The Glacial Geology of Highland County, Ohio

Home , Lilley Formation, Yarmouthian (stage)

71-7552

ROSENGREEN, Theodore Ernest, 1937- THE GLACIAL GEOLOGY OF HIGHLAND COUNTY, OHIO.

The Ohio State University, Ph.D., 1970 Geology

University Microfilms, A XEROX Company, Ann Arbor, Michigan

1971

THIS DISSERTATION HAS BEEN MICROFILMED EXACTLY AS RECEIVED THE GLACIAL GEOLOGY OP

HIGHLAND COUNTY, OHIO

DISSERTATION

Presented in Partial Fulfillment of the Requirements for the Degree Doctor of Philosophy in the Graduate School of The Ohio State University

Theodore Ernest Rosengreen, B.S., M.S.

******

The Ohio State University 1970

Approved hy

Adviser Department of Geology PLEASE NOTE:

Several pages contain colored illustrations. Filmed in the best possible way.

UNIVERSITY MICROFILMS ACKNOWLEDGMENTS

I wish to express my gratitude to the Ohio Geological Survey for

financial assistance during the field investigations. Thanks are due the Department of Agronomy for use of their laboratory during analyses

of till for clay-mineral composition and calcite-dolomite content.

Additional thanks go to Richard Drees for his assistance during the

analyses, and to Dr. L. Wilding, both of that department, for techni

cal aid on the soil characteristics of the area.

Appreciation is extended to Niles McLoda of the Soil Conservation

Service, U.S. Department of Agriculture, for discussing characteristics

of the recently mapped soils of Highland County. Identification of

wood collected in the county was made by Dr. G. Burns of the Depart

ment of Botany at Ohio Wesleyan University.

I wish to express appreciation to Dr. B. Goldthwalt, Dr. A.

LaHocque, and Dr. G. Faure of The Ohio State University, Department

of Geology, for help given in the final preparation and critical read

ing of this manuscript. Additional gratitude is expressed to Dr.

Goldthwalt for his constructive suggestions given during the field

investigations. Special appreciation is extended to my wife, Rita,

for her tremendous help in typing of the manuscript and assistance in

preparing the geologic map.

ii VITA

February 19, 1937 • • • Born - Tooele, Utah

1 9 6 2 ...... B.S. Geology, University of Washington, Seattle, Washington

196 2 ...... Geologist, Bear Creek Mining., Spokane, Washington

196 3 ...... Geologist, Shannon & Wilson Inc., Soil Engineers, Seattle, Washington

1963-6^ ...... Computer System Analyst, The Boeing Co., Renton, Washington

1 9 6 5 ...... M.S. Geology, University of Washington, Seattle, Washington

1965-67 ...... Geologist, Humble Oil & Refining Co., Corpus Christi, Texas

1 9 6 7 - 6 9 ...... Teaching Assistant, Department of Geology, The Ohio State University, Columbus, Ohio

1970 ...... Research Associate, Department of Geology, The Ohio State University, Columbus, Ohio

PUBLICATIONS

"Till Stratigraphy from Columbus southwest to Highland County, Ohio" (with R, P. Goldthwalt) Field Guide-Third annual meeting North- Central Section, Geol. Soc. Amer., 2-1 to 2-17 figs.

FIELD OF STUDY

Major Field: Geology

Studies in Glacial Geology and Geomorphology. Professors Richard P. Goldthwalt and Sidney E. White

Studies in Geochemistry and Isotope Geology. Professor Gunter Faure

Studies in Agronomy. Professors Larry Wilding and George Hall lii /

TABLE OF CONTENTS

Page ACKNOVfLEDMENTS...... ii

VITA ...... iil

LIST OF TABLES ...... vii

LIST OF ILLUSTRATIONS...... vili

P l a t e ...... vlli

Figures ...... • viil

INTRODUCTION...... 1

Regional Setting ...... 1

Purpose of Investigation ...... 3

Previous Investigation ...... »•••• ...... 5

Bedrock Geology...... 5

Glacial Geology...... 3

Procedures ...... 7

Field Methods...... 7

Office and Laboratory Procedures ...... 9

PREGLACIAL SETTING ...... 12

Bedrock Geology ...... 12

Preglacial Surface ...... • 12

Preglacial Drainage ...... 17

Economic Geology ...... •• 18

Limestone and Dolomite ...... 18

iv Page Sand and G r a v e l ...... 19 METHODS AND RESULTS OF STRATIGRAPHIC CORRELATION...... 20

Stratigraphy...... 20 Surface S o i l s ...... 25 Till Soil Associations...... 25 Depth of Leaching...... 31

Loess cover...... ^5 Soil p H ...... vr

Paleosols...... ^9 Clay-Mineral A nalyses...... 51

Particle-Size Distribution...... 57

Pebble Count...... 6l

Calcite-Dolomite Analyses ...... 63 Heavy Minerals Ana l y s e s...... 66 t , Fabric Analyses ...... 69

Radiocarbon Dating...... 7^ DESCRIPTION OF GLACIAL FEATURES...... 80 Illinoian Margin...... 80 Illinolan Ground Moraine ...... 83 Late Wisconsin Moraines ...... 87 Mt. Olive Moraine...... 87 Cuba Moraine...... 91

Wilmington M o r a i n e ...... 93 0 Reesville Moraine ...... 9b

v Page ...... 96 Illinoian...... 96 Late Wisconsin...... ’...... 99

Eskers...... 102

Outwash . » ...... - 103 Illinoian...... 103

Wisconsin ...... 106

Lacustrine Sediments ...... 109 Boulder Concentrations...... 110

Directional Indicators .... 113

GLACIAL HI S T O R Y ...... Il6 Illinoian Glacial S t a g e ...... Il6 Wisconsin Glacial Stage ...... 125 Late Wisconsin Substage...... 127

APPENDIX...... 137 Section A ...... 137 Description of Significant Sections ...... 137

Section ...... 1^5 Sample Locations ...... 1^5

Section C ...... 1^8 Results of Analyses...... lW3 Procedures of Clay Mineral Analyses...... llf8

BIBLIOGRAPHY...... 159

vi LIST OF TABLES

Table Page

1 Generalized Geologic section of Highland County .... 13

2 Significant characteristics of major till soil associations ...... ■ 28

3 Soil characteristics associated with till units .... 35

k Tabulation of clay-mineral compositions ...... 5^

5 Particle-size distribution of till u n i t s ...... 58

6 Confidence levels for significance of mean differences in the partlcle-size distribution of till units . . . . 59

7 Pebble lithologles of till units and Illinoian gravel . 62

8 Tabulation of Chittick-Gasometric analyses for determina tion of calcite and dolomite weight percentages in till u n i t s ...... 65

9 Tabulation of heavy mineral analyses of till units . . 68

10 Radiocarbon age determinations...... 7^

11 Tabulation of clay-mineral analyses...... 151

12 Tabulation of mechanical analyses ••...•••••. 152

13 Tabulation pebble counts ...... 15^

Ik Tabulation Chittick-Gasometric analyses...... 156

15 Tabulation heavy mineral analyses ...... 157

vil LIST OF ILLUSTRATIONS

Plate

Plate Page 1 Map of the Glacial Geology of Highland County Ohio ...... in pocket

Figures

Figure 1 Map of Ohio showing the location of Highland County 2 2 Generalized geologic map of Highland County .... 14

3 Bedrock contour map of Highland C o u n t y ...... 16

4 Sketch of type section of Boston Ti l l ...... 22 5 Map of southwestern Ohio showing distribution of major soil associations...... 27 6 Map of Highland County showing distribution of major soil associations...... 29 7 Map of Highland County showing areas which have different thicknesses of loess cover and depth of carbonate lea c h i n g...... 32 8 Histograms showing depth of leaching in relation to frequency ...... 33 9 Graph showing a curve which represents change in rate of leaching with t i m e ...... 42 10 Diagram showing depth of leaching in relation to carbonate content ...... 43

vili Figure Page 11 Photograph of dark colored Sangamon, soil covered by Wisconsin loess * ...... k6

12 Three-component diagram showing the clay-mineral composition of till ...... 53

13 Three-component diagram contrasting clay-mineral composition of the central mid-west area ...... $6

lit Three-component diagram showing the sand-silt-clay composition of till units ...... 60

15 Three-ccmponent diagram showing the pebble lithologies of till units ...... 6k

16 Map of Highland County showing till fabrics of Late Wisconsin Darby I and Caesar t i l l s ...... 71

17 Map of Highland County showing till fabrics of Boston Till...... 72

18 Map of Highland showing till fabrics of Illinoian Danville T i l l s ...... 73

19 Map of Highland, Clinton, Warren, and Butler counties showing location of moraines and radiocarbon dates • • 7 6

20 Photograph of kame-moranic deposits in Beech Flats • . 8k

21 Photograph of Illinoian till p l a i n ...... 85

22 Photograph of the loop-moraine in Hussey R u n ...... 9°

23 Photograph of the moulin kame one mile west of New Petersburg ...... 101

2k Map of Highland County showing distribution of boulders 112

25 Map of Highland County showing location of striae, moraine crests, and a rock drumlin ...... 115

26 Map of Beech Flats area showing the position of the Illinoian ice margin during maximum advance ...... 118

27 Map of Beech Flats area showing the position of the Illinoian ice margin during a retreatal stand .... 119

lx Figure Page 28 Map of Highland County showing a retreatal position of the Illinoian ice margin ...... 121

29 Map of Highland County showing a retreatal position of the Illinoian ice m a r g i n ...... 123

30 Map of Highland County showing a retreatal position of the Illinoian ice m a r g i n ...... 126

31 Map of Highland County showing the position of Late Wisconsin ice margin during stand at the Mt. Olive moraine ...... 128

32 Map of Highland County showing the position of Late Wisconsin ice margin during stand at the Cuba m o r a i n e ...... 130

33 Map of Highland County showing the position of Late Wisconsin ice margin during stand at the Wilmington m o r a i n e ...... 131

3^ Map of Highland County showing the position of Late Wisconsin ice margin during stand at the Reesville moraine ...... 133

35 Map of Highland County showing the position of Late Wisconsin ice margin during stand at an unnamed moraine in Fayette C o u n t y ...... 13^

36 Map of Highland County showing the position of Late Wisconsin ice margin during stand at the Glendon m o r a i n e ...... 136

x INTRODUCTION

Regional Setting

Highland County is located in southwestern Ohio (figure l) and has an area of 558 square miles. The climate of the county Is humid- temperate continental and the annual precipitation of ahout ^3 Inches is well distributed throughout the year. Short periods of heat and cold are common; the highest temperature recorded is 105° and the lowest is -30° F. The average January temperature is about 31° and for

July about 7^° F. The county lies predominantly in the physiographic province of the glaciated Central Lowland, but about 15 percent of the land area is in the low Applachian Plateau province. Most of the latter is unglaciated. Geologically, Highland County is one of the most diversified areas

In Ohio. The stratigraphic range of exposed bedrock Is greater than that of any other county, with the exception of Mams County; it ranges from Upper Ordovician to Lower MLsslssippian. One of Ohio's largest limestone cave developments (in Late Silurian Peebles formation) is located at the eastern border of the county on the south wall of Rocfcy

Fork Gorge. Glacial drift from two glaciations covers nearly all the county; about a tenth of its area Is unglaciated (plate I). Late

Wisconsin drift mantles the northern third of the county.

1 2

a s h t a b u l a

WILLIAMS LUCAS

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HURON IHCDINA [SUMMIT

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[DCLAWAfit I Champaign jV pranklin I

Cl* a R k r IrAIRFICi.O| PCRRY PRCBLC uontGOHCRT

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Figure 1. Map of Ohio showing location of Highland County, Illinoian drift covers the remainder of the lowland province and abuts the hills east at the foot of the plateau area.

The highest elevation within the county is Washburn Hill in the plateau east of Marshall, 13^8 feet above sea level. The lowest point, 700 feet, is five miles to the south along Baker Fork at the southern county line. In contrast to this relief of about 650 feet, there is an extensive flat-plain in the western sector of Highland County. Here the elevation is about 1,000 feet. In the southern part of the county between these two extremes is an upland area which is thoroughly dissected by streams and topography is controlled by bedrock. The northern third of the county has rolling topography, which is controlled chiefly by glacial drift.

Purpose of Investigation

Prior to this study, the glacial geology of Highland. County had been investigated on a reconnaissance basis by several geologists.

The investigations revealed that the area had been involved in multi ple glaciations. The drift deposited during these glaciations exhib its contrasting weathering profiles (soils). Based primarily on degree of soil development, geologists have hypothesized that drift from three glaciations were deposited in Highland County, Illinoian,

Early Wisconsin, and Late Wisconsin. The occurrence of an Early Wisconsin glaciation (about $0,000 years before the present) in Ohio appears well established (Forsyth,

1961, p. 59“6l), "bub advance of the glacier south into Highland County has not heen proven. However, glacial drift of Early Wisconsin age is thought to occur in the county. Evidence for this has heen a helt of drift one to four miles wide, along the southern edge of the Wisconsin drift area, whose soil development appears intermediate between those developed in drift of Late Wisconsin and Illinoian age.

The assignment of drift to Early Wisconsin on the basis of soil devel opment (primarily the depth to which carbonates have been leached) has been strongly contested. Instead criteria such as composition, strati graphy, radiocarbon dates, and paleosols are needed to determine If drift of Early Wisconsin age is present.

In addition to the above problem, the topography of the area is greatly influenced locally by bedrock in contrast to the construction al topography in adjoining Clinton and Fayette counties. The rough bedrock surface has been a major obstacle in identifying the sequence

of criss-crossing end moraines. In Clinton County to the west they

occur as well-defined arcuate belts. The greater relief in Highland

County also affects the soil profiles developed in the drift, causing variations over short distances.

The area of Highland County was chosen as the subject of a doc toral dissertation in the anticipation that the till stratigraphy might be solved and that the moraine systems might be traced. This would then unravel the glacial history of this glaciated borderland. 5 Previous Investigation

Reports on Bedrock Geology

Early geologic investigations of the county dealt mainly with

"bedrock. Edward Orton in 1871 contributed the earliest significant

report, "The Geology of Highland County." Orton mentions the

"glacial drift" in the county, but he did not recognize the moraines

and consequently indicated the boundaries of the drift in only a

general way.

One of the greatest contributions to our knowledge of the stra

tigraphy and paleontology of Highland County was made by August

Foerste (1917)# when he revised the nomenclature of the Niagaran

series. In the years that followed Forste unraveled much of the

Silurian history in southwestern Ohio, southeastern Indiana, western

Tennessee, and Kentucky. In 1935# Forste published his most compre

hensive work on this large area which summarized the knowledge of the

Niagaran series. A major contribution to the bedrock geology was made by Richard

Bowman (195^) in his Ph.D. work entitled "Stratigraphy and Paleontology

of the Niagaran Series in Highland County, Ohio." Particular emphasis

was given in his study to the lithofacies and faunal variations within

each formation and an interpretation of these variations.

Reports on Glacial Geology

The earliest significant report available on the glacial geology

of this area Is that by Frank Leverett (1902). He wrote a monograph

dealing with the glacial formations and drainage features of the Erie and Ohio "basins. leverett's work is concerned mainly with the surficial geology; he discusses very thoroughly the surface topography, occurrence, character, and relation of the glacial features of the entire area. Leverett recognized three main glacial drift deposits

in Highland County, to which he attached ages of Illinoian, Early

Wisconsin, and Late Wisconsin. Although his work, was of great value, more detailed studies in later years have made it necessary to modify

some of Leverett's glacial boundaries and some ages assigned to gla

cial drift. By today's standards, which stress interpretation of gla

cial stratigraphy and quantitative data, Leverett's work has to be

considered reconnaissance.

In 1936 the Geological Survey of Ohio published the investigations

of James Rogers into the geology of Highland County during the summers

of 1929 and 1930. Rogers’ work encompasses both bedrock stratigraphy

(two-thirds of the lU8 page publication) and glacial geology. However,

his study contributed little more than the descriptive work of Leverett.

He did cast doubt on the position and age of Leverett's "early11

Wisconsin drift and concluded that it is "probably" of Illinoian age

(Rogers, 193^, p. ¥ 0 -

Forsyth (1961) described unique soils in a narrow belt across

Highland County between Late Wisconsin and Illinoian drift as evidence

for an "early" Wisconsin drift. She had begun county mapping for Ohio

Geological Survey but this was never finished. The existence of an

"early" Wisconsin drift belt, based on topography and soil profiles

was strongly debated during the Friendb of the Pleistocene (Midwest)

field trip in Highland County (Forsyth and Goldthwalt, 1962). 7 James Teller (196*0 mapped the glacial geology of Clinton County, and Richard Goldthwait has unpublished studies made for Ohio Division of Water in Ross County, which lies just east of Highland County.

Results of the writer's first field season, along with Pleistocene information of others were the basis of a field guide during the third annual meeting of The Geological Socity of America, North-Central Sec tion (Goldthwait and Rosengreen, 1 9 6 9 )-

Procedures

Field Methods

Most of the field work was conducted during the summers of 1968 and 1 9 6 9 . Every road in the county was examined and stops were made at nearly all road cuts. Numerous trips were made on foot to areas where adequate coverage was not possible from the road. Separate trips were made to the area during late fall and early spring of each year to make notes of boulder occurrences and to map morainal topography. The abundance of foilage and crops hinders an accurate and comprehensive survey of these features during the summer and early fall. '

Material was investigated chiefly by digging, but abundant use was made of the soil auger. Soil auger samples were collected at about

1,000 locations in the county, and notes were taken on thickness of loess cap, depth of leaching, parent material, pH of the soil, and soil profile. Depth of leaching was measured by application of dilute hydrochloric acid from a dropper-bottle on to drift material. Calcar eous drift reacts with the acid by strongly effervescing, whereas leached drift shows no observable reaction. Only well-drained sites of slight relief were measured.

Most pH determinations were made in the B1 horizon, because It yields the lowest values most consistently. A Hellige-Truog kit was used to measure pH. The procedure involves placing a pea-size sample of soil in an indentation on a ceramic plate, mixing a few drops of

Hellige-Truog solution into the sample, sprinkling a white powder

(CaSOij.) on the moistened sample, then matching the color absorbed by the powder to a color chart, and reading the corresponding pH values.

