

distance from the updip edge of the Devonian shales 

increases because of the effects of the erosional thinning 

of outcrops of the upper confining unit and the 

downwarping of the crust in the Appalachian Basin. A 

similar configuration is found along the Michigan and 

Illinois Basins, again because of (a) the relative position 

of the updip edge of the Devonian shales, (b) erosion, 

and (c) downwarping of the crust in the basins.

Hydrologic data for the upper confining unit of the 

carbonate-rock aquifer system are sparse, but some 

vertical and horizontal hydraulic conductivities have 

been determined from analysis of cores collected from 

the upper confining unit in Ohio. Horizontal and vertical matrix permeabilities determined for cores from two 

wells drilled into the Ohio Shale ranged from 10"5 to 

10~7 ft/d (unpublished data maintained in the files of the 

USGS, Columbus, Ohio), and are similar to those reported for shales by Heath (1983). Hydraulic conductivities in the upper confining unit are three to five orders 

of magnitude lower than the calculated hydraulic conductivities (10~2 to 5xl02 ft/d) for the Silurian and Devonian carbonate-rock aquifer (Casey, 1992). In Ohio 

and Indiana, the Devonian and Mississippian shales 

and siltstones have been described as having a very low 

effective porosity (Bailey and Imbrigiotta, 1982; Coen, 

1989). Yields of water wells completed in the shales and 

siltstones of the upper confining unit typically are low 

(less than 2 gal/min), and dry holes are common (Smith 

and Schmidt, 1953; Walker and Schmidt, 1953; Walker, 

1953; Schmidt, 1954; Hartke and others, 1980; Bailey 

and Imbrigiotta, 1982).

CARBONATE-ROCK AQUIFER

In southeastern Indiana and southwestern Ohio, the 

thickness of the Silurian and Devonian carbonate-rock 

aquifer increases from its contact with the underlying 

Ordovician shales (the updip edge of the carbonate-rock 

aquifer) downdip into the various structural basins (figs. 

12 and 2). The thickness of the carbonate-rock aquifer 

ranges from zero at its contact with the Ordovician 

shales to a maximum of nearly 2,500 ft in southeastern 

Michigan. Along the crests of the Cincinnati, Findlay, 

and Kankakee Arches, in a structurally high position, 

the aquifer units crop out and have been subjected to 

several extensive episodes of erosion. This erosion has 

resulted in the loss of entire sections of the carbonate-
B20 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

rock aquifer in the central part of the study area (fig. 

12).

In Ohio, near the edge of the Appalachian Basin along 

the eastern limit of the study area, the carbonate-rock 

aquifer ranges in thickness from about 500 ft in the 

south to nearly 1,300 ft in the north. In northern Indiana and northwestern Ohio, where the study area borders the southern edge of the Michigan Basin, the thickness of the carbonate-rock aquifer ranges from 600 ft in 

northwestern Indiana to 800 ft in northwestern Ohio 

near the Indiana-Ohio State line to nearly 2,500 ft in 

southeastern Michigan. Along the western limit of the 

data-collection area, near the northeastern edge of the 

Illinois Basin, the thickness of the carbonate-rock aquifer ranges from about 100 ft in southeastern Indiana to 

600 ft in northwestern Indiana.

In Indiana, the carbonate-rock aquifer is cut by the 

following major faults: the Royal Center, the Fortville, 

and the Mt. Carmel (fig. 12). These faults, located along 

the northeastern and eastern edge of the Illinois Basin 

(fig. 2), are thought to represent movement during Mississippian and Pennsylvanian time (Melhorn and 

Smith, 1959; Shaver and Austin, 1972). Vertical displacement along these faults is generally thought to be 

less than 200 ft. The altitude of the Silurian and Devonian carbonate-rock aquifer near the Mt. Carmel and 

Royal Center Faults was determined by Bassett and 

Hasenmueller (1979).

In Ohio, the Silurian and Devonian carbonate-rock 

aquifer is displaced by faults within the Bowling Green 

Fault Zone (fig. 12). A large number of multiple faults 

have been mapped within this fault zone (VanWagner, 

1988), which extends north from northwestern Ohio 

along the western edge of the Appalachian Basin into 

southeastern Michigan. Movement along this feature 

may have taken place during early Paleozoic time but 

could have happened as recently as Mesozoic or possibly Cenozoic time (Onasch and Kahle, 1991). Vertical 

displacement along the Bowling Green Fault Zone 

ranges from 90 to 300 ft (VanWagner, 1988).

The effects of the ancient Teays-Mahomet bedrock 

valley system (fig. 9) on the thickness of the carbonaterock aquifer are evident in the map in figure 13. The 

Ordovician shales of the basal confining unit crop out 

beneath the unconsolidated sediments within the buried valley in areas where glaciofluvial erosion has cut 

down through the carbonate-rock aquifer.

The altitude and configuration of the top of the carbonate-rock aquifer are shown in figure 13. Within the 

subcrop area of the Silurian and Devonian carbonate 

rocks, the top of the aquifer is the bedrock surface. A 

broad area of low relief is depicted on the top of the 

carbonate-rock aquifer along the southern edge of the 

Michigan Basin. Where the aquifer units dip beneath

overlying strata into the Michigan Basin, the slope of 

this surface is noticeably less steep (approximately 10 

ft/mi) than it is where the aquifer units dip into the 

Illinois Basin (approximately 15 ft/mi) and the Appalachian Basin (approximately 20 ft/mi).

The permeability of a carbonate rock is the result both 

of primary openings that form when the carbonate sediment is deposited or precipitated and of secondary openings that form after the sediment has been lithified. The 

carbonate rocks that form the Silurian and Devonian 

carbonate-rock aquifer have been affected by many processes that control the ability of the various geologic 

units to transmit water. These processes include cementation, recrystallization, micritization, solution, dolomitization, uplifting, faulting, unloading, and weathering (Brahana and others, 1988). Many of these processes 

can either increase or decrease the ability of carbonate 

rocks to transmit water.

In the Silurian and Devonian carbonate-rock aquifer, 

certain facies have a porous and vuggy texture (noted 

in the section "Stratigraphy"). This texture can be the 

result of various diagenetic processes that can increase 

the porosity and permeability of the carbonate-rock 

aquifer in the facies affected. Throughout the carbonate-rock aquifer, rocks that have this porous and vuggy 

texture can be laterally equivalent to dense rocks that 

do not have this texture. These relations are present 

throughout the carbonate-rock aquifer. At a regional 

scale, the areas of diagenetically controlled increases or 

decreases in permeability are not mappable.