Pebble counts were taken at all significant sections and many

single till exposures. The procedure involves collecting 100 pebbles from one to three inches in diameter as they are uncovered during the

course of digging below the weathered soil zone. They were collected

from a selected exposure covering a few square yards at most. Pebbles were saved from several sampling sites until several hundred could be

identified at one time. Each stone was washed and broken with a ham mer. This gives greater uniformity of identification and assures a

clean fresh surface for consistent limestone-dolomite determinations.

Till fabric was recorded at the time of collecting pebbles by

measuring the preferred orientation of the long axis of stones not less

than one inch long. Only stones with a length-to-breadth ratio greater

than 3.2 were measured. This is the minimum practical ratio, since it

is difficult to judge the orientation of a long axis in the case of

stones that are not elongated. Only the direction of plunge of the

long axis was taken, not the amount. Care was taken to measure only

orientations from stones in compact till not affected by frost-heaving or slump. At most sites 15 to 25 orientations were measured. Young

(1969, p. 23U8 ) concluded that in till possessing a significant degree of preferred orientation, there is virtually no difference in calculat ed orientation, whether 25, 50 or 100 stones are used although strength values do vary. At a few localities only 10 stones were measured due to the very sparse occurrence of elongate pebbles.

Mapping was done on 7*5 minute topographic maps (U.S. Geological

Survey, 1960-6 1 ). Names of the quadrangles used are as follows:

Memphis, New Martinsburg, Martinsville, New Vienna, Leesburg, Green field, South Salem, Bainbridge, Rainsboro, Hillsboro, New Market,

Iynchburg, Sardinia, Sugar Tree Ridge, Belfast, Sinking Spring, Bying- ton. Plate 1 is a composite of these quadrangles reduced to half size.

Unpublished date collected for the "Soil Survey of Highland County,

Ohio," headed by Norris Williams, was used to assist in mapping of bed rock, terrace, and alluvial deposits.

Office and Laboratory Procedures

Water well logs on file with the Ohio Division of Water were check ed for information regarding thickness and character of the glacial drift. About 700 well logs were examined, of which approximately 500 had been accurately located by the Ohio Geological Survey. The well- log data were used by the survey to construct a generalized Bedrock

Contour Map. A reduced copy of this map is shown in figure 3, page 16 .

Aerial photographs were used to locate topographic patterns that could not be observed from the ground. In addition, they helped In locating terraces and obscure morainic topography in woodland tracts. 10

Particle-size distributions were determined for 52 till samples. The method used for grain-size analyses involved sieving for 10 minutes on a Ro-Tap machine all material greater than silt size (0.062mm), Hydrometer analysis was used for the silt (0.062-0.002mm) and clay size ( < 0.002mm) fractions. The procedure followed is that described in the American Society for Testing Materials (19^4, p. 95" 106). Heavy mineral analyses were made on the very fine sand grade size (0.062 to 0.125mm) for 32 till samples. Mineral separations were made using bromoform (specific gravity 2.79) and an apparatus shown in Krumbein and PettiJohn (1938, P* 335, £*5* 153)* The heavy minerals thus obtained were divided using a micro-splitter until a representa tive sample containing about 500 to 1000 grains was separated. A por tion was then mounted on a glass slide with Canada Balsam. Heavy minerals were identified uEing a petrographic microscope and 200 grains were identified on each slide. Semi-quantitative estimations of the clay minerals, were deter mined by a modified Johns, Grim, and Bradley (195^, P* 242-251) x-ray diffraction method developed by Dr. L. P. Wilding and L. R. Dress of the Ohio State University's Agronomy Department. Peak areas were utilized and appropriate relative diffraction intensity ratios applied to these peaks as determined from mixtures of standard reference clay minerals analyzed in this laboratory and from current literature. Illite was used as comparison standard. Clay minerals were identified in 18 till samples, and were classi fied as chlorite, illite, kaolin!te, montmorilIonite, and vermiculite. Quartz was also identified in the clay fraction. The criteria used to identify the above minerals and the ratios and area factors employed for the clay mineral quantitive estimations are given in the Appendix section C, along with the tabulated results.

Calcite-dolomite percentages of the less than 2mm size fraction were determined for 37 tills in Highland County. The Chittick-Gaso metric determination technique was used as described by Dreimania

(1962). PREGLACIAL SETTING

Bedrock Geology

The oldest rocks exposed in Highland County belong to the Arnheim formation (Upper Ordovician), and the youngest to the Berea formation

(Lower Mississippian). Table 1 is a generalized stratigraphic column for the Paleozoic rocks which outcrop in the county. Figure 2 is a generalized geologic map showing the distribution of the time-rock systems. Rocks belonging to the Niagaran series (Middle Silurian) have a greater areal distribution than all others combined.

Structurally these Paleozoic rocks form part of the east limb of the Cincinnati arch. The general strike of these rocks is north-north west, and dip east-northeast at 20 to 30 feet per mile (Bowman, 195^, p. l). The oldest formation is exposed only in the southwestern corner of the county along the creek bottom of Flat Run. Eastward across the county successively younger rock is exposed. The youngest bedrock forms the flat-topped mountains of the Appalachian Plateau province along the eastern border of Highland County south of Rocky Fork.

Preglacial Surface

The preglacial surface of the county may be divided into four areas on the basis of topography and well-log data. These divisions

12 13 TABLE 1 GENERALIZED STRATIGRAPHIC SECTION FOR HIGHLAND COUNTY ca 0) w h Thickness co m Formation Lithology In feet • • CJD H Berea Sandstone, buff to gray, fine-grained, 200 interbedded thin shales I j . Ohio Shale, dark brown or gray, fissile, 250-300 calcareous concretions, pryrite and marcaslte %H 0>> S3 « Olentangy Shale, blue with black partings, 0- 60 P fissile E5 e? Hillsboro Sandstone, white or yellowish, 0- 20 fine-grained, friable Tymochtee Dolomite, gray to blue-gray, very I- 0- 80 I fine-grained, argillaceous partings Greenfield Dolomite, tan to blue-gray, fine OcS grained, distinctly bedded Peebles Dolomite, light gray to bluish gray, ' 20-100 very fine-grained, vugs and cavities common, massive Lilley Dolomite, gray to bluish gray, finely 40- 55 crystalline, argillaceous locally, £ crinoidal carbonate lithofacies Bisher Dolomite, reddish-brown or buff, fine- 23- 84 grained, silty, with locally blue- gray limestone Clay Shale, bluish-green, weathers to 36- 95 light yellow Dayton Limestone, gray to greenish-gray, fine- 2- 7 grained, very dense and hard s Brassfleld Limestone, bluish-gray to pink, massive 26- 50 % to thin bedded, shale partlns Elkhorn Shale, greenish, calcareous, with 12 thin bedded limestone ^ Whitewater Shale, calcareous, with thin bedded 65 limestone m o Liberty Shale, calcareous, with thin bedded 30 5 1 limestone g 3 Wayne sville Clay Shale, calcareous, with thin bedded 50 o « limestone Arnhelm Shale, calcareous, with thin bedded 5 limestone BROWN COUNTY Figure 2. Generalized geologic map of geologicmap HighlandCounty Generalized 2.Figure BROWN □ Devonian - shale Devonian Ordovician -and shaleslimestone Ordovician -limestone and dolomite Silurian issipa sandstone - Mississipplan ONY | COUNTY <5 FAYETTE I COUNTY

ROSS COUNTY lA 15 agree in part with the distribution of the various rock series (see figure 2). One of these areas is a narrow strip along the south eastern border of the county, and it forms the edge of the Appalachian

Plateau province. The western boundary is here capped by the resis tant Berea sandstone, which overlies the Ohio shale, and forms the

Mississippian Escarpment. In Highland County, however, the escarpment is represented only by outliers such as Fort Hill, Washburn Hill, and

Long Lick Hill, which rise about 300 feet above the surrounding land.

A dissected upland area with accordant levels extends west of the Mississippian Escarpment for about two-thirds the distance across the county. The western edge of the area iB formed by the Niagaran Escarp ment where hills of the Bisher and Lilley dolomites rise about a hund* red feet above the flat area farther west. Several isolated outliers such as Calebs Hill occur as remnants of this dissected escarpment in the area of Danville and Russell. The northern extent of the dissect ed upland area is the valleys of Clear Creek and Rocfcy Fork.

An extensive flat and poorly drained area occurs west of the

Niagaran Escarpment. Although the topography is almost entirely drift controlled, data from well records show that the rock surface below is also very flat (figure 3)- The bedrock surface probably represents an I erosion surface at the base of weak Ordovician shale and limestone.

A large area, roughly trapezoidal in shape, with moderate bedrock relief, covers the northern sector of the county. The apex extends south a short distance bisecting the dissected uplands and Mississip pian Escarpment. Several broad bedrock hills stand above the general rolling surface. Silurian bedrock is the chief material underlying the 16

OOJI

Figure 3* Generalized bedrock contour map of Highland County.

Contour Interval 100 feet 17 glacial drift of this area, hut Ohio shale caps some of the prominent hills (see figure 2 ).

Preglacial Drainage

The Teays is the term used in a general sense to indicate the work of streams during that general period of erosion before glaciation

* (Stout and others, 19Uk, p. 5 1 ). The Teays, the master or at least type stream of the system, headwaters were in the Piedmont Plateau of

Virgina and North Carolina. It flowed northwestward through West

Virgina and south central Ohio. Beyond the Ohio line the drainage

system is believed to have trended westward through Indiana to the

Wabash River and then southwestward to the Mississippi valley and to the Gulf of Mexico.

Highland County was indeed a "highland" drainage-divide area be

fore glaciation. A major divide extends north-south through the western

part of the county along the Niagaran Escarpment. Drainage east of the divide flowed east and joined the master Teays. Drainage west of the divide flowed southwest and was part of the headwaters of the Norwood

River, a major tributary to the master Teays. According to Wilber

Stout and others (l9^> P* 6 8 ), the outlet of the Norwood River was

along the valley of the present Ohio River to where this old tributary

joined the master Teays River near the mouth of the present Wabash River just west of Mount Vernon, Indiana. However, work in recent

years (Durrell, 1 9 6 1 , p. 5l) indicates this drainage may have flowed

north or northwest from Hamilton from the southwest corner of Ohio to 18 join the master Teays.

During the Teays Stage major valleys developed east of the drain age divide. They were also used by streams of the Deep Stage which followed. Today, Rocky Fork, Clear Creek, Rattlesnake Creek, and Paint

Creek occupy parts of these valleys. Areas of greatest relief occur along the course of these four valleys. However, much of the erosion done by the preglacial streams is now obscured by later streams and by drift deposited during the Illinoian and Wisconsin glaciations.

Economic Geology

Limestone and Dolomite

The most valuable resources in Highland County are limestone and dolomite. They find their greatest use presently in road aggregate and to a smaller extent for agricultural amendments. In the past the

Brassfield limestone, Bisher, Lilley, and Peebles dolomites were all quarried but in recent years the Brassfield and Lilley are the only units exploited. An asphaltic phase in the Lilley formation has been quarried since the early 1 9 3 0 's as natural asphaltic aggregate which is used for road construction. It occurs in several places along the drainage divide between Willettville and Hillsboro. At present the only active production of this stone is from a quarry 1.5 miles south west of Willettville. The interested reader is referred to the work of Richard Bowman (1956) for a detailed report on the economic aspects of bedrock in Highland County. 19 Sand and Gravel

At present, sand and gravel are of secondary importance as a natural resource in Highland County. There are numerous deposits with in the area affording an ample supply, however, only one gravel pit 1b presently "being actively exploited. It is located two miles north of

New Petersburg in Wisconsin age material of Paint Township (locality

B^7). Commonly, gravel is used for road material without any addi tional sorting; however, if it is to be used for concrete aggregate screening and washing are necessary. The most important sand and gravel deposits of the county are glacial in origin. Detailed descriptions are given later under the sections on kames, eskers, and outwash, be ginning on page 9$.

Illinoian sand and gravel deposits exceed by far those attributed to the Wisconsin glaciation. Likewise, however, the cost of exploita tion is far greater than excavating the younger Wisconsin deposits.

This expense is due to two factors; cementation and thick overburden.

In nearly all large kame and esker deposits of Illinoian age, the de posits are locally cemented with calcium carbonate forming massive conglomerates three to eight feet thick. Overlying the conglomerate is overburden of 3 to 7 feet of weathered gravel. Limestone pebbles have been leached out, or if present, have a soft chalky consistency.

Where deposits of Illinoian age are poorly drained or fine-grained the overburden is 12 to 15 feet thick. Only two gravel deposits of

Illinoian age are presently being used in the county and then on a infrequent basis (localities C9^ and Dlfl). METHODS AND RESULTS OF STRATIGRAPHIC CORRELATION

The main purpose of stratigraphic correlation of glacial deposits is to determine their sequence of formation and, hence, the glacial history of the area. Identification and correlation of glacial strata is accomplished through several empirical methods, each "being of ques tionable value if used alone. The methods utilized during this study are as follows: stratigraphy, surface soils, paleosols, particle-si2e distribution, pebble lithology, calcite-dolomite content, clay-mineral

composition, till fabric, and radiocarbon dates. The results and con

clusions obtained by these methods are also presented in this section; the detailed data are listed in the appendix.

Stratigraphy

The most important aspect of stratigraphy is the establishment of

local stratigraphic sections each contributing to a segment of the

glacial history. These are then correlated to other sections by equat

ing strata on the basis of quantitative or semi-quantitative analyses.

Seldom does a problem arise as to relative age of units at any single

section. Correlation between sections, however, is very difficult, if

not impossible in glacial deposits when only the method of equating

similar sequences of materials is employed. Glacial deposits are char

acterized by repeatable sequences (i.e. till-gravel-till) of nearly 20 21 identical appearance, and two such sequence within close proximity may belong to different glaciations. Without the presence of a dis tinctive lithologic marker bed, correlation based solely on similar sequence of beds in several exposures and/or intervening well-logs is of very questionable value. Surface weathering and paleosols can be among the best methods of stratigraphic correlation. The absolute age of a deposit, however, can not be determined by consideration of stra tigraphy alone. In the following the principal exposures of till in

Highland County are described.

Two tills separated by ten feet of gravel with a paleosols five feet thick at the top, is exposed in a cut bank along Blinco Branch.

Analysis of clay-mineral composition, mechanical composition, pebble lithology, and carbonate content identify the upper till as belonging to the Late Wisconsin ice advance. The name Boston Till is here pro posed for this unit. It directly underlies the surface, or loess cap, in a belt of drift one to four miles wide along the southern margin of the Wisconsin drift in Highland County (plate i). The Boston Till is named from the village of Boston in Highland County. The type section

(figure U; location 058 in Appendix, section A) is exposed along

Blinco Branch 2.1 miles east of Boston and about J00 feet south of

U.S. Highway 50.

The Boston Till is composed primarily of calcareous till, which consists of a compact but uncemented silt loam matrix that contains fairly sparse pebbles (about 6 percent by weight) and cobbles.

Details of the composition of the till are given under appropriate sec tions in this chapter. The upper surface of the Boston Till is con- ‘DEEP RUSSELL SOlL.x

LEACHED A A BOSTON A Gilt L0AM T1LL ,0YR 5/4"5/0 A TILL SH A R P CONTACT! A A A A

PALEOSOL 3 6 -6 0 f'////"///■ LEACHED 30 - 36 A A LOAM TILL IOYR S/4-5/6 /. o ■ | . ^ <5^ j• */ • V?- \- • -V? 7i. T -Tfl ° X% * p ft o ♦ i, » *>^7 •* • ^ ^ c“ \ * >. C' ° * # * o * . • * .—* A j j k f l J ■ e"$- • ;■— a. *• a . '« A , 'o WELL SORTED, CALCAREOUS * -- t>— a O ^<— •9 " ' > ’ no RBAUFlGRAVEL nnrtond x"" ^ o < . ^ 0-.* ’ — U ^ L IOYR 5/) '~JS ■*''■■ / SAND Jfm ” S? ' ‘

A N

Blinco Branch Creek Flow

Figure If. Type section of the Boston Till ro ro 23 structional. Its southern extent is formed by the Mt. Olive moraine.

The lower till, at the type locality for the Boston Till, is iden tified as belonging to the Illinoian drift that directly underlies the surface, or loess cap, over the southern two-thirds of the county. In following common usage by Quaternary geologists for western Ohio, this till is hereafter referred to as Danville. This name has been infor mally given to Illinoian till of the area by E. P. Goldthwait (1955* p. 1*5) from the village of Danville in Highland County, where about 18 feet of the till overlying Silurian limestone was exposed in a ‘quarry.

The Danville Till is composed primarily of calcareous till, very compact, locally cemented, with a loam matrix that contains abundant pebbles (about 15 percent by weight) and cobbles. The Danville Till is significantly different from the Boston Till in composition and, hence, can be readily identified in sections containing both units.

A sequence of three tills is exposed in a cut bank in Fall Creek

(locality D36). The lower till, identified as Danville, Is separated from the middle till, which is Boston, by six feet of paleosol develop ed in sandy silt (fluvial). A one foot layer of rubble and gravel separates the Boston Till from the upper till, which is identified as

Late Wisconsin on the basis of its composition, stratigraphic position, and radiocarbon age determination. Following current terminology it is called the Caesar Till. It directly underlies the surface, or thin loess cap, south of the Reesville moraine and extends to the distal edge of the Cuba moraine. The Till is calcareous, compact, with a loam matrix, and very similar in composition to the Danville Till.

A section with two tills is exposed in a cut bank of a tributary zh to Walnut Creek, 2.2 miles east of East Monroe (locality A60). The lower unit, identified as Caesar Till, is separated from the over-lying till hy a calcareous unoxidized silt bed, two feet thick. The upper three feet of the Caesar Till are oxidized to a dark brown (10 YR V 3 ) color. The upper till, here located on the distal edge of the Rees- ville moraine, is Late Wisconsin. This unit is called the Darby I

(Goldthwait and others 1965). It forms the drift directly underlying the surface, and was deposited during the readvance of the Scioto Lobe to the Beesville moraine. The paleosol (oxidized till) at the top of the Caesar Till was developed during the time interval between retreat of the glacier from the Cuba moraine to its subsequent readvance to the

Reesville moraine.

The Derby, Caesar, and Danville tills all have similar composition and could not be identified from each other on this basis. However, elsewhere in western Ohio a significant difference in the mechanical composition of the Darby and Caesar tills has been described (Forsyth,

1965). A sequence of three tills separated by gravels is exposed in a cut bank along Clear Creek three miles north of Hillsboro (locality C5 1 ). The upper two tills are identified as Danville on the basis of composi tion and their location south of the Wisconsin boundary. The lower till differs in composition from the Danville Till and overlies a pale- sol which is four feet thick. This till represents a pre-Danville advance, whose age may be "early" Illinoian or possibly pre-Illinoian. Ho other pre-Danville till of similar composition was found elsewhere in the county. The paleosol is developed in a gravel which contains peb- 25 ties of foreign lithology, namely granitic and metamorphic rock suites. This suggests the gravel is an earlier drift deposit, possitaly Kansan. Drift of Kansan Age has taeen identified in the Cincinnati area (Teller,

1970). Exposures with stratigraphy of several units occur in a numtaer of localities in Highland County. All sections with significant stratigraphy are described in the Appendix, section A.

Surface Soils

Till Soil Associations Five different Late Wisconsin tills are recognized in western Ohio. They have taeen associated with five major soil associations (Forsyth, 1965). These soils occur in irregular east-west belts gener ally parallel to end moraines. The boundaries for these major soil associations are caused by significant changes in parent material. In most cases a significant readvance of the glacier is accompanied by a significant change in parent material. However, a major soil boundary appears to have been established in one case (without significant dif ferences in soil characteristics), because of the occurrence of an end moraine which represented a major readvance of the glacier; the bound ary separates Miami 6A-6O soils. Recent work by soil scientists has shown that there is no signif icant difference between the major soil associations of Miami 6a and Miami 60 in west-central Ohio (Wilding, Jones, and Schafer, 19&5)* The boundary separating these two soil associations is generally the 26 distal edge of the Farmersville moraine (Miami Lobe) and the Reesville moraine (Scioto Lobe) (figure 5)* Apparently no significant differ ence exists in the composition of the parent material of the 6A soils

(Darby I Till) and that of the 60 soils (Caesar Till). This conclusion is also supported by the present study in Highland County. In Ohio, soil scientists do not recognize Miami 6A and 60 areas anymore, but use the terra "Miamian" (for the well-drained sites).

Although no significant difference may exist between Miami 6A and

60 soil areas elsewhere in Ohio, in Highland County a significant dif ference occurs in the thickness of the loess cover. On this basis, the two areas can be readily separated. For this reason, the former terminology of Miami 6A and Miami 60 will be used in this dissertation.

It Ehould be remembered, however, that all other soil characteristics are similar between the two areas.

In addition to the "deep" Russell soil, three of the five major till soil associations of Late Wisconsin age occur in Highland County.

These soils are distinquished from each other on the basis of (l) the presence or absence of a silt (loess) cap, and (2 ) the depth of soil development, The characteristics of these soils are summarized in

Table 2. Those which are diagnostic for a particular soil are under lined. For comparison the Illinoian soil "Cincinnati" is included.

Figure 6 shows their general distribution in Highland County.

It has been postulated that an older, so-called "early" Wisconsin drift exists on the basis of a soil whose Intensity and depth of weathering are intermediate between those of Illinoian and Late

Wisconsin age. These soils, called "deep" Russell, are restricted in . 5ENECA. PAULDING 8e&cu Line PUTN rmrrcnCit

VAN WERT VANDOT CRAWFORD

HARDIN

MORROW

SHELBY LOGAN h DELAWAR DARKE PAIGN

MADISON RANKLIN QA CLARK MOHTOO^E PICKAWAY fayette

butler WARREN

ILTON CLERMONT

BROWN

62 - St. Clair soils 6B - Morley soils 6A - Miami 6A soils 60 - Miami 60 soils 67s- "shallow” Russell soils 67 - "deep" Russell soils 75 - Cincinnati soils

Adapted from Jane Forsyth (1 9 6 5 ) Figure Map of southwestern Ohio showing relationship between end moraines and distribution of major till Boil asso ciations. Soils are labelled by field mapping symbols. TABLE 2 CHART PRESENTING SIGNIFICANT CHARACTERISTICS OF MAJOR TILL SOIL ASSOCIATIONS IN HIGHLAND COUNTY

Soil Soil Characteristics

Mapping Thickness Depth of Clay- Clay Ratio of Name symbol of silt leaching (at content content clay in B Boundary Boundary cap well-drained of B of C clay in C to south to north site), inches horizon horizon * ..._ *

Miami 6A gen. lU-Vf 33-^0 11-27 1.8 Reesville Powell absent moraine moraine

Miami 60 < 1 8 17-58 33-to 10-27 1.8 Cuba Reesville moraine moraine

"shallow" Russell 67s > 1 8 J?-60 33-ifO 15-27 1.7 Mt. Olive Reesville moraine moraine

"deep" Russell 67 > 1 8 60-80 33-**0 15-27 1.7 Mt. Olive Cuba moraine moraine

Cincinnati 75 12-5? 6?-l^ 33-^0 15-27 1.7 Illinoian Wisconsin boundary boundary

Modified after Jane Forsyth, 1965, page 223

to 00 BROWN COUNTY BROWN Figure Figure ICNAI 75 CINCINNATI 6 COUNTY Wisconsin Glacial Boundaries Glacial Illinoian . Map of Highland County showing distribution distribution showing of HighlandCounty Map . of associations. soil of major till I FAYETTE IM 60 6 MIAMI COUNTY 29 occurrence, "being recognized only in a very narrow "belt along the

Wisconsin "boundary in Highland and western Ross counties. The

Russell soils are characterized specifically by a silt (loess) cap

greater than 18 inches thick. The "deep” Russell soil differs from

the ’’shallow” Russell soil mainly in depth of weathering, being

leached to depths greater than 60 inches. The soils of the Russell

area appear to he more weathered than the ’’Miamian” soils, having

somewhat brighter colors for sites of similar drainage.

In the Miami Lobe of western Ohio the areas dominated by "shallow”

Russell soils to the south are generally separated by & so-called

"Silt Line” (Forsyth, 19^1) from areas characterized by Miami 60 soils

to the north. The Miami 60 soils may have a silt cap, but it is less

than 18 inches thick. To the east, in the Scioto Lobe, these soils

tend to occur together as a complex. In Highland County a "Silt Line” separates areas dominated by Russell soils to the south from dominately

60 soils to the north. Although both Miami 60 soils and "shallow”

Russell soils occur on both sides of this line, "shallow” Russell soils

are much more common to the south in a complex association with "deep”

Russell soils. The "Silt Line" which separates the two areas gen

erally is the distal edge of the Cuba moraine, suggesting a signif

icantly greater amount of loess deposition prior to its construction.

The overall separation of the two complex soil associations is clearly

on the presence or absence of a thick silt cap. In the complex of

Russell soils south of the "Silt Line," it is believed that the signifi

cant differences between the "deep" and "shallow" soils are quite

■ clearly related to the combined effects of local compositional varia- 31 tlona is the Boston Till, and loess thickness.

Another "Silt lane" separates the area dominated by Miami 60 soils from dominately 6A soils to the north. In this case the distal edge of the Reesville moraine separates the two areas. The area of 6A soils is generally without a noticeable loess cover.

Depth of leaching

Surface soils have long been used by geologists as a basiB for determining the relative ages of glacial deposits. There are five factors which control the nature of any soil. These are: (l) parent materials, (2 ) time, (3 ) climate, (U) topography, and (5 ) organisms.

If topography, climate, and organisms are similar over a given area, any difference in soil development may be the result of time and parent material. If it Is possible to deduce in each case which of these Is the controlling factor, then one can utilize soils information to interpret a facet of the glacial history of the area.

The present work in Highland County has resulted in delineation . of four areas which differ from each other in average depth of leach ing (figure 7)* These four areas coincide with the areas covered by the major soil associations (figure 6 ). The areas coincide because time and parent material, In each case, sore the chief parameters which controlled their development.

A series of histograms (figure 8 ), one for each till unit, shows the distribution of depth of leaching in relation to their frequency of occurrence for sites examined in Highland County. The arithmetic mean and standard deviation for the depth of leaching associated with BROWN COUNTY I > 8 8 8 4 > * I O Figure Figure BROWN r Glacial Boundaries Glacial MILES 7 Mi- . Map of Highland County showing areas which have have which areas showing County Highland of Map . distinctly different thicknesses of loess cover cover loess of thicknesses different distinctly and depths of carbonate leaching. leaching. carbonate of depths and Late Wisconsin Late Illinoian COUNTY Area Area h Area 2 - Caesar Drift Drift Caesar - 2 Area Area Area I Drift -Darby 1 Area Area 3 - Boston Drift Drift Boston - 3 Area 13.1 Mean loess thickness loess Mean 13.1 34.3 Mean depth of leaching of depth Mean 34.3 FAYETTE k - Danville Drift -Danville J COUNTY 32 33 Boston T ill

mean 5 9 .1

Danville T ill 18 16 mean IOU.1 14 12 § 10 10 % 8 & 8 c P£m 6 6 s k k 0) 2 & 2 0 LIH 0 E n x m o in o ia O i a O ia o in o in m in in in in in in vo rooo-=r -d- in mvo vo t- oo r- co ov O rH cvj ro in lit i i i i i i i i I I I r lrH r-l »—I r-t r-l VO r-l VO HVOrlVO rl VO H VO VO VO VO i I I I I I OJ to ro in in vo vo t— t— vo t- 00 vo vo vo vo vo on 8 i—I CVJ oo j* rH rl rH H r-l Depth of leaching (inches) Caesar T ill

mean 3^*3

Darby I T ill

mean 23*3 ko 36 32 Ik >>28 12 g 2 U 10 § 20 0 o1 , c 8 B 16 1 6 ** 12 u k 8 Pm

01 i n tnoinom o in o o in o in o in o in O H cvj C\J ro ro J- in cvj cvj on o j J- m invo I i i i i i i i i i i i i i i i i O VO rl VO rl VO H V0 vo rl VO rl vo H vo rl VO rl H Ol W (OM 4 4 H c\Jcvjcoco-=f-=i- tnin

Depth of leaching (inches)

Figure 8. Histograms showing the distribution of depth of carbonate leaching in relation to frequency for t ill units in Highland County* each till unit are listed in table 3* The value for the depth of leaching includes the thickness of the leached loess cover. The important question concerning this data is the significance of dif

ferences between the means. The major concern is to determine whether the observed difference between any two means is larger than random variation of the two statistics can be expected to produce.

To test observed difference between means, one can use the

statistic X± - Xq t = ------... Sp V (!/%) + (l/Hg) 2 where Sp is the pooled mean-square estimate of the variance squared,

gi-ven T>y , ^ (Ml-l)Sl2 + ( H g - p s / ^

1*1 + N2 - 2 where X = arithmetic mean, H = number of observations, and S =

standard deviation. The value of t can be computed and from it the

level of significance can be determined from a statistical table

giving the percentiles of the t distribution (Dixon and Massey,

p. 121 and 3®0- Using this method for the depths of leaching, confidence levels

for the significance of mean differences are as follows: Darby and

Caesar tills, 99 percent: Caesar and Boston tills, 95 percent: Boston and Danville tills, 99 percent. Clearly, the means for the depths of

leaching are significantly different and may be used as a criterion

for differentiating these till units. The depth of leaching of carbonate material from calcareous glacial drift is a principal criterion which geologists use in deter- 35

TABLE 3 TABULATION OF SOIL CHARACTERISTICS ASSOCIATED WITH TILL UNITS IN HIGHLAND COUNT!

(inches) Till Depth of Inches of CaCO^ Equiv. Unit pH Leaching Loess Content

Darby I mean 6.4 23.3 generally 32.6 (S.D.) 0.5 7*5 absent 2.4 (C.V.) 7.9 32.1 7.4 (N) 26 45 45 3 (range) 5*5 - 7.8 14 - 47 30.4 - 35*2

Caesar mean 6.2 34.3 13.1 26.6 (S.D.) 0.9 8.0 4.2 4.6 (C.V.) 14.9 23.3 32.4 17.3 63 172 172 12 IrLge) 4.7 - 7.8 17 - 58 6 - 2 7 21.0 - 34.0

Boston mean 5-3 59.1 19.7 19.7 (S.D.) 0.5 10.6 6.3 2.9 (C.V.) 9-0 18.0 31.9 14.8 0 0 47 89 89 9 (range) 4.5 - 6.5 2 7 - 8 0 10 - 36 14.3 - 22.9

Danville mean 4.6 104.1 28.3 ( 3 4 .4 )* 30.5 (S.D.) 0.2 16.0 7.8 (9.3) 4.6 (C.V.) 3.6 15.4 27.6 15.2 (N) 37 37 37 (104) 12 (range) 4.2 - 4.9 69 - 149 12 - 49 21.1 - 35.7

* Loess values for 104 sites on the Illinoian till plain

mean is arithmetic mean (S.D.) is standard deviation (C.V.) is coefficent of variation (N) is number of sites examined (range) is smallest and largest value mining the time factor in soil development. Generally, the greater the span of time during which material has been exposed to'weathering the greater the depth of leaching. However, time is not the only factor controlling the depth of leaching, but texture, permeability of parent material and of the resulting soil, carbonate content and type, clay content and type, topography, rainfall, temperature, depth to ground water, biotic environment, and rate of surface erosion or deposition may also affect carbonate leaching. According to Merritt and Muller

(1 9 5 9 )> the carbonate content seems to be the most Important.

Carbonate content has an inverse relationship to the depth of leaching; the smaller the content of carbonate, the greater the depth of leaching (other factors remaining constant). Depth of leaching is directly related to time; the greater the time interval of leaching, the greater the depth of carbonate removal. If we let L represent the depth of leaching, T time, and C the carbonate content, then the pro portionality t = 5 (!) may be written. By careful selection of sites to be examined, the numerous other factors mentioned above that affect leaching can be kept closely constant. If we let k be the proportionality constant, then the proportionality (l) becomes an equations

L = - k (2 ) C

Although equation 2 is a general expression relating the depth of leaching to time and carbonate content, its use is not widely applica ble because k is a variable constant; its value changes with time and 37 carbonate content. This is clearly seen if we use the mean values from

Table 3 for the depth of leaching and carbonate content, and time values (in units of 10^ years) of 1 7 *3 > 1 8 .1 , 2 1 .0, and 128.0 for the

Darby, Caesar, Boston, and Danville till (time values in thousands of years), respectively, and compute k in each case as follows:

Darby Caesar Boston Danville

(with loess cap) k » ----- 5 0 .1* 55*5 2 U.8

(without loess) k = ^3*9 31*2 3^*0 18.0 Probably the most significant factor causing k to change with time

is the very important effect, which is seldom recognized, that carbon

ate content has on depth of leaching as a result of its removal. Upon

leaching the remaining material is concentrated proportionally to the

amount of carbonates removed. For example, consider a parent material

containing 50 percent carbonates, and 25 percent clay and 25 percent

coarser material. On removal of the carbonate, the zone of leached material is reduced to half its original thickness. Now it consists

of 50 percent clay and 50 percent coarser material. This clay-rich

zone greatly decreases the permeability of rain fall through the

leached layer. Therefore, the rate of leaching progressively decreases with time not only because of the greater depth to carbonates, but

also as result of an increasingly impermeable zone being developed

above the carbonates. A material with only 25 percent carbonate content will affect

the rate of leaching much less than half that of the material contain ing 50 percent. On its removal, a material with originally 25 percent

clay content will be concentrated into three-quarters of its original thickness, and consist of one-third clay material. In the 50 percent carbonate example above, the clay content increased by 100 percent in the leached zone. In the 25 percent carbonate example, it increased only by 33 l/3 percent. This shows the exponential relationship be tween removal of carbonates and the resulting clay content increase.

One can therefore expect a till of lower carbonate content to be leached to greater depth than a till of higher carbonate content; this depth should be somewhat greater than a direct proportionality (other factors being equal). This relationship suggests an answer to the apparent anomaly of greater depths of leaching for the Boston Till compared to the Darby, Casear, and Danville tills.

Radiocarbon determinations on organic matter from drift associ ated with areas 1 and 2 (figure 7 ) yielded dates which Identifies area

2 as being about 800 years older than area 1 (on the average). How ever, area 1 was found to have a mean depth of leaching of 23.3 inches, in contrast to 3^*3 inches for area 2. This apparent anomaly is ex plained by consideration of the loess cover. Area 2 has a mean loess cover of 13.1 inches, whereas area 1 is generally without a measure- able loess thickness (see table 3)» Subtraction of the loess thickness from the mean depth of leaching gives area 2 a leaching depth very similar to area 1. This suggests that thin deposits of loess (lesB than 2 feet ?) are leached relatively fast compared to till. This is probably due to its texture and composition.

On the other hand, area 3 (postulated as "early" Wisconsin by earlier workers, see page 6) is leached to a mean depth of 59*1 inches.

It has a mean loess cover of 19*7 inches, which subtracted from the 39 mean depth of leaching gives a mean depth of leaching for the till of

39.1+ inches. This depth is about 16 and 18 inches more than areas 1

and 2, respectively. The greater depth of leaching associated with

the Russell soils of area 3 has been assumed to be the result of time.

Jane Forsyth states (1965, p. 225): "Thus, differences between the

"deep” and "shallow" Russell soil profiles are believed, with little

question, to represent a significant difference in age and no appre

ciable variation in composition."

To determine if the increased depth of leaching associated with

"deep" Russell soils was due to the time factor and not tovariation

in composition, carbonate content analyses were made on the till units

in Highland County (See Calcite-Dolomite Analyses, p.63 for details).

Tills from area 1 and 2 (Darby and Caesar) averaged 67 and 35 percent

more total CaCO^ equivalent, respectively, than tills from area 3 (Boston Till). Since only three carbonate analyses were made for the

Darby Till and its composition being similar to the Caesar in other

respects, the values for the two tills will be combined in the follow

ing discussion.

Under similar conditions of weathering, if a till with a CaCOg

content of 27.8 percent can be leached to a depth of 2 1 .1+ inches

(means of Darby and Caesar tills) in a unit of time, then a till with

19.7 percent carbonate content should be leached about 30 inches in

the same amount of time.