Data from 10 wells within the study area were examined in order to determine the variation in the matrix 

porosity and permeability in the carbonate-rock aquifer 

(figs. 1 and. The data were analyzed by using several 

nonparametric statistical methods (Casey, 1994a, b). 

The porosity and permeability data were tested by various groupings, and in all but one case, the groups of data 

had identical distributions, except where the data were 

grouped by composition (limestone or dolomite). In a 

regional study, like the RASA Program, the mapping of 

the compositional variation of the carbonate-rock aquifer is impractical because of the large study area, the 

variation of the composition of the carbonate rocks that 

compose the aquifer, and the changes in composition of 

laterally equivalent rocks over small distances (tens of 

miles). These results indicate that the matrix porosities 

and permeabilities of the Silurian and Devonian carbonate rocks are statistically similar and that variation 

between the groups is small. Only the compositional 

grouping can be used to define a difference in matrix 

porosity and permeability of the carbonate-rock aquifer 

(Casey, 1994a, b).

The flow and storage of ground water within the carbonate-rock aquifer are primarily within those zones of
HYDROGEOLOGIC FRAMEWORK B21

38°

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

20 40 60 MILES Lines of equal thickness of the Silurian and Devonian carbonate-rock

| | ! 1 [-1 ' aquifer from Casey (in press)

0 20 40 60 KILOMETERS Geology compiled and modified from Bownocker (1920), Burger and 

others (1971), Gray (1972b), Gray and others (1972), Gray and others 

(1979), Grey and others (1987), Willman and others (19E7), Milstein (1987) 

Data on location and extent of faults compiled from Bassett and 

Hasenmueller (1979), VanWagner (1988)

EXPLANATION

-1.000-1

-1,100-

-1,200-

-1,300-

Approximate thickness of the

Silurian and Devonian carbonaterock aquifer Lines of equal thickness 

dashed where infered. Interval 100 feet. 

Darker colors indicate greater thickness

Subcrop of Silurian and Devonian carbonate rocks

Subcrop of Ordovician shales

Limit of the principal hydrologic investigation area

 Location of the Bowling Green fault zone

Fault Hachures on downthrown side

Figure 12. Approximate thickness and extent of the Silurian and Devonian carbonate-rock aquifer in the Midwestern Basins

and Arches region.
B22 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

rock that contain openings along joints, fractures, and 

bedding planes (secondary permeability). Some of these 

openings have been enlarged by dissolution as the

ground water flowed through them. The magnitude and 

degree of interconnection among these openings determine the ability of the rock to transmit and yield wa-

- \

I KENTUCKY

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

f 1200- - 

 1,000 

- 600 

- 400 

- 200 

0 20 40

EXPLANATION

60 MILES Altitude of top of the Silurian and Devonian carbonate-rock aquifer

-pJ ' from Casey (in press)

60 KILOMETERS Geology compiled and modified from Bownocker (1920), Burger and 

others (1971), Gray (1972b), Gray and others (1972), Gray and others 

(1979), Grey and others (1987), Willman and others (1967), Milstein (1987) 

Data on location and extent of faults compiled from Bassett and 

Masenmueller (1979), VanWagner (1988)

SEA LEVEL__ o _ Approximate altitude of the top of the

 200 

 $00 

 600 

 800 

 7,000 

 7,200 

7- 1.400-- 

f -7,600- -

^^^H

Silurian and Devonian carbonaterock aquifer Contour interval 200 feet 

Dashed where inferred. Datum is sea level. 

Darker greens indicate greater elevation 

above sea level; darker blues indicate 

greater depth below sea level

:---. -. ' | Subcrop of Silurian and Devonian carbonate rocks 

§§;:;:] Subcrop of Ordovician shales

 Location of the Bowling Green fault zone

 i r Fault Hachures on downthrown side

FIGURE 13. Approximate altitude of the top of the Silurian and Devonian carbonate-rock aquifer in the Midwestern Basins

and Arches region.
HYDROGEOLOGIC FRAMEWORK B23

ter. The matrix of the carbonate rocks also contains 

water that contributes to the ground-water flow system 

(primary and secondary permeability), but this water 

is assumed to be insignificant when compared to the 

quantity of water that moves through the joints, fractures, and bedding planes (L.D. Arihood, USGS, written commun., 1992). Results of a series of aquifer tests 

in northwestern Indiana showed that "almost all of the 

transmissivity is derived from horizontal fracturing; 

however, only a few fractures present in the carbonate

are transmissive" (L.D. Arihood, USGS, written 

commun., 1992). Transmissivities determined from 

aquifer tests in northwestern Indiana ranged from 300 

to 27,000 ft2/d.

The upper zone is the most highly fractured zone of 

the Silurian and Devonian carbonate-rock aquifer (the 

strata at or near the bedrock surface regardless of the 

lithologic unit), as compared to the more deeply buried 

zones, and generally contains the greatest number of 

fractures and solution-enlarged openings. This preva38° -,

Base from U.S. Geological Survey digital data. 

1:2,000,000,1972 i ^ r 

20 40 60 KILOMETERS

EXPLANATION

Geology compiled and modified from Bownocker 

(1920), Burger and others (1971), Gray (1972b), 

Gray and others (1972), Gray and others (1979), 

Grey and others (1987), Willman and others (1967), 

Milstein(1987)

Subcrop of the Silurian and Devonian carbonate-rock aquifer 

SDH-363. Weii location

FIGURE 14. Location of wells used to determine matrix permeability and porosity in the Midwestern Basins

and Arches region.
B24 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

lence of fractures and solution-enlarged openings is a 

result of the weathering of the bedrock, unloading, and 

dissolution of the carbonate rock by ground-water flow. 

At depths greater than 250 to 300 ft below the land 

surface, however, these fractures generally are not 

thought to be capable of transmitting water because the 

weight of the overlying strata limits the fracturing related to unloading, and the secondary mineralization of 

the fractures limits the size of the openings between the 

fracture walls. The Great Lakes region has been glaciated several times, and some investigators (Beaumont 

and others, 1988) have postulated that a thick sequence 

of sedimentary rock was deposited on top of the carbonate-rock aquifer and has since been removed from the 

study area. The removal of the overlying strata, coupled 

with the multiple glacial advances and retreats, allowed 

the joints related to unloading to form preferentially at 

preexisting points of weakness in the Silurian and Devonian carbonate rocks (Kappel and Tepper, 1993).

Some zones below the upper fractured zone within the 

carbonate-rock aquifer have an increased transmissive 

capability compared to the rest of the carbonate-rock 

aquifer. The "Newburg Zone," which is a term used by 

the oil and gas industry in eastern Ohio for one of these 

zones, was documented by Norris and Fidler (1971). 