21.1+ x 27.8 = 19.7 x L percent inches percent

L » 30.2 inches 1*0

About 17,500 years (W-91, W-331, Y - ^ 8, OWU-2 5 6) Is a fair approxi mation of the average time that the Darby and Caesar Tills have been exposed to weathering since deglaciation (see page 7^). Then, 1.25

Inches of till was leached (on the average) each thousand years from the Darby and Caesar till.

21.1* -7- 17.5 inches thousands of years

= 1.25 inches/thousand years

In the same unit of time the Boston Till would be leached at an average rate of 1.75 inches per thousand years.

30.2 17.5 inches thousands of years

= 1-75 inches/thousand years

Two radiocarbon determinations (D-46, D-Vf,' see page 7h) date the

Boston Till at 21,000 years B.P. (clearly not "early" Wisconsin). At the average rate of 1.75 Inches of leaching per thousand years, this amounts to an additional 6.1 inches, or a total of 3^.3 inches, of carbonate removal. This compares very close to the average 39-^*- inches measured for thedepth of leaching in the Boston Till, exclud ing the loess cap thickness. When the important effect of the carbon- nate content is considered (mentioned above), the depths of leaching for the respective till units becomes even more compatible. Therefore, they should be approximately of the same age, which is what radio carbon dates have revealed. Illinoian till at the surface in Highland County is associated with characteristic soils which are consistently thicker and more deeply weathered than those in Wisconsin age till. Analyses (given in kl appropriate sections in this chapter)- reveal that the till parent mate rial of the 6A and 60 soils are very similar to that of the Illinoian till. Depths of leaching in Illinoian till soils averaged about 1(A inches for 37 well-drained sites examined. The mean loess thickness was

28.3 inches. Subtracting the loess thickness from the total depth of leaching gives a mean depth of 75*7 inches for leaching of the Illinoian till. This is about 5^ inches more than that for the mean depth of leaching of the Darby and Caesar tills.

According to Rhodes Fairbridge (1968, p, 923), the Illinoian

Glaciation ended about 128,000 years ago. The average rate of leach ing for the till has then been 0.59 inches per thousand years.

75-7 -5- 128 inches thousands of years

« 0.59 inches/thousand years

Compared to the Wisconsin 6k and 60 till soils which have an average rate of leaching of I.25 inches per thousand years, it is clearly seen that the rate of leaching must decrease considerably with time.

Figure 9 shows the depth of leaching plotted against time for average values obtained for Late Wisconsin and Illinoian soils of similar parent material. The important point shown by the curve is that the rate of leaching does appear to decrease with time; the rate is given by the slope of a line tangent to the curve at a given time. It is believed by the writer that the significant differences between these soils are quite clearly related to age, and not parent material.

Values for the CaCO^ content and the corresponding depth of leach ing have been plotted on the graph in figure 10 for the Caesar, Boston, Depth of carbonate leaching in inches iue9 Graph showing changing Figurerate The ofslope 9*of leaching a with time. 80 0Illinoian Danville Till 70 60 ko 50 20 30 10 0 0 10 per thousand years at that tine* line tangent to thecurve represents the rate of leaching in inches

> Darby Darby I and Caesar tills > Late Wisconsin / 20 " (averaged) "" —

Thousandsof years before thepresent 40

100

110

120

130 Depth of carbonate leaching (inches) 20 10 Figure 10. Diagram showing depth of carbonate leaching leaching carbonate of depth showing Diagram 10. Figure relation to carbonate content. carbonate to relation (minus thickness of loess cover) in in cover) loess of thickness (minus Caesar Till Caesar 20 slope = — = slope ecn CaCO^ Percent Danville Till Danville Boston Till Boston 0 slope -U- slope = - = slope 1.8 0.7 1* and Danville tills. The Darby Till was not plotted because only three carbonate analyses are available. Just those carbonate values were used which had depths of leaching values taken at or in close proxim- ■ ity to the site sampled. The resulting scatter diagram forms three clusters of points, one for each till group. The distinct grouping of these points further exemplifies the role of time and carbonate content on depth of leaching.

A best-fit regression line is drawn through each set of points.

It is recognized that many more points for each till should be plotted before any sound conclusions can be derived from such a diagram. Never theless, the distribution of the points (and the resulting regression lines) suggest that variability in the depth of leaching within the. same till-parent material is a result of carbonate content. The marked change in slope of the regression line for the Danville Till compared to the Caesar Till, about - 1.8 and - OA , respectively, further demon strates the exponential relationship of depth of leaching in relation to carbonate content over a period of time as discussed earlier. In actuality, a regression curve would probably be more representative of the relationship, and if more points were available this might be shown. This is suggested in the slope of the Boston Till regression line, about -0.7# compared to - 0 A for the Caesar Till. The greater portion of this increase is probably due to the lower carbonate content and not the additional 3#000 years of exposure to weathering.

Depth of leaching is a significant means of differentiating the till units in Highland County. The method should prove useful wher*- ever calcareous tills of contrasting carbonate content and/or age occur. ^5 Loess Cover From the above discussion one notices that the boundaries of sig nificant change in the thickness of the loess cap coincides with dis tal edges of the major moraines, Mt. Olive, Cuba and Reesville. Detailed petrographie and x-ray analysis of the loess cover of Ohio

indicates that the loess was deposited in two stages during Early and

Late Wisconsin time (Goldthwait, 1969)* The thickest loess cover in the area occurs upon Illinoian drift

loess averaged inches in 10^ sites examined on the Illinoian till

plain (table 3)* The loess iB also thicker to the west and becomes

thinner eastward. The clay minerals in the basal soil underlying the

loess clearly indicates a weathering period longer than postglacial

time and it is clear from regional tracing that the basal soil is due

to Sangamon weathering or Sangamon colluvial accumulation of weathered

fine-grained material. Loess covering the Boston drift of Late Wis

consin age was found to have an average thickness of 19*7 inches in 89

sites. This suggests that about the lower 15 inches of the loess cover in the Illinoian area was deposited prior to the Late Wisconsin, probably during the Early Wisconsin. However, a significant amount may have been deposited during advance of the Late Wisconsin glacier to its southernmost position. Only by observation of the mid-loess

break in the field or by laboratory analysis can the amount of loess belonging to the Early Wisconsin be determined. Deposition of the second loess probably began at least 21,000 and perhaps as much as

28,000 years ago. (Goldthwait, 1969).

Loess covering the Caesar drift averaged 13*1 inches in the ITS I

Figure 11. Dark subsoil phase of a Sangamon ‘till soil

covered by Wisconsin loess. Note G.I.

shovel in top center for scale. Bites which were examined. Thus, about six inches of loess was de posited during the time interval between retreat of the ice margin from its stand at the Mt. Olive moraine to the beginning of the re treat from the Cuba moraine. Loess deposition continued after retreat from the Cuba moraine but tapered off significantly after the readvance of the glacier to the Reesville moraine, about 17,300 years ago. Loess is generally absent, or patchy at best, northward from the Rees- ville moraine. Perhaps this was caused by a change in the regimen of the meltwater streams whose deposits provided a source for the loess, or perhaps vegetation rapidly stablized the source deposits upon de glaciation.

There is a significant difference (99 percent confidence) in the mean values of the loess thickness associated with the till units in

Highland County. Therefore, the use of these values appears a use ful criterion for distinguishing the till parent material for this area. Elsewhere this criterion should be used with caution due to the f variability in loess deposition over short distances.

Soil pH

Generally, pH reflects the base status of the soil and is a mea sure of the intensity of acidity or alkalinity (not the capacity or total amount). Differences in pH values are generally attributed to degree of weathering or time, providing the other soil forming factors are the same. However, pH values may reflect differences in parent material which are not determinable in the field. The procedure used in obtaining pH values during this study is described on page 8. The pH determinations did not show any significant difference "be tween the till soil associations developed in Darby and Caesar drift

(table 3)> This is not surprising since their parent materials are very similar and both are Late Wisconsin in age. Russell soils devel oped in the Boston drift had an average pH values of 5*3# significantly lower (99 percent confidence level) than the 6.4 and 6.2 values for soil developed in the Darby and Caesar drifts, respectively. Since the time factor for all three major soil associations (6a, 6 0 , 6 7 ) is nearly the same (Late Wisconsin age), one might conclude that the lower pH values in the Boston Till are related to its significantly lower CaC03 equivalent content. However, the pH measurements were made in the loess zone and not the till parent material as was the case in the

Darby and Caesar tills. Therefore, the lower pH values in the Russell

67 soil association is probably related to the texture and composi tional differences in the loess cover.

The lowest pH values in the Illinoian drift area occur generally near the base of the loess cover or the upper few inches of the under lying till parent material. Since the material in both these zones is older than the parent material of the 6 A, 6 0 and 67 soil associations, the significantly lower (99 percent confidence) mean pH value of 4.6 is the result of a longer span of weathering.

The use of pH values appears a useful criterion for distinquishing the major soil associations (with exception of the Miami 6A from the

6 0 ), hence, the identity of the till parent material. This method has extra value in that it can be used in the field. Faleosols

A buried soil, especially one developed during an interglacial period and covered by deposits of a later glaciation, is one of the more reliable marker beds used in glacial stratigraphic correlations.

A paleosol implies weathering of the unit in which it is developed, of sufficient duration for the formation of the soil. It can be used as

* evidence for retreat and subsequent advance of ice when found within a glacial sequence and, therefore, the identity of at least two strati graphic units.

The duration or time interval represented by a paleosol is not so readily deduced. If the entire soil profiles is preserved, a general estimate can be made as to the amount of time necessary for its for mation. From this estimate it may be possible to assign which time interval, i.e. Sangamonian, generated the paleosol. However, in most cases the paleosol is only partially preserved; the upper horizons are removed during subsequent ice advance leaving generally the C horizon and maybe part of the B horizon. In these cases, interpretation of the significance involves the use of the additional criteria discussed in this chapter. In the following the principal paleosols in Highland

County are described.

A buried soil layer, as reported by Orton (1 8 7 0 , p. 2 6 6 ) occurs at

Marshall where 11 out of 20 wells struck vegetal material at a depth of

20 to 30 feet. Since glacial drift extends deeper than the paleosol, which inturn is overlain by Illinoian drift, this buried soil may rep resent either the time interval between two Illinoian advances or a pre- 50 Illinoian (Yarmouth!an?) interval.

A paleosol developed in pre-Illinoian (?) stratified sediments of glacial origin (?) was found in a cut bank of Clear Creek during this investigation (locality C5l). A discussion of the section is given on pages 2k and 25. Since mechanical composition and rock suites of the overlying drift are indicative of the Illinoian Danville drift and the lower till of possible and Early Illinoian ( ? ), the paleosol may represent a partial soil profile of pre-Illinoian, perhaps

Yarmouthian Age.

Paleosols believed to have been formed during the Sangamon inter glacial time are exposed at several localities in the county (see the

Appendix, section A, for detailed descriptions). One Is locality C 58, two and three-quarter miles west of Rainsboro. It is 5 feet thick and developed in gravel and till. The paleosol is overlain by the Boston

Till, identified on the basis of its composition. Another Sangamon paleosol is three miles southeast of Samantha (location D3 6 ). This buried soil consists of five to six feet of leached sandy silt (fluvial, see Appendix, p. 153) overlying Illinoian till, identified by composi tion. Wood taken from the base of the Boston Till, which overlies the

.paleosol, gave a carbon lU date of 20,910 years (D-^7)- The Boston

Till Inturn is overlain by the Caesar Till. Another Sangamon paleoBol is exposed beneath Boston Till In a cut bank of a tributary to Little

Rock Creek (location C^7); wood from the till dated at 21,000 years old (D-^6 ). A thin paleosol, leached from six inches to two feet separates Danville Till from Caesar Till in a road cut (Route 1 3 8 ) about four miles southwest of Greenfield (locality B8 9 ). It appears 51 to consist of the lower B and C horizon

Other paleosols have been observed in the county but are pre sently covered. Dr. R. P. Goldthwait (personal communication, 1 9 6 8 ) observed a well-preserved Sangamon soil, a black "wiesenboden" (humle gley) four feet thick, developed in till beneath Late Wisconsin till on the northwest bank of Turtle Creek, two miles southwest of New

Vienna. This exposure has been disturbed and is no longer available for observation.

A paleoBol occurs 0.8 miles north-northeast of East Monroe on the east bank of Rattlesnake Creek. The location was visited by the

Friends of the Pleistocene (Midwest) during the Ohio meeting in 1962

(optional stop 12, mileage 1 6 0 .0 ). The paleosol is thought to have formed possibly during the interstadial between Early and Late Wisconsin.

The paleosol was not found during this study and has apparently been obliterated by stream erosion and slumping. A paleosol developed in

Caesar Till is overlain by Darby drift 2.2 miles east of East Monroe

(see discussion on page 21*-).

Clay Mineral Analyses

The clay mineral assemblages in till reflect the composition of bedrock and landscape (soils) that were incorporated into the ice dur ing glaciation. The source is generally within a few hundred miles of the point of till deposition. The clay mineral content of tills in

Ohio has been mostly discussed in the soils literature (Andrew, i9 6 0 ;

Bidwell, 19^9; Holowaychuk, 1950; and Wilding and others, 19^5), with 52 only a limited discussion by geologists (Droste, 195^; Teller, 1970)• Significant studies have been made in Illinois (Hillman, Glass, and

Fiye, 1963) and elsewhere in the midwest. Eighteen clay mineral analyses were made on tills in Highland County by x-ray diffraction using oriented-aggregate techniques. Quartz content was determined in each x-ray diffraction analysis and was found to be very similar in all samples. An average of 10 percent of quartz was obtained for each of the till groups. Quartz percentage was not included in computing the relative clay-raineral composition as it would only decrease the other clay-raineral percentages. Also presen tation of the data with quartz included would not allow easy comparison with other till clay-mineral data (Willman, and others, 1963, 19^6)• The clay-mineral composition of the Illinoian Danville Till, and the Wisconsin Darby I and Caesar tills are very similar and quite uni form within the county. They are characterized by a high illite and low vermiculite content (figure 12). The clay-raineral composition of the Boston Till is uniform and is characterized by a low illite and high vermiculite content relative to the Darby, Caesar and Danville tills. All the tills have very low montomorillonite content, but that of the Boston Till is apparently about twice that of the others. The contrasting illite-vermiculite contents are readily noticeable on x-ray diffraction patterns; it is also shown by calculating the peak- height ratio of l^X (vermiculite, chlorite, and montmorillonite) to loX (illite) for air-dried and ethylene glycolated samples (table k). The confidence level (C.L.) for which the mean differences are signif icant in relation to the Boston Till are also given in table k* \ 53

I-50ira»RlLL0NITE

ILLITE 80 50 20 CHLORITE, 20 80 KAOLINITE, percent VERMICULITE

Till Unite Age A Darby I A Caesar Late Wisconsin • Boston O Danville Illinoian Figure 12. Three-component diagram showing the clay-mineral composition of till units in Highland County. 54

T A B L E 4 RELATIVE PERCENT OF CLAY MINERALS IN THE LESS THAN 2 MICRON FRACTION OF TILL UNITS IN HIGHLAND COUNTY. RATIO OF PEAK HEIGHTS FOR 10 AND Ik ANGSTROM AIR-DRY AND ETHYLENE GLYCOL TREATED CLAYS.

Relative Percent Peak Height Till 5 Ratio

Unit 1 • * • • < w 3<; o

Darby (2 ) mean 80.5 3.0 13.5 3.0 461 4•37 (S.D.) 2.1 0.0 3.5 1.4 i,01 4•03 (c.v.) 2.6 0.0 26.2 26.0 «81 8.6 (C.L.) 99% 99* 99* - 99* 99* (range) 79-82 3-3 11-16 2-4 .61-.62 •35-.39

Caesar (k) 1 mean 75.0 2.3 12.5 10.2 4 35 1• 31 (S.D.) 1.4 0.5 4.0 2.4 0.5 .08 (c.v.) 1.9 22.2 32.3 22.0 13.3 28.4

(C.L.) 99* 99* 3

99* 99* 99* w

99* 0 1 (range) 74-77 2-3 7-16 8-13 .31-.42 . .

Boston (7) mean 54.9 6.9 33.5 4.7 1.18 .82 (S.D.) 5.8 4.0 6.3 5.0 121 .17 (C.V.) 10.6 58.6 18.8 94.4 17.5 20.5 (range) 43-62 2-14 21-39 1-15 .90-1.52 .55-1.03

Danville (5) mean 77.0 3.6 14.0 5.4 i• 55 .38 (S.D.) 4.4 2.0 4.3 3.9 1,12 1.12 (C.V.) 5.7 63.9 30.7 75.0 34.6 38.5 (C.L.) 99* 99* 99* - 99* 80' (range) 70-82 2-6 8-19 2-11 •30-.79 .ll+-.51

(n) Is number of samples; mean is arithmetic mean; (s.D.) is standard deviation; (C.V.) is coefficent of variation; (C.L.) is confidence level of mean differences compared with Boston Till value; (range) is smallest and largest value

i 55 The very close similarity in clay-mineral composition of the Darby,

Caesar and Danville tills probably reflects a similar origin in the

Erie Lobe. Glaciers that advance from the north contained a high pro

portion of illite derived from middle to late Paleozoic rocks in Ohio.

The clay-mineral composition of the Boston Till may in part reflect the

fact that a former landscape with an intensely weathered soil (Sangamon)

was incorporated into it.

\ The clay-mineral composition of the Illinoian Danville Till in

Highland County is most similar (figure 13) to the Buffalo Hart Till

(Latest Illinoian) described for Illinois (Willman, and others 1 9 6 3 )*

The average composition of the clay minerals in Buffalo Hart till is

6 9 percent illite, 5 percent montmorillonite, and 2 6 percent chlorite-

kaolinite (vermiculite is included in their chorite percentage).

* Willman, and others (1 9 6 3 , 1 9 6 6 ) give a northeastern source for the

Buffalo Hart till and those containing predominantly illite with minor

amounts of chlorite and kaolinite.