This zone is in the carbonate strata overlying the 

Lockport Dolomite in the lower part of the Salina Group 

(Norris and Fidler, 1971). The Newburg Zone is not 

contiguous within the study area, and other permeable 

zones have been noted in a broader titratigraphic section than that described by Norris and Fidler (1971). 

These zones of increased tranmissive capability can be 

associated with local unconformities that have been 

texturally described as near-reef and bank-type deposits. Strobel and Bugliosi (1991) proposed that the 

Newburg Zone could be the result of multiple, diachronous processes. Because of the lack of evidence that 

this zone is laterally extensive, it is probably not regionally important as a water-bearing zone, but it could be 

significant locally.

The carbonate rocks at and above a regionally extensive erosional surface (the Silurian-Devonian unconformity) can yield continuously large quantities of water from seeps within quarries and outcrops (Shaver, 

1989). This feature has been eroded in the central part 

of the study area where even older rocks crop out; however, the unconformity and a zone above the unconformity appear to be a less resistant path for groundwater flow than zones either above or below it. A clastic-rich zone that is contained within the lower part of 

the Middle Devonian Detroit River Formation, directly 

above the unconformity (described in the section 

"Stratigraphy"), transmits ground water effectively. The 

underlying Silurian rock is a massive carbonate rock,

whereas the rock within the clastic-rich zone is finegrained sandstone and sandy dolomite that are overlain 

by alternating units of argillaceous to pure bioclastic, 

vuggy, nonfossiliferous dolomite (Shaver, 1989). Additionally, surficial iron staining of carbonate rock below 

this zone indicates that water moves preferentially 

within this zone as a result of the change in hydrologic 

character between the overlying Devonian carbonate 

rock and the underlying Silurian carbonate rock. This 

staining results from the flow of ground water out of the 

more transmissive zone and down the quarry face below.

Faulting of carbonate rocks can affect ground-water 

flow in various ways. It can increase an aquifer's ability to transmit water along the fractures. This increased 

ground-water flow aids the dissolution of the carbonate 

rock and consequently enlarges the original fractures. 

Faulting also can restrict ground-water flow where a 

relatively impermeable unit is displaced along the fault 

and comes in contact with a more permeable unit.

Of the four major faults that affect the Silurian and 

Devonian carbonate-rock aquifer, only the Bowling 

Green Fault Zone has been studied with respect to its 

hydrologic effects. Van Wagner (1988) described the 

variation of specific capacity (which was termed "transmissivity factor") across sections of the fault zone. He 

noted that the largest specific capacities were found 

along fracture trends but that a number of unproductive wells were located within several hundred feet of 

wells that had large specific capacities. This example 

demonstrates that hydrologic characteristics can differ 

widely over short distances within a feature such as the 

Bowling Green Fault Zone.

Transmissivities for the carbonate-rock aquifer, determined from aquifer tests, ranged from 70 to 28,000 

ft2/d, and storage coefficients ranged from 0.00001 to 

0.01 (Joseph and Eberts, 1994). These transmissivities 

are three to five orders of magnitude greater than those 

reported for the Ordovician shales of the basal confining unit of the carbonate-rock aquifer and for the Upper Devonian and Lower Mississippian shales and siltstones that compose the upper confining unit of the 

aquifer system (Droste and Vitaliano, 1976).

BASAL CONFINING UNIT

The Maquoketa Group thickens eastward from the 

western border of Indiana toward Ohio. It ranges in 

thickness from about 200 ft in northwestern Indiana to 

nearly 900 ft at the Ohio-Indiana State line. The undifferentiated Cincinnatian rocks in Ohio gradually 

thicken as they dip into the Appalachian Basin. These 

units thin where they crop out in southeastern Indiana 

and southwestern Ohio because of the pre-Silurian ero-
HYDROGEOLOGIC FRAMEWORK B25

sion of the group and the post-Permian uplift and subsequent erosion along the crest of the Cincinnati Arch 

(fig. 15).

In Indiana, the basal confining unit of the carbonaterock aquifer is cut by the Royal Center, Fortville, and

Mount Carmel Faults (fig. 15). These faults, which are 

located along the northeastern and eastern edge of the 

Illinois Basin, are thought to represent movement during Mississippian and Pennsylvanian time (Melhorn 

and Smith, 1959; Shaver and Austin, 1972). Vertical

>icago

Base from U.S. Geological Survey digital data 

1:2,000,000,1972

0 20 40 60 KILOMETERS

60 MILES Linesof equal thickness of the basal confining unit from Casey (in press) 

Geology compiled and modified from Bownocker (1920), Burger and 

others (1971), Gray (1972b), Gray and others (1972), Gray and others 

(1979), Grey and others (1987), Willman and others (1967), Milstein (1987) 

Data on location and extent of faults compiled from Bassett and 

EXPLANATION Hasenmueller (1979), VanWagner (1988)

- 200 

- 400 

- BOO 

- BOO 

-1,000 

-1,200 -

-7,400-g

Approximate thickness of the 

basal confining unit Lines of 

equal thickness dashed where infered. 

Interval 200 feet. Darker colors indicate 

greater thickness

[5fl Subcrop of Silurian and Devonian carbonate rocks

[g>>x| Subcrop of Ordovician shales

 Location of the Bowling Green fault zone

i i r Fault Hachures on downthrown side

FIGURE 15. Approximate thickness and extent of the basal confining unit of the Silurian and Devonian carbonate-rock aquifer system

in the Midwestern Basins and Arches region.
B26 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

displacement on these faults is less than 200 ft; therefore, the basal confining unit does not appear to be completely offset along any of the faults.

In Ohio, the basal confining unit is displaced by faults 

within the Bowling Green Fault Zone, where a large 

number of multiple faults have been mapped (VanWagner, 1988). Movement along this feature may have taken 

place during early Paleozoic time but could have happened as recently as Mesozoic or even Cenozoic time 

(Onasch and Kahle, 1991). Because the vertical displacement along the Bowling Green Fault Zone ranges 

from 90 to 300 ft (VanWagner, 1988), the basal confining unit is not completely offset (pi. 2).

The altitude and configuration of the top of the basal 

confining unit are shown in figure 16. The altitude 

ranges from 1,000 ft above sea level in the south-central part of the study area to less than -1,600 ft below 

sea level in the structural basins. Along the eastern 

flank of the Cincinnati and Findlay Arches, the slope of 

the top of the basal confining unit is fairly flat near the 

crests of the arches (less than 10 ft/mi); however, the 

slope increases as the distance from the crests increases 

(approximately 40 ft/mi) because of the effects of 

downwarping of the crust in the Appalachian Basin. A 

similar configuration is found along the Michigan and 

Illinois Basins, again because of the relative positions 

of the crests of the arches and downwarping of the crust 

in the basins.

Hydrologic data for the Upper Ordovician rocks are 

scanty, but some vertical and horizontal hydraulic conductivities have been determined from analysis of core 

collected from the upper sections of the undifferentiated 

Cincinnatian rocks in southwestern Ohio. Vertical and 

horizontal hydraulic conductivities ranged from lO^5 to 

10~7 ft/d (Lawrence Wickstrom, Ohio Geological Survey, 

written commun., 1991). Comparisons of the hydraulic 

conductivities calculated for the carbonate-rock aquifer 

indicate that the hydraulic conductivities measured in 

the basal confining unit are three to five orders of magnitude lower than the calculated hydraulic conductivities for the carbonate-rock aquifer. Data from an inventory of drillers' logs in southwestern Ohio and southeastern Indiana indicate that far fewer wells are completed 

in the Ordovician bedrock than in the overlying Silurian 

carbonate bedrock. Wells that are completed in the 

Ordovician bedrock typically have small yields (less 

than 2 gal/min) or are dry.

The low hydraulic conductivity of the Ordovician shale 

units makes them favorable repositories for underground storage of liquefied natural gas. A room-andpillar storage facility constructed in south-central Indiana in the Maquoketa Group was found to be impermeable (Droste and Vitaliano, 1976). Additional evidence 

of the low hydraulic conductivity of the Ordovician shale

units is provided by the fact that the shale units have 

functioned as a barrier to the migration of oil and gas 

reserves and the associated highly concentrated brines 

within the Trenton Limestone. This stratigraphic trap 

is created by the low permeability of the Ordovician 

shale units that were upwarped during the post-Ordovician uplift that formed the Cincinnati Arch (Keller and 

Abdulkareem, 1980).

SUMMARY

The Silurian and Devonian carbonate-rock aquifer 

system of the Midwestern Basins and Arches region 

consists primarily of dolomite and limestone plus subordinate amounts of terrigenous clastic rocks and 

evaporites. The carbonate-rock aquifer is underlain by 

the Maquoketa Group and undifferentiated Cincinnatian rocks, which constitute the basal confining unit 

and are virtually impermeable and regionally extensive. 

These units collectively form a barrier to ground-water 

flow across the Ordovician-Silurian boundary, and this 

effectively limits the transfer of significant quantities 

of water through the base of the Silurian and Devonian 

carbonate-rock aquifer. The carbonate-rock aquifer is 

overlain by an upper confining unit on the margins of 

the study area that consists of Upper Devonian and 

Lower Mississippian shales and siltstones that are virtually impermeable; therefore, these units, where 

present, collectively form a barrier to ground-water flow 

that effectively limits the transfer of significant quantities of water to and from the underlying carbonaterock aquifer. Where the upper confining unit is absent, 

the carbonate-rock aquifer is confined by the moderately 

permeable, overlying glacial sediments.

The locations of the primary water-bearing zones in 

the Silurian and Devonian carbonate-rock aquifer are 

related to the degree of fracturing and dissolution, depth 

below land surface, and lithologic variation within the 

aquifer. At shallow depths (less than 300 ft below land 

surface), the upper part of the aquifer contains the most 

fractures and generally has the greatest number of solution-enlarged openings. Clastic-rich dolomite at and 

directly above the unconformable contact between the 

Silurian and Devonian carbonate rocks forms a regional 

water-bearing zone. Other locally significant waterbearing zones are found in the carbonate-rock aquifer. 

These water-bearing zones have been associated with 

local unconformities that have been described as being 

near-reef and bank-type deposits. An example of this 

type of water-bearing zone is the Newburg Zone.

The thickness of the Silurian and Devonian carbonate-rock aquifer ranges from zero at its contact with the 

underlying Ordovician shales (the updip edge of the 

aquifer) to a maximum of nearly 2,500 ft in southeast-
SUMMARY B27

38° ->.

Base from U.S. Geological Survey digital data, 

1:2,000,000,1972

 600 

 400 

 200 

 0 SEA LEVEL 200 

20

0 20 40 60 KILOMETERS

EXPLANATION

60 MILES Altitude of top of the basal confining unit from Casey (in press) 

 ' Geology compiled and modified from Bownocker(1920), Burger and 

others (1971), Gray (1972b), Gray and others (1972), Gray and others 

(1979), Grey and others (1987), Willman and others (1967), Milstein (1987) 

Data on location and extent of faults compiled from Bassettand 

Hasenmueller (1979), VanWagner (1988)

 too Approximate altitude of the top of the 600 basal confining unit Contour interval 

200 feet. Dashed where inferred. Datum 

is sea level. Darker greens indicate greater 

elevation above sea level; darker blues 

indicate greater depth below sea level

SF1 Subcrop of Silurian and Devonian carbonate rocks

BS§] Subcrop of Ordovician shales

 Location of the Bowling Green fault zone

T r Fault Hachures on downthrown side

FIGURE 16. Approximate altitude of the top of the basal confining unit of the Silurian and Devonian carbonate-rock aquifer system

in the Midwestern Basins and Arches region.
B28 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

ern Michigan. Along the crests of the various arches (the 

Cincinnati, Findlay, and Kankakee Arches), in a structurally high position, the aquifer units crop out and 

have been subjected to several extensive episodes of 

erosion. This erosion has resulted in the loss of entire 

sections of the carbonate-rock aquifer in the central part 

of the study area.

The carbonate-rock aquifer has been completely 

eroded in places by the ancient Teays-Mahomet bedrock 

valley system. The downcutting of this valley system 

has caused the basal confining unit to crop out beneath 

the unconsolidated sediments that today fill the buried 

valley. The downcutting also has thinned the aquifer 

along the course of the ancient Teays-Mahomet bedrock 

valley system.

The Silurian and Devonian carbonate-rock aquifer is 

overlain and confined on the margins of the study area 

by Upper Devonian and Lower Mississippian shales and 

siltstones where the aquifer units dip into the various 

basins (Appalachian, Michigan, and Illinois Basins) 

surrounding the study area. Elsewhere, the carbonaterock aquifer is overlain and confined by moderately 

permeable, unconsolidated glacial deposits.

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J.A., eds., Field trips in midwestern geology: Bloomington, Ind., 

Indiana Geological Survey, v. 1, p. 37-71.