The Boston Till in Highland County possesses a clay-raineral assem

blage different from that of th Altonian age (Early Wisconsin) tills

described in Illinois. The Darby I and Caesar tills contain a clay-

raineral assemblage that is very similar to the Late Wisconsin Wood-

fordian tills studied in Illinois. The clay-mineral composition of the

Illinoian and pre-Illinoian tills in the area of southwestern Ohio,

southeastern Indiana, and northern Kentucky apparently have a high con

tent of expandable minerals (figure 1 3 ) (Teller, 1970, page 3 6 ).

The clay-mineral data presented here serve as strong evidence for

the occurrence of a distinct till in Highland County, the Boston Till. \ 56

MONTMORILLONIIB

ILLITE CHLORITE, KAOLINITE, VERMICULITE Woodfordian (Late Wisconsin) Altonian (Early Wisconsin) Illinois Buffalo Hart (illinoian)

Boston (Late Wisconsin) Darby, Caesar, and Danville Ohio (Late Wiscon.) (illinoian)

Figure 1 3 . Three-component diagram contrasting clay-mineral compositions of till units in Highland County with selected tills from Illinois and Indiana, 57

It can be readily distinguished from the overlying Late Wisconsin and underlying Illinoian till units by its lower content of illite and much higher content of vermiculite.

Particle-Size Distribution

The distribution of particle sizes has been used as a criterion for correlation of tills on Ohio. It has proven very satisfactory and internally consistent in some studies (Shepps, 1953# Steiger, 19&7 and

Inconclusive in others (Forsyth, 1956). Those plotted by Goldthwait

(Goldthwait and Rosengreen 196 9 , fig. 2-1) for central south Ohio, are difficult to use because most compositional areas over-lap greatly. A marked contrast in particle sizes between tills is generally the re sult of a different source area or a change in the size mode of the material and, hence, and emperical criterion for distinguishing be tween tills. Although the grain-size distribution for most samples within a till unit are similar, some vary widely from the median. These generally occur at the base of till units which overlie unconsolidated or readily erodeable deposits.

Mechanical analyses of 52 till samples from Highland County were made in the hope of distinguishing till units and establishing a cri terion for correlation (see Appendix, section C, p. 152 ). Particle- size distributions reveal that the Darby I, Caesar, and Danville tills have very similar mechanical compositions; the corresponding arithmetic means for the sand, silt, clay, and pebble size grades are within four- percent (table 5 ). However, the mean for the Boston Till analyses TABLE 5* PARTICLE-SIZE DISTRIBUTION OF TILL UNITS IN HIGHLAND COUNTY

Percent by Weight (pebbles on total sample; sand-ailt-clay on 2mm size fraction)

Pebbles-

ITvtM

Darby (4) mean 15.0 5.7 5.8 6.8 8.1 7.7 34.1 51.0 14.9 (S.D) 5-2 .26 .42 •95 .53 .49 * 2.0 2.8 2.7 (c.v.) 34.4 4.6 7.3 14.0 6.5 6.3 5.8 5.5 18.0 (range) 11-21 6.1-5.5 6.4-5.4 5-5-7.7 7.5-8.5 7-2-8.3 32-35 47-54 11-17

Caesar (17) mean 11.5 4.9 5.2 7-1 8.9 8.2 34.5 48.1 17.4 (S.D.) 3*4 1.5 1.4 1.7 1.7 1.3 6.7 3-7 4.1 (C.V.) 26.1 7.8 4.1 29.8 29.5 23.8 19.5 16.4 19.3 3 •d* LPv (range) 5-19 2.1-8.4 2.7-8.5 3.7-11.1 5.1=12.1 5.0-9.9 19-47 1 10-27

Boston (9) mean 6.2 3.2 3.7 5.8 8.1 8.1 28.7 51.2 19.7 (S.D.) 1.1 .70 .59 .88 1.1 1.1 4.9 3.6 1.8 (C.v.) 18.2 21.6 16.0 15.1 13.3 14.7 15.6 7.0 9.2 (range) 5-8 2.3-4.7 2.9-4*9 4.8-7.6 7.1-10.6 7.2-10.6 25-39 43-55 17-22

Danville (21) mean 14.9 5.6 6.0 8.2 9.7 8.3 37.8 48.8 14.4 (S.D.) 5.1 1.4 1.5 2.1 2.2 1.4 8.0 5.1 3-7 (c.v.) 44.0 25.0 24.4- 26.0 22.9 17.5 21.3 10.8 26.0 > - J5.2-10.6. 7-22 (range) 7-23 2.6-7.6 3.0-8.1 4.1-13.0 2 15.0 21-53 ^ - 5 ? . mean Is arithmetic mean; (S.D.) is standard deviation; (C.V.) is coefficent of variation 59 shows noticeable differences from the others: sand is five to eight percent lower; clay is five percent higher than in Danville Till; pebbles are seven to ten percent lower. Confidence levels for the significance of mean differences between the Boston Till and the Darby,.

Caesar, and Danville tills are given in table 6 .

TABIE 6 CONFIDENCE LEVEIS FOR.SIGNIFICANCE OF MEAN DIFFERENCES FOR PARTICLE-SIZE DISTRIBUTIONS BETWEEN THE BOSTON TILL AND THE DARBY, CAESAR, AND DANVILLE TILL UNITS______Percent Confidence Boston Till Till 2 .0 1 .0— 0«5** Total Unit Pebbles 1 .0mm 0 .5nm 0 .25mm Sand Silt Clay

Darby I 99 99 99 - 90 99

Caesar 99 . 99 99 95 95 -

Danville 99 99 99 99 99 99

Figure lU- shows the distribution for the sand, silt, and clay fractions of the tills examined.

Particle-size distributions show the Boston Till is overall finer in texture than Darby, Caesar, and Danville tills. This textural dif ference is readily observable in sections containing these units, as at locations C$Q, D 36 . The relative scarcity of pebbles longer than one inch In diameter in Early Wisconsin till is very critical when digging out pebbles for stone counts or fabric analyses. Particle-size distri bution proves a useful and corroborating criterion for correlation of tills in this area. \ 60

SAND 2 .0 -0 .062mm

8 0 50 20 20 0 .002mm percent

Till Units Age

▲ Darby I A Caesar Late Wisconsin • Boston O Danville Illinoian □ pre-Danville Figure lif. Three-component diagram showing the particle-size

distribution for till samples from Highland County. 6l

Pebble Counts

Pebble lithology has proven to be a very useful method in distin guishing drifts in central Ohio. Drift materials derived from diffe rent source areas generally have the most contrasting lithologies.

Wisconsin drift deposited by the Miami Lobe varies significantly from that deposited by the Scioto Lobe ice (Norris, Cross, and Goldthwait, i960);

Miami drift (west) Scioto drift (east) Calcareous; 79* 89* Clastic: 6 jb (calcareous) 1$ (noncalcareous, Ohio) Crystalline: 15$ (Canadian) 10$ (Canadian) Ls/Dol; 2256/5756 17&/72* Kempton and Goldthwait (1959) found significant differences in the pebble lithologies of the successive Illinoian and Wisconsin glacial outwash deposits in any one valley such as Hocking and Scioto Rivers.

Pebble counts were made from 51 till exposures and 13 gravel de posits in Highland County. The Darby, Caesar, and Danville tills have very similar pebble lithologies; they contrast sharply with those of the Boston Till (table 7)* The Boston Till is significantly different from the other three till units at the 99 percent confidence level for all lithology groupings in table 7» except the "Igneous + Metamorphic."

The most significant contrast in lithologies is that of the limestone/ dolomite ratio; it is nearly 1.0 for the Boston Till, 0,2k for Darby,

0.35 for Caesar, and 0.35 for Danville tills. The Danville ratio is strongly influenced by the relative increase in limestone and decrease of dolomite in the Upper Ordovician and lower Silurian strata which occur in western Highland County, i.e. for locations C80, C9 2 , C93> TABLE 7. PEBBLE LITHOLOGIES OF TILL UNITS AND ILLINOIAN GRAVEL IN HIGHLAND COUNTY

Till Percentage Igneous + Shale + Limestone IS + CHT Total Unit Metamorphic Sandstone + Chert Dolomite Dolomite Calcareous samples No. No. of

Darby I Till (5) mean 4.2 7.6 17.6 70.6 0.24 87.8 (S.D.) 2.8 3.8 1.3 3.6 .03 3.1 (c.v.) 66.1 49.8 7.6 5.2 12.2 3.5 (range) 5-14 16-19 .21-.29 0-7 66-751 85-91 Caesar Till (15) mean 7.5 8.9 21.1 62.5 0.35 83.6 (S.D.) 3.3 5-5 5.9 9-5 .15 6.6 (c.v.) 44.3 61.6 27.2 15.1 43.3 7.9 (range) 3-14 3-24 12-31 44-78 .15-49 68-94

Boston Till (7) mean 7.1 17.5 37*3 38.1 0.98 75-4 (S.D.) 3.6 6.1 8.6 8.6 .15 6.2 (c.vO 50.1 34.7 2 3 .O 22.5 41.9 8.2 (range) 2-12 13-26 32-51 . 30-51 .57-17 63-81 Danville Till (23) mean 7.0 7.0 22.5 63.5 0.35 86.1 (S.D.) 2.5 4.6 9.3 9.6 .24 5.0 (c.v.) 36.1 66.1 41.2 15.0 61.9 5.7 (range) 2-12 2-20 12-46 40-80 .15-1.15 74-93

Illinoian Gr, • (1 0 ) mean 5.2 4.7 23.2 66.9 0.36 90.1 (S.D.) 2.1 2 .8 8.2 7.7 .16 3.0 and Dl6 the mean ratio is 0.80 (see Appendix, p. 155). Figure 15 is a three component diagram which gives the distribution of the significant

rock groups for each unit. Pebble lithologies are deflnitly a useful

criterion for distinction and correlation of till units in Highland

County. Of added significance is the fact that the method can be

used in the field.

Calcite"Dolomite Analyses

The composition and quantity of calcite and dolomite present in

tills is determined by the composition and quantity of bedrock and

derived soil incorporated by the ice during glaciation. Using the

Chittick-Gasometric method (Dreimanis, 19^2), 72 dolomite analyses

were made on the less than 2 mm size fraction of 36 till samples from

Highland County (each sample was run twice, theresults averaged).

Analyses involved the determination of the weight percentage of calcite

and dolomite and the total CaC0 3 equivalent ($CaCC>3 =$ dolomite (1 .0 8 3 )

+ calcite). The mean values for each till unit are shown in table 8 ,

along with the confidence level of mean differences with the Boston

Till.

The analyses show that their is a significant difference in per

centage of limestone, dolomite, and total CaCOg equivalent occurring

in the Boston Till compared to the other till units. Calcite-dolomite

content can be used for stratigraphic correlation of the Boston Till

and for distinquishing it from the Darby, Caesar and Danville tills in

Highland County. As with the clay-raineral data, pebble counts, and 6k

SANDSTONE-SHALE CRYSTALLINE

LIMESTONE 20 DOLOMITE CHERT 20 percent

Till Units Age

A, Darby I A Caesar Late Wisconsin • Boston O Danville Illinoian □ pre-Danville Figure 1 5 . Three-component diagram showing the pebble lithology

for till samples from Highland County, 65

EABLE 8 CALCITE AMD DOLOMITE CONTENT IN THE LESS THAN 2mm SIZE FRACTION FOR TILL UNITS IN HIGHLAND COUNTY

Till Percent by Weight (for mean values)

Unit CaCOq Calcite (N) Calcite Dolomite equivalent Dolomite

Darby I (3) mean 8.8 22.0 32.6 .40 (S.D.) 0.7 2.8 2.4 .08 C.V. 7-9 12.7 7-4 21.0 (C.L.) 99* „ 99* 99* - 1 •p* . 0 .

8.4-9.6 VJ1 (range) 19-25 30-35 CO •v Caesar (12) mean 8.3 16.8 26.6 .49 (S.D.) 2.7 2.0 4.6 .13 C.V. 32.9 12.1 17-3 2 5 . 6 (C.L.) 95* 99* 99* - (range) 4.8-13 14-20 21-34 .31-.75 Boston (9) mean 6.0 12.5 19-7 .48 (S.D.) 1-7 1.4 2.9 .11 (C.V.) 2 7 - 6 11.3 14.8 23-3 (range) 3-0-8.7 10-14 14-23 .29-.66 Danville (12) mean 10.7 19-0 30.5' .56 (S.D.) 2.6 1.6 4.6 .12 (C.V.) 24.2 8.3 15-2 21.4 (C.L.) 99* 99* 99* , - (range) 4.1-13 1 6-21 21-36 .26-.72

(N) is number of samples; mean is arithmetic mean; (S.D.) is standard deviation; (C,V.) is coefflcent of variation; (C.L.) is confidence level of mean differences compared vith Boston Till value; (range) is smallest and largest value particle-size distribution, the average percentage of limestone and dolomite in Darby, Caesar and Danville tills is very similar, while that of the Boston Till is quite different.

Calcite-dolomite content of the Darby I Till is most similar to that of the Danville Till. The Caesar Till has large individual devia tions from the average values, some of which approach values for Boston

Till, i.e. B31, D25, D3^ (Appendix, page 1 5 6 ). However, difference be tween the two tills is great enough to allow a distinction. The ratio of calcite to dolomite, however, is fairly similar among all the till units. This is an anomalous relationship compared to the calcite/dolomite ratios for the pebble lithologies. There is no readily apparent explanation for this anomaly. An extensive discussion on the role which carbonate content plays in the depth of leaching is given in this

chapter beginning on page 3 1 -

Heavy Mineral Analyses

The usefulness of heavy minerals as an important criterion in establishing stratigraphic correlations in glacial deposits has been demonstrated in Ontario (Dreimanis and others, 1957) and in Illinois

(Willman and others, 1 9 6 3 )* Certain heavy minerals provide an effec tive method of differentiating tills from different source areas. The primary source of heavy minerals occurring in tills of Highland County is the Frecambrian raetamorphic-igneous rocks of the Canadian Shield.

Heavy mineral analyses were made on the very fine sand fraction

(0.062ram-0.125mm) of 32 calcareous tills in Highland County. In table 9 the individual suites are reported in percentage of total heavy minerals (Appendix, table 1 5 ), The suites are grouped as opaque, and transparent and translucent. The heavy mineral suites consist gener ally from 25 to percent opaque minerals and 55 to 75 percent trans parent. The black opaque minerals are chiefly magnetite, ilmenite, and hematite; the "other” opaque minerals are largely reddish hematite plus a few dark nondescript grains. The "other” transparent-translucent minerals are those which are too scarce to be of significance for cor relation purposes. These include such minerals as tourmaline, silli- manite, and andalusite, kyanite, pericline, topaz, zircon, olivine, and apatite.

A look at the mean values in table 9 shows that for the most part there is a similar distribution of mineral suites between the till units.

When standard deviation is considered, the mean differences are not sig nificant for Individual mineral suites. James Teller (1970, page 3 8 )

came to the same conclusion for the heavy mineral suites in the Illinoian and pre-Illinoian tills of southwestern Ohio, southeastern Indiana, and

northern Kentucky. This similarity is expected since all the tills in

Highland County were deposited from ice of the Erie Lobe. However, sig

nificant differences do occur between tills for the mean values of the

total opaques and total transparent-translucent minerals. The Boston

Till is different at the 95 percent confidence level in these two "total"

groups from the Caesar Till, and at the 99 percent level from the Dan

ville Till. Therefore, it appears that these two groups, total opaque

and total transparent-translucent heavy minerals, afford a means of dis- TABLE 9 . HEAVY-MINERAL CONTENT OF THE VERY FINE SAND FRACTION (0.062 - 0.125mm) FOR TILL UNITS IN HIGHLAND COUNTY

Heavy Minerals (percent) Till Opaque Transparent and Translucent et* 0 f Unit +> AJ0 GJ a H 0 number number of samples rutlie clear total pink actinolite augite diopside hypersthene enstatite hornblende sphene others total epidote tremolite & S total Darby I (3 ) mean 19.0 21.3 2.3 1.7 8.0 10.6 18.7 37.3 5.7 5.0 2.7 3.7 1.0 0.0 1.0 78.7 (S.D.) 6.9 9.1 2 . 6 3.1 4.0 6.5 9.1 (C.V.) 36.5 It2.5 33.1 28.6 33.1 17.4 (2 .7 3 ) 11.5

Caesar (1 0 ) mean 27.5 36.5 1.7 0.9 7.6 12.1 19.7 27.2 2.7 2.7 2 .9 2.0 1.6 0.6 1.5 63.5 (S.D.) 6.6 9.8 2.0 3.7 4.6 6.9 9.8 (C.V.) 2 3 . 8 26.9 25.7 30.3 23.3 25.5 *(2.69) 15-5

Boston (8) mean 24.6 27.8 1.1 2 . 2 6.0 14.5 20.5 30.8 3-4 4.3 1 . 8 1,3 2.4 1.1 3.7 72.2 (S.D.) 4.5 It.6 1.8 2 .8 2.7 3.7 4.4 (C.V.) 1 8 . ^ 16.5 29.5 19.5 13.3 12.0 (2.86) 6.1

Danville (10) mean 2 9 . ^ 37.3 1.8 1.2 6.0 13.5 19.5 27.1 3-0 2.4 2.3 1.6 1.5 0.2 2.0 6 2 . 7 (S.D.) 7.1 6 .1t 2.2 4.4 5.3 6.0 4L 6.4 (C.V.) 2 lt.3 17.2 34.0 32.2 27.1 22.1 (3.27) 10.3 Weight percent of heavy minerals in size fraction mean is arithmetic mean; (S.D.) is standard deviation; (C.V.) is coefficent of variation 69 tin

Fabric Analyses

The basic premise in making till fabric analyses is that the pre ferred alignment of the long axis of the pebbles is imparted either during transportation of the pebble within the ice or at the time of emplacement by moving ice, and corresponds to the direction of movement of the ice. It is also found that the pebbles tend to plunge upstream towards the source of the moving ice (Holmes, 19^1). However, it is not clear whether pebble fabrics are inherited from the orientations of pebbles in the ice or whether alignment results from deposition. It is now questioned whether till fabric represents the direction of ice motion during active glacial erosion, as the till was certainly de posited during a depositional phase of glaciation (Young, 19&9* P* 235l) 70 Nevertheless, till fabric is used in this study as an indicator of direction of ice motion because, as mentioned by Goldthvait (1 9 7 O, in press), • so may strong fabrics elsewhere do nearly parallel known striae and indicator paths, that the relation can hardly be fortuitous."