Kappel, W.M., and Tepper, D.H., 1993, An overview of the recent U.S. 

Geological Survey study of the hydrogeology of the Niagara Falls 

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of the Canadian National Chapter, International Association of 

Hydrologists: Hamilton, Ontario, May 11-13,1992, Proceedings, 

p. 609-622.

Keller, S.J., and Abdulkareem, T.F., 1980, Post-Knox unconformity 

Significance at Unionport gas-storage project and relationships 

to petroleum exploration in Indiana: Indiana Department of 

Natural Resources, Geological Survey Occasional Paper 31, 

19 p.

Keys, W.S., 1990, Borehole geophysics applied to ground-water 

investigations: U.S. Geological Survey Techniques of WaterResource Investigations, book 2, chap. E2, 149 p.

King, J.M., 1977, Ground water resources of Williams County, Ohio: 

Toledo, Ohio, University of Toledo, unpublished M.S. thesis, 

114 p.

King, P.B., 1977, The evolution of North America: Princeton, N.J., 

Princeton University Press, 197 p.

LaFerriere, A.P., Hattin, D.E., Foell, C.J., and Abdulkareem, T.F., 

1986, The Ordovician-Silurian unconformity in southeastern 

Indiana: Indiana Department of Natural Resources, Geological 

Survey Occasional Paper 53, 12 p.

Larsen, G.E., 1991, Development of Silurian and Devonian lithostratigraphic nomenclature, central-western and northwestern

Ohio: Ohio Division of Geological Survey Open-File Report 91- 

1, 1 pi.

Lineback, J.A., 1970, Stratigraphy of the New Albany Shale in 

Indiana: Indiana Department of Natural Resources, Geological 

Survey Bulletin 44, 73 p.

Melhorn, W.N., and Smith, N.M., 1959, The Mt. Carmel Fault and 

related structural features in south-central Indiana: Indiana 

Geological Survey Report of Progress 16, 29 p., 1 pi.

Mesolella, K.J., Robinson, J.D., McCormick, L.M., and Ormiston, A.R., 

1974, Cyclic deposition of Silurian carbonates and evaporites in 

the Michigan Basin: American Association of Petroleum 

Geologists Bulletin, v. 58, no. 1, p. 34-62.

Mickelson, D.M., Clayton, L., Fullerton, D.S., and Borns, H.W, 1983, 

The late Wisconsin glacial record of the Laurentide Ice Sheet in 

the United States, in Wright, H.E., Jr., ed., Late-Quaternary 

environments of the United States: Minneapolis, University of 

Minnesota Press, v. 1, 407 p.

Milstein, R.L., 1987, Bedrock geology of southern Michigan: Michigan 

Department of Natural Resources, Geological Survey Division, 

scale 1:500,000.

Norris, S.E.,1979, Hydraulic properties of a limestone-dolomite 

aquifer near Marion, north-central Ohio: Ohio Division of 

Geological Survey Report of Investigations 110, 23 p.

Norris, S.E., and Fidler, R.E., 1971, Availability of ground water from 

limestone and dolomite aquifers in northwest Ohio and its 

relation to geologic structure, in Geological Survey research 1971: 

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___1973, Availability of water from limestone and dolomite aquifers 

in southwest Ohio and the relation of water quality to the 

regional flow system: Reston, Va., U.S. Geological, 46 p. 

(Available from U.S. Department of Commerce, National 

Technical Information Service, Springfield, Va., PB-222-558.)

Norris, S.E., and Spieker, A.M., 1961, Geology and hydrology of the 

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paleontology of the Sexton Creek Limestone and the Salamonie 

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29 p.

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Circular 4, 26 p.

Shaver, R.H., 1974, The Muscatatuck Group (new Middle Devonian 

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____ regional coordinator, 1985, Midwestern Basins and Arches 

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REFERENCES CITED B31

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44, 694 p.

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Geological Survey Circular 1099, 126 p.

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Applied geophysics: Cambridge, England, Cambridge University 

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Bowling Green Fault using multispectral reflectance, potential 

field, seismic, and well log data sets: Bowling Green, Ohio, 

Bowling Green State University, unpublished M.S. thesis, 

171 p.

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aquifers in southwestern Linn County and adjacent parts of 

Benton, Iowa, and Johnson Counties, Iowa: Iowa Geological 

Survey Water Supply Bulletin 15, 58 p.

Walker, A.C., 1953, The water resources of Jackson County, Ohio: Ohio 

Division of Water Information Circular 3, 20 p.

Walker, A.C., and Schmidt, J.J., 1953, The water resources of Scioto 

County, Ohio: Ohio Division of Water Information Circular 2, 

23 p.

Walker, A.C., Schmidt, J.J., Eagon, H.B., Jr., Johe, D.E., Stein, R.B., 

with a section on A study of the carbonate rock aquifers by 

Janssens, A.E., Norris, S.E., and Fidler, R.E., 1970, Ground water 

for planning in northwest Ohio: Ohio Department of Natural 

Resources, Ohio Water Plan Inventory Report 22, 63 p.

Wayne, W.J., 1956, Thickness of drift and bedrock physiography of 

Indiana north of the Wisconsin glacial boundary: Indiana 

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Progress 7, 70 p.

Westgate, L.G., 1926, Geology of Delaware County: Ohio Geological 

Survey, 4th ser., Bulletin 30, 147 p.

Whillans, lan, 1985, Glacial geology of central Ohio, field excursion 

3, in 6th Gondwana Symposium: Columbus Ohio, Ohio State 

University, Institute of Polar Studies, Miscellaneous publication 

226, 12 p.

Willman, H.B., 1973, Rock stratigraphy of the Silurian system in 

northeastern and northwestern Illinois: Illinois State Geological 

Survey Circular 479, 55 p.

Willman, H.B., Frye, J.C., Simon, J.A., Clegg, K.E., Swann, D.H., 

Atherton, Elwood, Collinson, Charles, Lineback, J.A., and 

Buschbach, T.C., 1967, Geologic map of Illinois: Illinois State 

Geological Survey, scale 1:500,000.
TABLE I. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arc

Well identifier used 

for this 

project

Al

A2

A3

A4

A5

A6

A7

A8

A9

A10

All

A12

A13

A14

Well or drill-hole designation

SDH 350

NEVAWEALING1

JAS7

BENTRACHSEL 2

517475495640

523920497175

WILLIAM MOSLEY 1

INPU-9

PUL 1

ORVILLE WHITE SDH166

L. BOWEN 1

CHARLES KENNEDY 1

CONTINENTAL OIL CO.

1

HELEN AMES 1

Site identification 1

403342087220701

404021087131801

404424087091001

404631087055001

404836087030601

405204087020001

405440086555401

405712086533101

405924086524801

410425086512601

410829086393501

411700086363501

411558086214801

412237086111101

Latitude

40° 33 '42"

40°40'21"

40° 44 '24"

40° 46 '31"

40° 48 '36"

40° 52 '04"

40°54'40"

40° 57 '12"

40° 59 '24"

41° 04 '25"

41° 08 '29"

41° 17'00"

41° 15 '58"

41°22'37"

Altitude of 

land surLongitude face (feet 

above sea 

level)

87° 22 '07"

87°13'18"

87° 09 '10"

87° 05 '50"

87° 03 '06"

87° 02 '00"

86° 55 '54"

86° 53 '31"

86° 52 '48"

86° 51 '26"

86°39'35"

86°36'35"

86° 21 '48"

86°11'11"

790

750

740

717

700

685

675

682

675

686

712

710

763

803

Depth 

logged 

(feet)

425

1,600

192

1,030

228

27

1,640

160

200

720

1,480

1,160

1,690

4,080

Typ

lo

Core

Geolog

Core

Driller, 

gist, ca

neutron

ma

Driller

Driller

Driller, 

gist

Driller

Core

Driller, 

gist, el

Driller, 

ma, neu

lateral

Driller

Driller, 

ma, ne

lateral

Driller, 

ma, ne

inducti

per, mi

eral
TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this 

project

A15

A16

Bl

B2

B3

B4

B5

B6

B7

B8

B9

BIO

Bll

Well or drill-hole designation

INEH-03

INEH-02

INLAND STEEL CO. 2

MIDWEST STEEL WD-1

PFIZER INJECT WELL 2

N.AMER. EXPL. 3

N. AMER. EXPL. 2

INLP-01

B.N. SEGHETTI 1

PUL 6

PUL503

PETERS 1

MARION GOHNN 1

Site identification

412803086033701

413629085590001

413934087254001

413746087102101

412850087000601

412133086592901

411739086575701

411747086510601

411245086434601

410636086360501

410408086361401

410336086310501

410303086155301

Latitude

41°28'03"

41°36'29"

41°39'34"

41°37'46"

41°28'50"

41°21'33"

41°17'39"

41°17'47"

41°12'45"

41°06'36"

41°04'08"

41°03'36"

41°03'03"

Altitude of 

land sur- Depth 

Longitude face (feet logged 

above sea (feet) 

level)

86°03'37"

85°59'00"

87°25'40"

87°10'21"

87°00'06"

86°59'29"

86°57'57"

86°5r06"

86°43'46"

86°36'05"

86°36'14"

86°31'05"

86° 15 '53"

870 1,750

865 1,880

596 4,380

603 4,310

774 4,530

698 224

677 211

670 1,120

712 1,520

715 163

710 238

718 1,500

763 1,510

Ty

Latera

gamm

Gamm

Gamm

per, ne

lateral

Gamm

tron, i

tion, s

Gamm

tron, i

tion, c

gamm

ma

Driller

Drille

Electr

Driller

ma, ne

lateral

Drille

Drille

Driller

ma, ne

lateral

Driller

ma, ne

fluid c
B34 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

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Well identifier used Well or drill-hole designafor this tion 

project

B26

B27

B28

B29

B30

B31

B32

B33

B34

B35

B36

B37

B38

B39

B40

B41

B42

M. & S. OLYNGER 1

GEORGE HEINLEIN 1

NORMAN & DEB LIGHT

2

INDW-6

DEL 2

WF-11

INDW-9

TERRY SHREVE 1

WF-13

ROBERT DRAGOO 1

WF-6

WF-333

RAN501

JONAS MILLS 1

JOHNCULLISON 9T13

437165672545

433415678680

Site identification

402951085300401

402633085295601

402305085262301

402146085241201

402023085204501

401641085195201

401547085193701

401419085194301

401310085182301

401220085155301

401135085111101

401015085070101

401055085073501

400930085064701

400712085045801

400408084583601

400202084542101

Latitude

40°29'51"

40°26'33"

40°23'05"

40°21'46"

40°20'23"

40°16'41"

40° 15 '47"

40°14'19"

40°13'10"

40°12'20"

40° 11'35"

40°10'15"

40°10'55"

40°09'30"

40°07'12"

40°04'08"

40°02'02"

Altitude of 

land surLongitude face (feet 

above sea 

level)

85°30'04"

85°29'56"

85°26'23"

85°24'12"

85°20'45"

85°19'52"

85°19'37"

85°19'43"

85°18'23"

85°15'53"

85°iril"

85°07'01"

85°07'35"

85°06'47"

85°04'58"

84°58'36"

84°54'21"

874

911

868

930

920

940

960

958

981

1,001

1025

1,025

1,030

1,038

1,099

1,160

1,220

Depth 

logged 

(feet)

1,260

1,520

1,760

127

206

121

102

1,280

101

1,240

139

91

58

1,370

1,570

181

217

Typ

lo

Driller, 

tric,

Driller

ma, n

caliper

ti

Driller, 

gamm

tron, l

Dri

Dri

Dri

Dri

Driller

ma, n

Dri

Driller

ma, n

Dri

Dri

Dri

Dri

Driller, 

ma, neu

dip me

Driller

Driller
B36 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

0) V* *"*

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TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this 

project

B61

B62

B63

B64

B65

Cl

C2

C3

C4

C5

C6

C7

Well or drill-hole designation

FA-126

PK-205

PK-30

PK-31

F-25

BRO 1

WILBERHIATTETAL 1

GEORGE I WHITE 1

BILL OLIVER SDH-20

SHE506

HAROLD LAUTENBACH

1

GENERAL ELEC. CO. 1

Altitude of 

landsur- Depth 

Site identification Latitude Longitude face (feet logged . 

above sea (feet) 

level)

394047083171900 39°40'47" 83°17'19"

394011083100300 39°40'11" 83°10'03"

393933083053100 39°39'33" 83°05'31"

393940082540000 39°39'40" 82°54'00"

393636082463000 39°36'36" 82°46'30"

391426086143401 39°14'26" 86°14'34"

391525086115201 39°15'25" 86°11'52"

392244086060601 39°22'44" 86°06'06"

392357086000301 39°23'57" 86°00'03"

392917085555201 39°29'17" 85°55'52"

393110085571201 39°31'10" 85°57'12"

393 1 14085444401 39°3 1 '14" 85°44'44"