31 till fabrics were measured in Highland County and the results plotted in the form of "rose" diagrams. Till fabrics from the Caesar

Till indicate that ice movement was from the north-northeast between

Samantha and Rattlesnake Creek to the east (figure 16 , nos. 9-12* while those near Leesburg (nos. 1-3) indicate a north-northwest direc tion. The three fabrics measured in the Darby Till near Greenfield

(nos. ^-6 ) indicate that ice movement was from the north-northeast.

Of the four fabrics measured in the Boston Till, three show strong north-northwest direction of movement of depositing ice (figure

17* nos. l-3)» Till fabric no. ^ was made in the distal edge of the

Mt Olive moraine and its anomalous fabric compared to the others may be due to the mode of implacement of the till, or to subsequent slump ing. 15 till fabrics were determined in Illinoian Danville Till. Nine show strong preference for a north-northwest direction of movement of depositing ice (figure 1 8 , nos. 3 * 5* 6 , 7 * 9 * 1 0 , 1 2 , 1 3 , and l^f).

In sections containing multiple till sheets, till fabric can be used as an supplementary criterion to distinguish between units. This i is clearly seen at locality D 36 where three tills are present. The upper till (figure 1 6 , no. 1 2 ) predominantly indicates an eastern source as does the lower till (figure 1 8 , no. 4) while the middle till (figure •

1 7 * no. 2 ) shows a north-northwest direction of ice advance. 12 11

ReesviHe Moraine .(Darby X Till) Cuba Moraine (Caesar Till) Figure l6. "Rose” diagrams showing till fabrics of the Darby j and Caesar tills in Highland County. Number of pebbles used at top of diagram and site number at the bottom. Area of exposed Boston Till

^ ■njl-'** Wisconsin Glacial Boundary

Illinoian Glacial Boundary

Figure 17. ’’Rose1’ diagrams showing till fairies of the

Boston Till in Highland County. Number of

pebbles used at top of diagram and site

number at the bottom. T3 Wisconsin Glacial Boundary

Illinoian Boundary 2 0

C51ut

C99ut Dl6

10 10 20

C80 10

Figure 18. "Rose'* diagrams showing till fabrics of the Danville

Till in Highland County. Number of pebbles used at top

of diagram and site number at the bottom. Radiocarbon Dating

Previous radiocarbon dating in Ohio show that the Late Wisconsin ice front advanced into Ohio 2l*,600 years ago (W-71 Cleveland) and reached its maximum southward position 20,500 years ago (W-3 0 I* West chester) in the Miami Lobe and 18,500 years ago (Y-^8 Cuba) in the

Scioto Lobe (Goldthwait 1 9 5 8 ). An average of several age determina tions showed that the Miami Lobe reached its maximum position about l,i*00 years before the Scioto Lobe (Goldthwait, 1959)* Five radiocar bon age determinations have been received on wood found in Highland

County during this study. All wood was identified by Dr. George Bums of the Department of Botany at Ohio Wesleyan University. Four of these radiocarbon dates give additional evidence that the Scioto Lobe did not attain its southernmost position 1,400 years after that of the

Miami Lobe (table 10).

TABLE 10 RADIOCARBON AGE DETERMINATIONS ON WOOD FROM HIGHLAND COUNTY

Till Dated Age in Lab. Unit Location *ar Material years B.P. no.

Caesar D35 U.S.G.S. Picea sp. 2 0 ,i*60 ± 700 (W2l*59) Wash., D*C. (log)

Caesar E>39 U.S.G.S. Picea sp. 20,820 ± 600 (W2i*65) Wash., B.C. (log)

Boston 0*7 111. State Picea sp. 2 1 , 0 8 0 ± 200 (D-l*6) Geol. Survey (log)

Boston D 36 111. State Larix sp. 20,910 t 200 (D-l*7) Geol. Survey (branch)

* B.P., before the present; Pieea (spruce), Larix (larch) 75 A date of 21,080 - 200 years B.P* (D-^6) on a log found near the

"base of Boston till In the Mt. Olive moraine, two miles south of

Samantha (locality C^7)* identifies the till as Late Wisconsin. The till overlies a paleosol (Sangamon ?) developed in gravel. A cut "bank along Fall Creek (locality D 3 6 ) reveals three tills, the lower two separated hy a paleosol consisting of six feet of leached sandy silt.

A small tree branch found in the base of the till unit overlying the paleosol was dated at 20,910 - 200 years B.P. (D-Vf). This till is identified by clay-mineral data, texture, pebble lithologies, and car bonate content as Boston Till. It is covered by 12 feet of Caesar Till and separated from the latter unit by a one-foot thick layer of rubble and gravel.

These dates from the Boston Till are important in two ways: (l) they definitly identify the drift as Late Wisconsin in age and not

"early Wisconsin", as has been postulated, (2) these dates give sup porting evidence to two previous radiocarbon dates (on buried wood from pre-Cuba moraine till in the Todd Fork valley of Clinton County) that the Scioto Lobe reached its maximum southward advance about 21,

350 years B.P. (average of OWU-1 5 9 ,1 6 0 , about 8 5 0 years be fore the Miami Lobe maximum. The two age determinations from Todd

Fork valley west of Silgo of 21,137 - 1*^35 years B.P* (OWU-159) ■f* and 22,255 - 1 * 6 5 2 years B.P. (OWU-1 6 0 ) probably date the ice advance to the stand at the Vandervort moraine in Clinton County (Teller, 1957)*

The moraine trends southeast in western Clinton County and is overlap ped at right angles by the Hartwell moraine of the Miami Lobe in Warren

County (figure 19). Eastward the Vandervort moraine is diagonally over- Wisconsin Boundary

Warren Co. Clinton Co Ulinoian Boundary 22,2551 1,652 (OWU- J --- M 0 ^ 21,13711,435 (0WU-I59)

Butler Co (I- 4795)

18,5001400 20,820*600 (Y -4 48) _ / MW2465)

-121,0801200 (D-46) / 20,9101240 (D-47) Hamilton Co 25,300*600 (1-4797) H a r tw e ll

Mt. Olive Highland Co. Vandervort

Figure 19. Map of Highland, Clinton, Warren, Butler, and Hamilton counties showing location of moraines and radiocarbon dates. o\ 7T lapped by the Cuba moraine, which also overlaps the Mt. Olive moraine at right angles farther to the east at the Highland-Clinton county line. The drift of the Vandervort and Mt. Olive moraines may well be the same stratagraphic unit.

A date on a log found in the Caesar Till of the Cuba moraine

(locality D35) of 20,460 - 700 years B.P. (W2459) identifies the moraine as Late Wisconsin. Another log from the Caesar Till was found in a cut bank along Cedar Run (locality D39)* and gave a date of 20,820

- 600 years B.P. (W2465). A recent radiocarbon determination dates a log from Caesar Till in Clinton County (Teller, 19&4, page 70, location + 4x) at 19,800 - 400 years B.P. (1-4795). The till underlies a sand- gravel-till-sand section that is about 23 feet thick (top to bottom) and occurs in the area of the Inner Cuba moraine. The till from which the log was obtained appears to be related to the drift deposited dur ing advance of the glacier to the position of the Outer Cuba moraine.

Several previous radiocarbon dates on logs from the Caesar Till give a younger age for the deposition of the Cuba end moraine, using the three youngest dates, the average date determined for the Cuba mo raine in Clinton and Ross counties is 18,177 years B.P. (Y-448, W-91,

W-331). The average standard error in these dates (- 400 yr) does not encompass the age differences compared to the more recent dates ob tained for the Cuba moraine (l-4795> W-2559, W-24 6 5 ).

Two hypotheses may possibly explain these apparently anomalous dates; I believe the first one seems the most plausible, (l) The group of three recent dates probably were made on wood incorporated earlier by the glacier during its southward advance in Ohio and represent the 78 time the trees were up-rooted. However, they were not deposited until the glacier made its stand at the Cuba moraine. The time of such a stand is more probably represented by the youngest dates within a group of dates, as they would come from the last trees to be up-rooted by the advancing glacier. In the case of the Cuba moraine stand this would be about 18,000 years ago. (2) In the second hypothesis, it Is assumed that the group of recent dates represents the glacier’s stand at the position of the Cuba moraine in Highland and Clinton counties at about

20,500 years ago (average of 1-4795* W2459* W2465). Since dates with in this range have not been obtained from the Cuba moraine In adjoin ing counties, it suggests that the outermost push of the Scioto Lobe in these counties came at a later time, about 18,000 years B.P. A cut bank along Blinco Branch (locality C5 8 ) yielded a log from till which was dated at 25,300 - 600 years B.P. (1-4797)* The till underlies ten feet of gravel in which a paleosol (Sangamonian?) is developed to a depth of five feet. The paleosol is covered by 8 to 10 feet of Boston Till of the Mt. Olive moraine. The till from which the log was obtained is correlated by stratigraphy, clay minerals, pebble • lithology, texture, and carbonate content as Danville Till of Illinoian age. However, the date on the log identifies the drift as Wisconsin.

The log came out of the upper one foot of the till unit. This part of

the till was soft and saturated with ground water seeping from the base

of the gravel unit. Possibly ground water drainage from the surround

ing pastures has contaminated the wood or it was contaminated in handl

ing. It does not seem plausible that 4,000 years allows enough time

to develope a soil represented by the paleosol; the gravel was covered ’by the 21,000 year advance of the ice to the stand at the Mt. Olive moraine. A second piece of wood obtained lower in the compact por tion of the Danville Till was found in May, 1970 and is now being dated. DESCRIPTION OF GLACIAL FEATURES

Illlnoian Margin

There is no well-developed marginal drift ridge at the "border of the Illinolan drift that can "be interpreted as end moraine. At its maximum advance, the Illlnoian glacier either did not make a stand that was long enough to "build a moraine, or erosion has since obscured any moraine that was formed. Instead there is a zone of transition from a driftless area to one in which the drift is a well-defined deposit.

This occurs in a distance of less than a half mile, and often in a space of few hundred yards. The "border of the Illlnoian till in Highland

County conforms more or less to features of major relief, abuting hills and extending short distances down valleys (plate I).

In a few areas the boundary of the drift becomes inconspicuous.

James Roger (1936, P* 30) mentions "on the ridge south of North Union- town, foreign boulders are scarce and the veneer of drift is only a few feet in thickness. The surface is strewn with silicified stroma- toporoids and geodes weathered from the Lilley and Peebles dolomite."

During this study, the entire ridge from North Uniontown to ElraBvllle showed no evidence of glaciation. A cistern and a basement excavation at North Uniontown revealed no indication of glaciation. However, foreign boulders and pebbles occur In Cox Branch Just northeast of North

Uniontown, and till soils occur on the interstreara area north of Cox 80 81

Branch and of the headwaters of the Middle Fork of Ohio Brush Creek.

East of Middle Fork the soil is derived from residuum, and not a single foreign pebble was found during a thorough search of several plowed fields.

That the glacier extended on to the top of Long Lick Hill is attested by a gneissic granite erratic ^ x 3 x 2 ^ feet in size, locat ed on the westernmost point of its nearly flat top, at an elevation of

1310 feet. Several other granitic cobbles are present on this hill along with a small sand and gravel veneer covering its highest point,

1321 feet above sea level. Also several exposures of till occur in the valleys between Long Lick Hill and Washburn Hill, and the latter and

Feeds Hill. Leverett, a careful and thorough observer, notes the com mon occurrences of till in this area: (1902, p. 2 7 3 -27^ • . •

"Near the bend of Brush Creek, a short distance north of Fort Hill, in Highland County, there are deposits of till rising to a height of about 75 feet above the creek and ex tending to an undetermined distance beneath the creek bed. The till contains not only pebbles, but also boulders of Canadian derivation, some of which are 2 feet or more in di ameter. The great thickness of till at this point may seem remarkable, since there is scarcely any drift south and east of this creek. It is probable, however, that it is in the line of a preglacial valley."

The till in this area is coarser textured, with higher than normal amounts of sand and pebbles. Thin scattered patches of poorly sorted gravel overlying till are common.

An irregular discontinuous belt of drift extends from the gravel hills west and south of Hillsboro eastward to the north margin of the

Beech flats area in Pike and Ross counties. The belt of drift does not have the characteristics of the well-developed moraines of Wisconsin 82 age in the northern half of the county. Instead, it is composed pre

dominantly of kames, with till ridges uncommon and short. Over much

. of its course the boundaries of the drift belt are not clearly defin

able.

This belt of drift was described by Leverett (1902). He believed

that it was a continuation of the ’’early" Wisconsin moraine, (which he

had named Cuba) that was so-well developed south of New Vienna (see

plate I). In describing the belt of drift at Beach Flats, he says (p.

3^1—3*+S): "On the north side of "Beech Flats," in Pike County, and near the eastern line of Highland County, Ohio, this moraine becomes clearly separated from, and distinctly developed out side of, the later ones. It is readily traced westward along the south side of Rocky Fork, from the mouth to the source of that stream, the villages of Cynthiana, Carmel, and Marshall being situated near its southern margin, and Hillsboro Just north of it. Its breadth is one to two miles. In the vici nity of Hillsboro, the creek winds among sharp gravelly knolls, which have a contour strikingly different from the remainder of the belt, and which may prove to belong to the earlier drift sheet. Northwest of Hillsboro the moraine for several miles is not well developed, but a mile or two southeast of New Vienna it reappears in considerable strength. From that point it takes a westward course . • . Continuing westward into Clinton County its margin at the East Fork of Little Miami River is at the crossing of the Martinsville and Hills boro Pike. . . North of Beech Flats, In Pike County, and in south eastern Highland County, the moraine is of subdued type and stands only 10 to 25 feet higher than the north border of these flats. Towards the west, sharp gravel hills, 80 to 100 feet in height, set in, among which are low tracts no higher than the tracts outside (south) of the moraine and but little higher than the valley of Rocky Fork, which lies to the north. As already stated, these gravel hills may belong to the ear lier drift sheet Instead of this moraine. Both north and south of this portion of the moraine there are rocky hills bearing scarcely any drift, which stand much higher than the moraine. The moraine is, therefore, not so conspicuous a feature as it would be on plane tracts, such as are found in northwestern Ohio, or even those in the adjoining counties, Clinton and Fayette, where there are few rocky hills." From tbis description it is apparent that Leverett bad doubts about the age of the kame deposits within the course of the "moraine,” but, perhaps because of its subdued and discontinuous nature and the relatively shallow depths of leaching of many kames, he felt it be longed to the Early Wisconsin.

Rogers (1936, p. b^-bb) believed this belt of drift was probably of Illinoian and not Early Wisconsin age. The findings of the present study support his conclusion. In addition, it is believed by the writer that this irregular discontinuous belt of kame-moranic drift does not represent the position of the Illinoian ice front when it was built.

Instead, the discontinuous belt of drift is believed to represent successive stages in the retreat of the ice front; segments of the moranic belt being constructed over a period of retreat. The subdued kame-moranic deposits in Beech Flats (figure 20) were built during and shortly following the time of maximum advance of the glacier. The large kame complex south and west of Hillsboro (plate I) was the last part of this belt to be deposited.

Illinoian Ground Moraine

An area of about 150 square miles of Illinoian till plain covers the western one-fourth of Highland County. Its surface is generally very flat (figure 2 1 ) and is so nearly level as to be somewhat poorly to poorly drained (surface slope ranging from less than 5 to about 15 feet per mile). The average thickness of drift In this area west of Qk

Figure 20. Subdued kame-moralnic deposits in western Beech Flats

View looking southwest towards Irons Mountain from

McNary Road, one mile north-northwest of Cynthiana. 85

Figure 21. View of Illinoian till plain two miles

north of the village of Russell. 86 the Niagaran Escarpment is 53 feet (based on data from 60 vell-logs), with a range from 6 feet to 1*4-7 feet. Controlling the topography is the nearly flat southvestward sloping bedrock surface below the drift cover (see figure 3 )* From the Niagaran Escarpment eastward, the preglacial bedrock sur face predominantly determines topography; only in the eastern central part of the county, in the vicinity of Carmel, Marshall, and Rainsboro, is ground moraine constructional with hummocky, undulating topography.

Just south of Hillsboro kames and related ice-contact drift is chiefly responsible for the topography (plate I).

In the hilly region around Hillsboro and to the south and south east, thickness of till is variable. In the northern portion of this hilly region, Illinoian till mantles all the upland with a thickness averaging about 15 to 20 feet. Till accumulation is much thicker in valleys, with depth of *4-0 feet common. However, on the valley slopes between the upland and the valley bottoms till is generally absent and bedrock is the predominant surface material. Proceeding southward the till continually becomes thinner on the upland (flat-topped ridges for the most part) and bedrock exposures become more frequent. Finally in the region of Fairfax-Belfast and southward ridges and slopes are al most devoid of till, which is restricted to valleys between ridges.

Apparently Illinoian ground moraine was deposited with very lit tle erosion of the preglacial surface over much of Highland County.

This is logical, at least in the terminal area of a far-travelled glacier. At several sites, including rock quarries, residual soils and/or oxidized weathered rock extend 10 to 2 0 feet beneath the base 87 of unoxidlzed till. Thick exposures of Illinoian till are few, hut where present the average depth of oxidation is 13 feet (from 12 sites), ranging from 9 to 15 feet. Both the yellowish-brown oxidized and the dark gray unoxldized portion of the till are very compact, even notice ably more so than Wisconsin age till. Illinoian till is also charac terized by vertical joints to a much greater extent than Wisconsin till.

The joints extend down from the oxidized till into the dark gray till for a distance of three to 10 feet. The joints are filled with illuvi- al clay films ranging in color from yellowish-red, strong brown to yellowish-brown.

late Wisconsin Moraines

Late Wisconsin or Woodfordian drift covers the northern third of

Highland County. The drift was deposited in a system of four end mo raines and associated ground moraine. Three of the moraines are more or less continuous across the county. Drift associated with these moraines was deposited during a major advance or readvance of the glacier and are recognized as individual till units.

Mt. Olive Moraine

Drift deposited by the first advance of the Late Wisconsin glacier forms a belt one to four miles wide across the county from Clinton

County, two to three miles southwest of Hew Vienna, eastward to just be low the junction of Rattlesnake Creek with Paint Creek at the Ross

County line. An end moraine forms the southern one to two miles por- 88 tion of this Late Wisconsin drift. It is herein named Mt. Olive moraine from the church on its crest three miles south of New Vienna.

The Mt. Olive moraine is readily traced across most of the county (plate I). At its western boundary the moraine emerges as a low ridge from beneath the Cuba moraine (next northward) which over laps the former at about right-angles. The Mt. Olive Moraine trends

southeast one mile, then abruptly turns east for about two miles.

Turtle Creek follows a meltwater channel southward through the moraine at the locality of the abrupt turn. The moraine crest rises in eleva tion from about 1120 feet at the meltwater channel to 1180 feet two to three miles to the east. However, the rise in elevation does not in dicate an increase in drift thickness as the north-south trending

Niagaran Escarpment is beneath the moraine at this locality. Well-log data reveal that bedrock occurs 30 "to kO feet below the crest (ll80

feet high), while westward the drift thickness increases until at the

county line bedrock is over 100 feet below the surface.

The Mt. Olive moraine in the western portion of the county has

several crests of from a third to half a mile wide with intermittent

stream drainage developed parallel to the individual crests. The mo

raine area between Mt. Olive church and Turtle Creek to the west con

sists of five crests, radiating like spread fingers on a hand; the

southernmost one trends southwest and the northern one trends north

west (plate I). The multiple crests show that Wisconsin ice margin

either retreated in pulses or fluctuated back and forth during formati

on of the Mt. Olive moraine.

Eastward the moraine trends southeast down the headwaters of the Clear Creek drainage "basin as far south as the mouth of Hussey Run.

Several short moraine crests occur in the "basin. A well developed

"loop-moraine" occurs along the sides of Hussey Run valley for ahout half a mile (figure 2 2 ) and then curves in towards the center of the small valley where Hussey Run has cut a gap through the moraine.

Similar loops, "but less distinctive, occur a mile west in Clear Creek valley, and two miles east in little Rock Creek valley.

From Hussey Run valley, eastward to Boston the "boundary between the moraine and Illinoian drift to the south is inconspicuous as a result of strong bedrock control of topography and accompanying thin ning of the Wisconsin drift. For the most part the Wisconsin drift ex tends southward just beyond the bedrock crest which forms the northern drainage divide of Clear Creek. The Wisconsin glacier was strongly in fluenced by topography between Boston and Rainsboro. A tongue of ice extended southward down Blinco Branch, coming within a mile of Rocky

Fork Lake, depositing moraine in a broad loop. From here the Mt. Olive moraine can be traced eastward crossing the road three-quarters of a mile north of Rainsboro. The moraine trends northeastward towards Faint

Creek and continues into Ross County just south of the mouth of Rattle snake Creek. __

In the newly built section of Ohio Highway 73 that crosses the Mt.

Olive moraine, the average depth of oxidation is about 12 feet. Depth of leaching ranges from 38 inches to 65 inches. The average loess thick ness on flat areas along this two-mile-long section of highway is about llf inches. The thickness of the drift forming the Mt. Olive moraine east of Boston averages 31 feet in 8 well-logs. 90

Figure 22. A segment of the well-developed "loop-moraine"

in Hussey Run valley. View looking east from

Careytown South Road. 91

Cuba Moraine

Leverett (1902, p. 3^1) named the Cuba moraine after a town that

stands on its crest in south-central Clinton County. However, he

ascribed it to the Early Wisconsin based on its topography, its gen

eral freedom from silt in relation to the Illinoian till plain to the

south, and that it occurs beyond the terminus of the Late Wisconsin as

mapped by Chamberlin (1883, pp. 339-3^1)* Radiocarbon dating identifies

the Cuba moraine as Late Wisconsin.

In this study the Cuba has been traced from Clinton County east

ward into Highland County; it forms the next end moraine north of the

Mt. Olive moraine. However, Leverett traced the Cuba moraine across

Highland County to just south of Hillsboro and then east to Beech Flats

(see page 82). James Rogers (1936, P* correctly cast doubt on the

age of this "early” Wisconsin drift border. He believed it to be "pro

bably" Illinoian. Rogers believed, incorrectly however, that "early"

Wisconsin drift occurred at the surface in the county. He assigned a

belt of drift to this age chiefly on the basis of depth of leaching and

loess cover; the Mt. Olive moraine, which he called the Cuba, formed its

southern boundary. To the north he believed that Rattlesnake Creek

and Lees Creek was the boundary for this "early" Wisconsin drift.

Over most of the course of the Cuba moraine in Clinton County it

consists of two moraines, and Outer and Inner, separated by narrow

stretches of ground moraine. In Highland County the Inner Cuba gen

erally abuts the Outer Cuba moraine and patches of ground moraine

seldom occur between them. Field relationships suggest the Inner Cuba

moraine represents a stand of the Late Wisconsin ice after a short re- 92 treat from the Outer Cuba position. Ho stratigraphic evidence was found to suggest that the Inner Cuba represents a stand after a sig nificant readvance of the glacier.

The Outer Cuba moraine enters Highland County from Clinton County just south of New Vienna, where it overlaps the Mt. Olive moraine.

The distal edge of the Outer Cuba moraine just enters Highland County and disappears; ground moraine is mapped for about two miles before moranic topography, assigned to the Outer Cuba moraine, is again observ able (plate I).

The crest of the Inner Cuba moraine is 105 feet above bedrock at the radio tower a mile and a half east of New Vienna; it stands 50 feet above the ground moraine to the south and as much as 90 feet above the surface to the north. Drift is 78 feet thick on the Inner Cuba moraine at Careytown. The Outer Cuba moraine has a drift thickness of 75 feet three quarters of a mile south of Careytown and has a double crest.

At Samantha and westward for about two miles a narrow belt of ground moraine up to half a mile wide extends beyond the Outer Cuba mo raine and abuts the bedrock hills and ridges. The Inner Cuba moraine fades out northeast of Samantha, but is prominent two miles east of

Samantha on the north side of Ohio highway 138. Several wells just north and east of Samantha go through morainic drift that is about 80 feet thick. North of New Petersburg, Fall Creek flows along the distal edge of the Outer Cuba Moraine and Big Branch separates it from the

Inner Cuba moraine. The Cuba moraine of this area is very hummocky, with numerous knolls and short ridges, and does not possess the long continuous crests and gently undulating surface found to the west. 93

East of Rattlesnake Creek the Cuba moraine is hard to recognize

"because of the influence of "bedrock on its topography. However, data

from over 30 well-logs in the area allows raorainic portions to he iden

tified. One of these is between Rattlesnake Creek and Cedar Run and is

quite hummocky. Here drift covers bedrock to depths up to l6j feet.

Most of the topography between these isolated patches of moraine

consists of bedrock covered with drift less than 25 feet thick. The

moraine patches trend eastward into Ross County; here the course of the

Cuba moraine is not sure or obvious because of the numerous bedrock

hills involved. It is at this position, near the Ross County line,

that the Late Wisconsin drift seems to overlap the northwest trending

Mt. Olive moraine.

Wilmington Moraine

The Wilimington moraine was named by Teller (196U, p. 2 5 ) for a

subdued ridge which lies parallel to the Cuba moraine and two miles

north of it in Clinton County. Rogers (1936, p. ^7) noted the moraine

but he did not give it a name. In Highland County, it rises less than

20 feet above the till plain to the south, and about 30 feet above that

to the north. It enters Highland County three miles west of Highland

village. Here the South Fork of Lees Creek flows eastward along its

distal edge for about a mile, then turns northward through the moraine

and flows along its proximal edge for a mile. The moraine becomes indis

tinguishable from ground moraine just south of Highland. Scattered

hummocks just north and paralleling Bridgewater Creek suggest a pos

tion of Late Wisconsin ice edge at the time of Wilmington moraine deposition. Its faintness and lack of stratigraphy do not suggest the important readvance postulated by Teller (196^, p. 6 7 )*

Reesville Moraine

The Reesville Moraine was named "by Leverett from the village that stands on its crest in Clinton County. The moraine trends southward and southeastward through Clinton County, crosses the southwestern cor-

♦ ner of Fayette County, and enters the northwest c o m e r of Highland

County trending eastward* The Reesville moraine is double crested throughout much of its course in Clinton County, but in Highland County, the crests are discontinuous and hummocky topography is characteristic.

The moraine forms a slightly arcuate belt across the northern por tion of Highland County, nowhere extending far enough southward to be completely inside the county. The distal edge of the Reesville moraine is scarcely noticeable to the casual observer for the rise onto the mo raine is seldom abrupt. The most noticeable height occurs due north of

Leesburg, and the rise is less pronounced from East Monroe eastward.

The crest of the moraine rises 30 to 80 feet above the ground moraine to the south. Limited well-log data available (l4 wells) indicates the drift form ing the Reesville moraine is somewhat thinner than that of the Cuba moraine. Its average thickness is 50 feet compared to about 80 feet for the Cuba moraine and feet for intervening ground moraine.

Ground Moraine

The largest area of ground moraine deposited in association with the Mt. Olive moraine occurs from Samantha eastward to Faint Creek, be- 95 tween the Cuba and the Mt. Olive end moraines (plate X). The area of ground moraine attains a width of just over two miles in the vicinity of New Petersburg. Overall, the ground moraine is thin, averaging 211- feet in IT wells (exclusive of several broad bedrock hills that are veneered with less than five feet of drift). For the most part the topography is generally undulating.

Near Samantha and westward, the belt of exposed ground moraine is less than a mile wide. Generally it is thin, covering bedrock hills and slopes. At several sites, one can hand auger to bedrock within six feet. Commonly six inches to a foot of this is yellowish-red (5XR *j/8-

6/8) residual soil of clay texture, developed from dolomite, and occurs beneath the Wisconsin till. Deposition of this drift was not preceded by much abasion of the pre-Wisconsin surface in this area.

The largest area of Late Wisconsin ground moraine occurs between the Reesville and Cuba moraines from the region of Highland to Paint

Creek. The ground moraine has a characteristically low relief undulat

ing surface in which major streams and tributaries are incised from 40

to 80 feet. Here and there occasional bedrock knolls rise above the

general surface level, such as the two just south and southwest of

Leesburg, and the one just northwest of Greenfield. Most of these knolls hav3 a veneer of drift and exposure of bedrock is rare. An average of

60 well-logs from the ground moraine area yielded a depth of feet, with a range from 6 to 128 feet. Few areas of flat till plain exist,

but one of about four square miles is found just north of Highland.

Smaller areas, of flat till plain on the order of hundreds of acres,

exist south of Leesburg and southwest of Centerfield and Greenfield. 96

Soil profiles by auger indicate till in all three

Karnes

Kames are small mounds and larger hills consisting of poorly sort

ed to well-sorted sand and gravel, deposited from running water in close association with glacial ice or stagnant ice. They are common features

in Highland County and are most plentiful in drift of Illinoian age, with only a few occurring in the Wisconsin deposits.

Illinoian The largest area of kame accumulation and related ice-contact stra

tified drift occurs from two to four miles south of Hillsboro, and from

Rocky Fork westward for six miles to Shackleton. Within this area there

are at least 2k large kames or kame groups and numerous gravel mounds

and low knolls. Probably one of the more picturesque groups of kames is

one just north of Ohio Highway 62, and a half mile southwest of Hills

boro. Another very striking group occurs just north of Ohio Highway

138, between Shackleton and Rocky Fork Creek. It consists of several

connected hills,' forming kame and kettle morainic topography, in which

the highest kames obtain an elevation up to and exceeding 1200 feet. Several of the kames in this area are as high or higher than the

surrounding bedrock hills of the Niagaran Escarpment. Well-log data reveal that the bedrock surface is generally over 100 feet beneath the kame surface; two wells encountered bedrock more than 150 feet down. A

gravel pit located just south of Rocky Fork Creek, 2.If miles southwest

of Hillsboro (locality C9*f) has exposed the north side of a kame that 97 rises to an elevation of over 1130 feet. At this site about 100 feet of gravel and sand overlie 30 feet of exposed Danville till.

Kame material in this area is leached and oxidized to variable depths. At site C9^ the gravel is fresh, limestone pebbles occur with in two to three feet of the surface and oxidation extends to about 5 feet. Large blocks of conglomerate, some exceeding 10 feet in diameter, resulting from cementation of the gravels by calcite are exposed in the gravel pit. Occasionally, these blocks are found on slopes and at the base of the kames within the area. Most of the steep sided kames com posed of gravel and minor sand have similar weathering characteristics.

However, kames consisting of finer materials are leached relatively deeper and generally are broad, low knolls. One of this nature, locat ed two miles south of Hillsboro on Ohio Highway 2kT, rises to Just over

1060 feet above sea-level. A pit in the east side shows it contains 15 feet of leached silty sand overlying very well-sorted pea gravel and sand. Oxidation extends to a depth of 20 feet.

Several scattered kames occur eastward along the northward-facing slope south of Rocky Fork Lake. The small village of Marshall is situa ted atop a broad kame. One three miles west of Marshall trends east- west for nearly a mile. Both' these kames contain chiefly sand with minor amounts of fine gravel, and are leached to at least eight feet

(limit of auger).

Numerous kames occur among the Mississippian outliers near the eastern border of the county. Two large kames are located Just west and north of Spargur Hill near Carmel. Both have variable surface weathering effects; the knolls consist of gravels leached to about four 98

feet, while the gentle slopes consist of sand leached to around seven

feet. Several small kames occur north of Irons Mtn. Intervening

areas consist mainly of sand and silt. Exposures of till were seen

four to six feet beneath sand and gravel in road cuts along Ohio Route

506 between Carmel and Cynthiana. Well-logs in this area show bedrock

occurs from about 7 0 to 100 feet below the drift surface.

A large kame complex occurs from The Point at the mouth of Rocky

,Fork northwestward for about three miles. Several of the kames are

elongate and sinuous and could be called eskers; they contain very

well-sorted gravel and sand. Most of the broad knolls have poorly

sorted gravels. Depths of leaching ranged from two to 15 feet^ oxida

tion from three to 15+ feet. Well-log data shows these stratified

ice-contact deposits are much thinner than those south of Hillsboro,

about 30 to ^0 feet thick. Isolated kames occur throughout the

Illinoian drift area east of Niagaran Escarpment.

The majority of Illinoian kames in Highland County exhibit the

fresh topography that is generally associated with kames of Wisconsin

Age. This fresh appearance is the main reason Leverett (1902) believ

ed the kames belonged to deposits of "early1' Wisconsin age. However,

the deposits occur several miles from the Wisconsin boundary (plate I)

and are surrounded by drift assigned an Illinoian age on the basis of

its weathered profile.

The variability in depth of leaching and oxidation mentioned above

illustrates the poor reliability of such criteria for age determina

tion purposes in stratified ice-contact deposits. Removal of weather

ed material (in part) from the slopes would account for the occurrence 99 of limestone pebbles near the surface of the steeper kames. Several of

the large karaes south and west of Hillshoro show significant erosion; they have radial drainage patterns with long spurs extending outward

up to half a mile from the summits. Ravins are cut up to 30 feet deep between the spurs. Calcareous gravel is within two feet of the surface

on the slope of the kames. When fine gravel and sand is the dominant

material forming the karaes, the topography is subdued and they are

covered by ten to 15 feet of leached soil. This indicates that the size

of material significantly effects the resulting topography of the kames.

Color of soil has been related to time in that they become redder

with time. Soils developed since Illinoian time are dark brown to red

dish brown, with hues of 7*5 YR to 51R when formed on topographic posi

tions with good soil aeration and internal drainage. These brighter

hues are characteristic of the karaes in the Illinoian area of Highland

County, while those in the Wisconsin area have hues of 10YR.

Pebble counts taken in several of the kames showed lithologies

similar to those obtained from the Illinoian Danville Till. Total

calcareous rock count averaged 90 percent for 10 sites examined

(Appendix, p. 155)*

Wisconsin

Only a few kames of Wisconsin age occur in Highland County. A

group of kames form the eastern edge of the Mt. Olive moraine near the

mouth of Rattlesnake Creek. The gravel hills are striking when viewed

from the ground moraine near New Petersburg. The highest kame rises to

« 1035 feet which is about 80 feet above the drift to the south or north 100

Numerous erratic boulders up to two feet in diameter, are scattered around the bottom and between the knolls of this kame group suggest ing ice contact origin. Depth of leaching varies from two to five feet. A raoulin kame occurs just south of the Cuba moraine a mile west of New Petersburg (locality B87)- A borrow pit in the west side ex poses the internal structure of the kame (figure 2 3 ). Limestone pebbles appear at the surface on slopes, and the depth of leaching is less than a foot. A flat area on the east side of the kame is leached five feet. Blocks of conglomerate formed by cementation of the kame gravel are scattered along its base.

A large gravel and sand deposit is exposed along the west wall of

Rattlesnake Creek, two miles north of New Petersburg (locality B^7)# and is being actively exploited. Overburden of up to five feet of till

(Late Wisconsin) and four feet of silt have been locally stripped away, but a few complete sections remain. Elsewhere this cover is absent and appears not to have been deposited. Large blocks of cemented gravel are scattered along the base and eastward facing slope (valley wall) of the deposit. Overall the sorting of the material is good, * but there are abrupt changes from coarse gravel to sand. Several erratic boulders are present. Since no matching terrace deposits at similar heights could be found across the valley or downstream, this probably was not a simple valley train. This deposit is interpreted by the writer as a kame terrace. Pebble counts from the gravel show rock suites similar to the Boston Till (see Appendix, p. 15*0• Several

kames are scattered about the Late Wisconsin drift area, but only two are as large as the earlier kame deposits. One kame is just north of 101

Figure 23. A Late Wisconsin kame one mile vest of New Petersburg,

showing internal structure. Blocks of conglomerate in fore

ground are from the kame. Note the thin soil development. 102 the mouth of Hardin Creek (locality B^5). It rises 100 feet above the valley floor, and is leached up to l6 inches. Pebble counts from the gravel show rock suites similar to the Caesar Till. The other kame is atop of the Outer Cuba moraine, one mile north-northwest of New

Petersburg. It consists of several gravel knolls at an elevation of about 950 feet. A small hillside kame deposit, partly exploited in the past for road material, is .locaxed two miles east of Leesburg. Its thickness is about 20 to 30 feet and consists mainly of sandy pea gravel.