897 3,540 Gamm

tron

840 98 Driller

785 3,730 Gamm

tron

820 3,270 Gamm

tron

1,090 3,770 Geolog

neutro

ma 

720 800 Driller

756 1,510 Driller

gist

785 1,890 Driller

gist

671 409 Driller

gist, el

735 150 Driller

712 1,140 Driller

ma, ne

caliper

790 1,590 Driller

ma, ne

caliper

C8 GLEN &ALTA BURTON 1 393415085400801 39°34'15'

85°40'08 856 884 Driller
B38 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

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TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this 

project

C23

C24

C25

C26

C27

C28

C29

C30

C31

C32

C33

C34

C35

C36

C37

Well or drill-hole designa- . . , . . i Site identification 

tion

D-78

D-10

D-50

MR-72

MR-77

MR-53

AU-21

AU-14

AU-46

AU-12

AU-29

AL-3

AL-48

AL-32

AL-22

401554084471500

401925084424900

402011084374700

402448084351900

402706084352400

402758084341300

403128084250500

403149084231600

403344084224600

403706084211100

403849084203200

404246084210200

404525084172100

404619084090500

404836084070100

Latitude

40° 15 '54"

40°19'25"

40°20'11"

40°24'48"

40°27'06"

40°27'58"

40°31'28"

40°31'49"

40°33'44"

40°37'06"

40°38'49"

40°42'46"

40°45'25"

40°46'19"

40°48'36"

Altitude of 

land surLongitude face (feet 

above sea 

level)

84°47'15"

84°42'49"

84°37'47"

84°35'19"

84°35'24"

84°34'13"

84°25'05"

84°23'16"

84°22'46"

84°21'11"

84°20'32"

84°21'02"

84°17'21"

84°09'05"

84°07'01"

1,040

1,060

995

931

920

900

860

860

874

835

830

825

806

825

785

Depth 

logged 

(feet)

1,800

340

137

1,200

1,220

242

240

355

1,250

228

70.6

320

1,330

72

60

Typ

lo

Driller,

ma

Driller, 

electric

ma

Driller

Driller

ma

Driller, 

ma

Driller

Driller, 

ma, cal

Gamm

Driller, 

ma

Electric

per, ga

Driller

Electric

ma

Gamm

Driller

Driller
TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this

project

C38

C39

C40

C41

C42

C43

C44

C45

C46

C47

C48

C49

C50

C51

C52

C53

Well or drill-hole designation

PU-12

PU-19

PU-15

PU-^3

HA^6

HA-27

HA-13

HA^4

HA-10

WO-11

WO-219-H11

WO-18

WO-254-PO9

WO-23 NWOH TESTSTEWART

WO-269-F20 (CONTRIES)

S-183-M18

Site identification l

405203084080300

405456084035300

405630084013900

405845083554600

405954083441500

410101083433000

410239083424800

410412083411700

410815083404700

411007083401600

411336083411200

411518083394000

411841083363900

412140083352700

412237083301800

412318083244600

Latitude

40°52'03"

40°54'56"

40°56'30"

40°58'45"

40°59'54"

41°01'01"

41°02'39"

41°04'12"

41°08'15"

41°10'07"

41°13'36"

41°15'18"

41°18'41"

41°21'40"

41°22'37"

41°23'18"

Altitude of 

land surLongitude face (feet 

above sea

84°08'03"

84°03'53"

84°01 '39"

83°55'46"

83°44'15"

83°43'30"

83°42'48"

83°41'17"

83°40'47"

83°40'16"

83°41'12"

83°39'40"

83°36'39"

83°35'27"

83°30'18"

83°24'46"

level)

770

775

755

760

795

785

765

787

750

725

705

689

677

670

685

695

Depth 

logged 

(feet)

300

161

320

1,330

100

2,050

330

84

621

300

58

2,770

46

235

82

92

Typ

l

Electri

per, ga

Electri

ma

Electri

ma

Gamm

tron

Driller

Gamm

Electric

ma

Driller

Gamm

Electri

ma

Driller

Gamm

Driller

Electri

per, ga

Driller

Driller
TABLE I. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this 

project

C54

C55

C56

C57

C58

C59

C60

C61

C62

C63

C64

Dl

D2

D3

D4

D5

Well or drill-hole designation

S-l 1 NWOH TEST-ACKERMAN

S-187-WO2

S-20

O-41

O-29

O-38

O-12

O-40

O-15

EX-10

EX-7

WILLIAM LOSEKAMP 1

363610686255

WALTER H. CLAWSON 1

INUN-1

JOHN SHEETS 1

Site identification 1

412356083212600

412539083193700

412615083185900

412745083140500

412932083143700

413057083124900

413438083092800

413509083090300

413536083083800

414953082520100

415700082500700

392212084525401

392413084501201

393024084595701

393323084565101

393448084552001

Latitude

41°23'56//

41°25'39//

41°26'15//

41°27'45//

41°29'32//

41°30'57//

41°34'38//

41°35'09'/

41°35'36//

41°49'53//

41°57'00'/

39°22'12//

39°24'13//

39°30'24//

39°33'23//

39°34'48//

Altitude of 

land surLongitude face (feet 

above sea 

level)

83°21'26"

83°19'37"

83°18'59"

83°14'05"

83°14'37//

83°12'49"

83°09'28//

83°09'03//

83°08'38"

82°52'01'/

82°50'07"

84°52'54//

84°50'12//

84°59'57//

84°56'51//

84°55'20//

650

645

640

606

602

596

575

575

575

597

591

986

930

700

920

997

Depth 

logged 

(feet)

250

100

2,780

1,710

75

1,710

300

2,290

1,720

2,350

2,600

1,800

70

704

120

2,760

Ty

l

Electri

ma,

Driller

Gamm

Driller

ma, ne

Driller

Driller

ma, ne

Calipe

tric, ga

Driller

ma, ne

Gamm

Geolo

Geolo

Driller

tion

Gamm

Driller

Driller

Driller

ma, ne
TABLE I. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this 

project

D6

D7

D8

D9

DIG

Dll

D12 

D13

D14

D15

D16

D17

D18

D19

D20

D21

D22

Well or drill-hole designation

UNI 2

HARRISON LAFUZE 1

FREDERICK TAYLOR 1

PR-39

LESLIE COOK SDH-57

418800684560

INWE-7 

D-65

D-54

INRA-4

WF-30

RAN516

D-82

RALPH MAY 1-26

MR-61

JAY504

JAY503

Site identification l

393643084571901

394016084550801

394649084514601

395257084475500

395343084494901

395403084502801

395553084485101 

395931084401000

400139084394900

400528084510401

400838084540301

401515084492301

402058084441500

402457084492801

403008084475700

403019084505301

403233084564601

Latitude

39°36'43"

39°40'16"

39°46'49"

39°52'57"

39°53'43"

39°54'03"

39°55'53" 

39°59'31"

40°01'39"

40°05'28"

40°08'38"

40°15'15"

40°20'58"

40°24'57"

40°30'08"

40°30'19"

40°33'00"

Altitude of 

land surLongitude face (feet 

above sea 

level)

84°57'19"

84°55'08"

84°51'46"

84°47'55"

84°49'49"

84°50'28"

84°48'51" 

84°40'10"

84°39'49"

84°51'04"

84°54'03"

84°49'23"

84°44'15"

84°49'28"

84°47'57"

84°50'53"

84°56'51"

945

958

1,030

1,180

1,028

1,085

1,075 

1,110

1,035

1,160

1,144

1,045

1,060

935

895

885

870

Depth 

logged 

(feet)

41

1430

3,330

220

1,080

100

121

85

49

181

160

103

1,260

1,690

182

80

159

Typ

l

Driller

Driller

Driller, 

gist

Driller

Driller, 

gist, el

Driller

Driller 

Driller

Driller

Driller

Driller

Driller

Driller

Driller

ma, ne

caliper

tion

Driller

Driller

Driller
TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this 

project

D23

D24

D25

D26

D27

D28

D29

D30

D31

D32

D33

D34

D35

D36

D37

Well or drill-hole designation

ROYCEE.WALL 1

INAD-3

BLAINE BAILEY 1

MR-74

MR-50

VW^O

VW-13

VW-23

VW-14

VW-11

ALL 36

ALL 35

BETTY LEUENBERGER

1

ALL 34

P-12

Site identification l

403354084543201

403521084505601

403805084491901

404032084410500

404147084361100

404532084373900

404626084371200

404845084384900

404915084385300

405448084424300

405543084514001

405728084514501

405751084541201

410026084522301

410234084463200

Latitude

40°33'54"

40°35'21"

40°38'05"

40°40'32"

40°41'47"

40°45'32"

40°46'26"

40°48'45"

40°49'15"

40°54'48"

40°55'43"

40°57'28"

40°57'51"

41°00'26"

41°02'34"

Altitude of 

land surLongitude face (feet 

above sea 

level)

84°54'32"

84°50'56"

84°49'19"

84°41'05"

84°36'11"

84°37'39"

84°37'12"

84°38'49"

84°38'53"

84°42'43"

84°51'40"

84°51'45"

84°54'12"

84°52'23"

84°46'32"

854

867

841

816

807

824

820

807

795

785

810

790

797

775

755

Depth 

logged 

(feet)

1,030

161

1,760

1,890

199

1,840

318

122

340

301

95

91

3,670

80

330

Ty

Drille

ma, n

Drille

Drille

gamm

per

Gamm

tron

Drille

Drille

Electr

ma

Drille

Electr

ma,

Drille

ma

Drille

Drille

Drille

ma, c

Drille

Electr

ma
B44 REGIONAL AQUIFER-SYSTEM ANALYSIS-MIDWESTERN BASINS AND ARCHES

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TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used Well or drill-hole designafor this tion 

project

E3

E4

E5

E6

E7

E8

E9

E10

Ell

E12

E13

E14

E15

MILN-10

LU-102-SY16

LU- 13-T TOLEDO AG

CENTER

LU-126 INVERNESS

G.C.NO 3 AT TOLEDO OH

LU-1 STATE OF OHIO

WO-313-RLOF2AT

ROSSFORD OH

WO-110

WO-316-LK4 BILLINGS

AT WALBRIDGE OH

WO-321-LK12 TRAVER

AT EAST LAWN OH

0^4

0^2

O-28

0^t3

Site identification 1

414402083443701

414132083423300

414007083403100

413905083385300

413704083362200

413658083332900

413608083303400

413542083282700

413455083260400

413458083210300

413121083134200

412952083085200

412935083080500

Latitude

41°44'02"

41°41'32"

41°40'07"

41°39'05"

41°37'04"

41°36'58"

41°36'08"

41°35'42"

41°34'55"

41°34'58"

41°31'2r'

41°29'52"

41°29'35"

Altitude of 

land surLongitude face (feet 

above sea

83°44'37//

83°42'33"

83°40'31"

83°38'53"

83°36'22"

83°33'29"

83°30'34"

83°28'27"

83°26'04"

83°21'03"

83° 13 '42"

83°08'52"

83°08'05"

level)

695

672

630

625

620

615

618

615

610

601

602

562

583

Depth 

logged 

(feet)

2,580

104

400

155

525

541

120

149

115

1,710

1,720

58

1,730

Ty

Driller

ma, ne

Drille

Gamm

tric, c

Drille

Electr

ma

Drille

Geolo

Drille

Drille

Driller

ma, ne

Driller

ma.

Drille

Driller

E16 S-18NWOH-TEST 412537083040100 41°25'37" 83°04'01'

ma, ne

575 340 Driller

ma, el
TABLE 1. Descriptions of wells used in construction of hydrogeologic sections of the Midwestern Basins and Arches re

Well identifier used 

for this 

project

E17

E18

E19

E20

E21

E22

E23

E24

E25

E26

Well or drill-hole designation

S-15

S-236-RL23 GRIFFAW

NRVICKERYOH

S-21

S-132-Y1 GROVES N OF

BELLEVUE OH

E-222

E-212

HU-24

HU-25

HU-23

HU-27

Site identification l Latitude

412445083025100 41°24'45"

412252082582600 41°22'52"

412134082550800 41°21'34//

412026082505000 41°20'26"

411929082434600 41°19'29"

411803082424900 41°18'03//

411230082403200 41°12'30//

411112082372300 41°11'12//

410539082345400 41°05'39"

410107082342000 41°01'07"

Altitude of 

land surLongitude face (feet 

above sea 

level)

83°02'5r

82°58'26"

82°55'08"

82°50'50"

82°43'46"

82°42'49"

82°40'32"

82°37'23"

82°34'54"

82°34'20"

580

597

640

735

715

662

752

803

963

1,035

Depth 

logged 

(feet)

2,400

62

2,690

150

3,650

58

3,220

3,460

935

3,940

_ 

Ty

' 

Gamm

tron

Driller 

Gamm

Driller 

Driller

ma, ne

Driller 

Gamm

tron

Gamm

tron 

Gamm

tron

Gamm

tron

^ite Identification refers to a unique identifier used in the U.S. Geological Survey's Ground-Water Site Inventory data base.