Eskers

Two eskers occur within the area of Illinoian drift. They are sinuous ridges composed of moderately well-sorted sand and gravel, deposited so high that Ice must have flanked running water. The lar gest esker is just east of Rocky Fork Lake (locality D^l) and has a length of over two miles. Ohio Route 70 follows the crest of the esker, 1 50 to 80 feet above the surrounding drift. A pit has been opened near the center of the esker and reveals depths of leaching from three to five feet and blocks of conglomerate on the flanks of outer slopes.

The other esker, which is more sinuous and subdued, Is just west of Ohio Route 73* "two and a half miles southeast of Hillsboro (local ity Dll). The esker is slightly over a mile long and rises as much as

35 feet above the surrounding drift at its north end. Exploitation of the gravels near its north end has removed the entire central axis of the esker for over a 1000 feet. Leaching depths are two to three feet and oxidation only slightly deeper in most exposures.

Pehhle counts were taken at both eskers. The esker at locality

D^l has a typical Illinoian composition, high in dolomite and low in limestone. The other esker has an unusual high chert content of 22

percent.

Outwash

Streams fed by glacial meltwater laid down outwash deposits adja

cent to and beyond the margin of the glaciers which invaded Highland

County. Illinoian outwash deposits are by far the most widespread.

Illinoian Extensive outwash terraces are developed along the upper parts of

the valleys of Rocky Fork and its main tributary, Clear Creek. The

terrace tops are from 40 to 60 feet above present stream level and are

highest at the valley edge; they decline towards the stream. Often

the terrace tops merge with the valley edge and no abrupt change in

slope occurs. These extensive terraces are remnants of Illinoian

valley train deposits, which filled the valley from a mile northwest

of Carmel to a position Just west of Hillsboro. Subsequent fluvial

erosion has removed the outwash deposits along the valley axes leav

ing terraces along the sides.

Terrace surfaces in Rocky Fork valley decline eastward from a

height of 1030 feet southwest of Hillsboro to an elevation of 950 feet

in Just over five miles down valley; this is a gradient of 15 feet

per mile. Eastward from here the terrace surfaces gradually decline until at the east end of Eocky Fork Lake, a distance of seven miles, they are at an elevation of 920 feet; a gradient of Just more than four feet per mile. The surface gradient of outwash deposits increase upstream as the source (glacier margin) is approached. Terrace sur faces in Clear valley decline from an elevation of a 1000 feet just north of Hillsboro to about 930 feet seven miles down valley at its juncture with Eocky Fork valley; a gradient of ten feet per mile. The gradient does not increase sharply along the upper portion as in Eocky

Fork valley. The downwasting margin of the Illinoian glacier probably lay just west of Hillsboro, if we may judge from the kames and terraces, during building of the valley trains in Eocky Fork and Clear Creek valleys.

The material of the valley train in the upper reaches of both valleys is gravel, and becomes finer textured down stream. Along Eocky

Fork Lake, sand and pea gravel are the dominant sizes. Depths of leach ing varies from about seven feet in gravels to 15 or 18 feet in sands and silt.

The preglacial Eocky Fork flowed northeastward with its valley located two miles north-northwest of Carmel. Abundant well-log data at the east end of Eocky Fork Lake show that the preglacial valley bottom at this site was at an elevation of about 753 feet (see figure 3, page l6). Illinoian drift filled up the valley and Illinoian drainage was diverted to the south along its present course. Here at Beaver Mill,

Eocky Fork became incised into Silurian bedrock and subsequently has formed what is locally called "Eocky Fork Gorge." Near the mouth of

Rocky Fork erosion of over 100 feet into the Silurian bedrock has form- 105 ed another gorge, in which the "The Seven Caves" developed.

Outwash was deposited in several smaller stream valleys in the county, "but compared to those mentioned above they are small and less significant. Poorly preserved terraces occur along the lower reachefl of the valley of North Fork White Oak Creek, south of Buford in south western Highland County. Better preserved and more extensive terraces occur along the East Fork White Oak Creek in the area of Mowrystown.

Sand is the chief material of the terraces in both valleys and deposits are thin, generally less than 20 feet thick. Leaching is over ten feet

on the few remaining flat areas. In the valleys of Brush Creek and its tributaries in southeastern Highland County, Illinoian outwash ter races are developed 20 to IfO feet above present stream level. For the most part the terraces are narrow and poorly preserved, with few flat terrace tops.

A large plain of thin outwash was deposited in the area from Rains boro to Paint Creek during retreat of the Illinoian glacier. The out wash forms a more or less smooth slope southeastward, and is overlapped

on the north by the Mt. Olive moraine. For the most sand and pea gravel cover the surface; in deep stream cuts gravel is seen overlying till. Well-log data indicate a drift thickness from 20 to 13^ feet.

The preglacial Rocky Fork valley may be located at the site of the well with unusually deep drift of 131*- feet (2.2 miles east-northeast of

Rainsboro). Meltwater flowing south and eastward from the Wisconsin

glacier that deposited the Mt, Olive moraine eroded deeply into this

outwash plain forming the valleys of Puncheon Run and Plum Run,

During retreat of Illinoian ice from its terminal position in Baker 106

Fork, nieltvater flowed southward through the cols between Irons

Mountain, McCoppin Hill, and Long Lick Hill depositing an outwash fan

up to two miles long. From the apex of the fan to its distal edge the

surface drops 80 feet; a gradient of IfO feet per mile. The tributary

valley to Baker Fork between Long Lick Hill and Washburn Hill had out-

wash deposited in a similar manner, but erosion has deeply dissected

the deposit exposing underlying till in most of the area.

Wisconsin

Numerous terraces are developed along the valleys of major streams

whose headwaters drain the area covered by Late Wisconsin drift. The

terraces are at various heights above the present stream levels and

consist mainly of gravel and sand. Depths of leaching range from 28

inches to 75 inches. Commonly a silty surface layer, 10 to 36inches

thick, covers the lower and more level terraces.

In Clear Creek valley south of the Mt. Olive moraine, a poorly

developed terrace system occurs 15 to 25 feet above the present stream

level (Wot-^, plate l). Terrace levels are five to 15 feet above the

present alluvial flood plain, and a gentle slope joins the two levels.

The terraces consist of gravel and sand on which are developed soils

having a silty surface layer and a moderately fine textured subsoil.

Depth of leaching range from 1*7 to 75 inches. These low-level terraces

are remnants of Wisconsin outwash deposited while the ice front was at

the position of the Mt. Olive moraine. Subsequent fluvial erosion has

removed much of the deposit and formed the terraces.

Terraces occur at several levels along the valleys of Rattlesnake

Creek and its two main tributaries, Hardin Creek and Lees Creek. The 107 highest terraces are about 50 to 60 feet above present stream level.

Several of these terraces occur in the area between the mouth of Hardin

Creek and Fall Creek in the valley of Rattlesnake Creek (Wotg, plate

I). One of these high-level terraces is developed one mile east of

Bridges on the south side of Hardin Creek. Another one (Wot3 , plate

I) occurs along the north edge of Leesburg and another a mile to the east, both in Lees Creek valley. Exposures generally reveal that a thickness of less than 20 feet of sand and gravel form the terraces.

The outwash forming the high level terraces was probably deposited dur ing initial establishment of drainage during retreat of Late Wisconsin ice.

A system of intermediate-level terraces (Wotl*, plate I) 20 to 30 feet above present stream level, is developed along the valleys of

Rattlesnake Creek, and its major tributary Lees Creek. Intermediate- level terraces in the valley of Rattlesnake Creek south of the Rees ville moraine merge up valley with the terrace at the mouth of Walnut

Creek and those of Lees Creek. The outwash gravels forming this system of intermediate-level terraces south of the Reesville moraine were de posited while the ice stood at that position.

A system of low-level terraces (Wotj, plate I) occurs in Lees

Creek valley near Leesburg 10 to 20 feet above the present stream level. Lees Creek valley has its headwaters north of the Reesville moraine. Meltwater cut a channel through the moraine northwest of

Leesburg while the glacier stood at a position of an unnamed moraine just north of the Reesville moraine. The outwash gravels forming these low-level terraces were deposited at this time. 108 Rattlesnake Creek cuts through the Reesville moraine; the present stream level is ahout 80 feet below the surface of the moraine. In that portion of Rattlesnake Creek valley north of the distal edge of the moraine, a terrace system (Wotg, plate i) occurs 20 to 1*0 feet ahove the creek. The headwaters of Rattlesnake Creek occur along the distal edge of the Glendon moraine, which is six miles north of the

Reesville moraine. The outwash gravels forming the terraces in Rattle snake Creek, valley north of East Monroe must have been deposited dur ing the time the ice retreated from the Reesville moraine and while it stood at the Glendon moraine.

Several terraces levels occur in Paint Creek valley, which to the east borders the northern half of Highland County. The highest level of sand and gravel deposits occurs from two to six miles south of Green field on the east side of the valley in Ross County. The deposits were mapped by James Petro and others (196T) during the soil survey of the county. Most of these deposits lie from 1*0 to 90 feet above the valley floor. Since deposits at similar elevations on the opposite side of the valley in Highland County do not occur, nor upstream, they probably represent remnants of kame terraces deposited during retreat of Late

Wisconsin ice. Remnants of two levels of outwash occur in Paint Creek valley Just south of Greenfield. The upper level is 1*0 to 50 feet above the level of Paint Creek and forms a terrace nearly a mile long on the Ross County side of the valley. On the Highland County side it (Wot^, plate I) ex tends up the valley of Sugar Run for two miles, occurring 10 to 20 feet above that stream. The lower level of outwash is 20 to 30 feet above 109 the level of Paint Creek and forms an extensive gravel terrace

(Wotg, plate I) at an altitude of 8U0 feet. Since the upper terrace level is absent further north in the valley of Paint Creek and Sugar

Run heads along the Reesville moraine, the outwash gravels forming this terrace were probably deposited while the ice stood at that position. The lower outwash level forms terraces well to the north of the Reesville moraine, and was probably deposited during a stand of the ice margin at the Glendon moraine.

Along Paint Creek below its juncture with Rattlesnake Creek, tiro terrace levels occur above the valley bottom. The lower terrace level is 20 to feet above the stream. The terrace level can be traced up stream to the border of the Late Wisconsin drift at the mouth of Rattle snake Creek. The outwash gravels of this lower terrace were probably deposited while the ice stood at the position of the Cuba moraine.

The upper terrace level is Uo to 60 feet above the present stream level and 20 to 30 feet above the low-level terraces. Depths of leaching are generally about 60 inches. Well-preserved remnants of this out wash form large terraces in Paint Creek valley between The Point and

Bainbridge in Ross County. The outwash forming the upper terrace level extends up Paint Creek valley to just south of the Mt. Olive moraine.

The outwash was probably deposited while the ice stood at that position.

Lacustrine Sediments

Laminated silty clay and silt were deposited as shown in two deep

I 1 1 0 exposures, locality Bj6 and C8 k, in Rock Fork valley. At the vest end of Rocky Fork Lake (locality C8k) is a sequence of strata indicating progradation of a delta into a glacial lake: laminated sediments at the bottom, crossbedded sands middle, and upper most channel gravel vithin sands. At both exposures the laminated sediments extend up to a height of 920 feet. During the early stages of deglaciation of Rocky Fork valley, a proglacial lake probably existed up valley from the site of

Beaver Mill. The proglacial lake was larger than the present Rocky

Fork Lake. The surface of the lake was as high as the bedrock surface at Beaver Mill, which is 920 feet above sea level. The proglacial lake was apparently filled while the valley train was being built up the valley of Rocky Fork and Clear Creek.

Nearly all the material at the surface in Beech Flats consists of silt. Well-log data reveals the silt is generally 20 to Uo feet thick and overlies sand, gravel and till. Several road cuts east and south east of Cynthlana expose bedded silt, some coarsely, laminated. In High land County these silts occur between McNary Hill and Jones Hill, three miles north of Cynthiana. For the most part they form a smooth surface at an altitude of about 960 feet. Locally, subdued karaes rise above the surface level of the flats. The silts were deposited in a proglacial lake which formed in the area as a result of Illinoian ice blocking northward drainage to Faint Creek.

Boulder Concentrations

The distribution of boulders on the surface of the county that are Ill greater than 10 Inches in diameter is shown in figure 2k, Different size dots are used to represent the number of boulders seen on an area of about kO acres. Although a study of the lithologies of the boul ders was not made, it is estimated that over 75 percent are foreign crystalline erratics from Canada. The remainder consists of local bedrock, largely dolomite and limestone. The majority of boulders are lying on the surface or partly covered with fines.

Greater concentration of boulders on end moraines relative to sur rounding ground moraine suggests that the boulders accumulated as ice marginal load, largely supraglacial (Goldthwait, 196 9 ). The distribu tion of boulders shows a definite increase in density on the Reesville,

Cuba (both Inner and Outer), and the Mt. Olive end moraines. Boulders density is somwhat greater along the eastern portion of each of these moraines. This eastward increase coincides with increase roughness of the surface and may in part reflect local removal of surficial flneB, which had partially covered some of the boulders. However, the in crease may reflect an actual greater number of boulders being deposi ted in this part of the county.

Concentrations of boulders on the thick loess covered Illinoian till plains are similar to those found on the relatively thinner loess covered Wisconsin ground moraine. Apparently boulders deposited on the surface were not buried by subsequent loess deposition. Frost heaving and related movements (Bryan, 19^6 ) probably managed to keep the bould ers on top of the surface.

The largest erratic observed occurs on the Mt. Olive moraine, O.85 miles north of Boston. It is a granite boulder eight feet long, three Figure 2*1-. Map of Highland County showing the distribution distribution the showing County 2*1-. Highland of Figure Map 8R0WN COUNTY iX- BROWN O Distal edge of Cuba Moraine Cuba of edge Distal Moraine Reesville of edge Distal Distal edge of Mt. Olive Moraine Moraine Olive Mt.of edge Distal *1-11 Boulders Boulders 1-3 2 Boulders 12+ Illinoian Glacial Boundary Glacial Illinoian and density of boulders. of density and and Wisconsin Glacial Boundary Boundary Glacial Wisconsin and COUNTY per per £.0 ^0 FAYETTE Acres COUNTY 1X2 113 feet vide, of which only one foot is exposed above the ground. The surface of the boulder is stained dark brown from oxidation of its ferro-magnesian minerals.

The largest erratic seen in the area glaciated by Illinoian ice lies on top of Long Lick Hill, 0.8 miles south of Carmel. It is a slightly-gneissic granite boulder having dimensions of 4.5 x 3*0 x 2.3 feet. The surface of the boulder is fresh, with only slight oxidation of its ferro-magnesium minerals.

Directional Indicators

During the present study no scratches, furrows, or grooves were observed on a rock surface. Only a few striae locations have been rec orded by others in Highland County (Leverett, 1902, p. 348 and 424;

Orton, 1870, p. 2 6 5 ). The striae occur in the Late Wisconsin drift area mainly near Leesburg; they were not seen during this study.

The fact that striae have not been found elsewhere certainly does not preclude their presence. In most localities where bedrock is ex posed it is not protected by drift and has been weathered to such an ex tent that striae, if ever present, were long ago obliterated. Two factB probably account for the lack of observable striae, (l) Along the Wis consin and Illinoian drift margins, glacial erosion was very slight. At several sites, a clay rich paleosol or strongly weathered bedrock exists below unoxidized till. (2) In the Caesar and Darby drift area where glacial erosion was more active bedrock exposures are rare because of the thick drift cover. Ilk

A rock drumlin, 1.2 miles south of Centerfield, is the only one well-developed streamlined molded formed that vas observed in the area*

It is an elongate hill about 2000 feet long, 50 feet high* with the typical drumlin shape of an inverted spoon; a thin veneer of till gen erally less than two feet thick covers the hill.

Long axes of drumlins provide good indicators of ice-flow direc tion and striae orientations generally parallel direction of ice move ment (Flint, 1957> P« 66-72). The common direction of the striae loc ations cited by Leverett and Orton is slightly west of south, which is nearly at right angles to the Cuba moraine a few miles south. These orientations agree in part with local till fabrics (see figure l6 , p. •

7l), and the long axis of the rock drumlin; all indicate southward ice movement (figure 2^). BftOWN COUNTY Figure Figure BROWN r 5 2 . Map of Highland County showing location and orientation orientation and location showing County Highland of Map . Orientation of striae striae of Orientation Distal edge of Mt. Olive Moraine Moraine Olive of Mt. edge Distal Moraine Reesville of edge Distal drumlin rock of Orientation Distal edge of Cuba Moraine Cuba of edge Distal moraines end of Crests Illinoian Glacial Boundary Glacial Illinoian of striae, moraine crests, and a rock drumlin. rock a and crests, moraine striae, of and Wisconsin Glacial Boundary Boundary Glacial Wisconsin and ONY AO^S ^ O A | COUNTY FAYETTE / COUNTY 115 glacial history

Pre-Illinoian drift is recognized at the surface In Ohio only in the southwestern corner near Cincinnati (Durrell, 19 6l; Teller, 1970).

Possible pre-Illinoian drift occurs in Highland County at the "base of an exposure, about three miles north of Hillsboro (locality C5l)* The drift in question consists of a till unit overlying a paleosol (four feet thick) that is developed in sand and gravel, which contain foreign crystalline pehhles. Analyses of the till show it is unlike the

Illinoian Danville Drift which overlies it. The lower till may be either an "early” Illinoian or Kansan drift, with underlying strati fied material being older in each case.

Illinoian Glacial Stage

During the Illinoian Glaciation ice advanced into Highland County from the north-northwest. At its maximum advance the ice margin formed an arcuate boundary covering all but the southeastern comer of the county. It trended northward from a mile west of Louden (Adams County) to North Uniontown, then northeastward to the valley of Bakers Fork and into Pike County (plate I). With exception of the maximum advance, the position of the ice front during later phases of the Illinoian Glacia tion is not conclusively known. This is due to a general absence of

116 117 morainic features, caused by erosion and possibly nondeposition. Re- treatal positions of ice fronts described below are based on eroeion- al and constructional features, and on the assumption that such posi tions are grossly similar to that of the maximum advance.

During maximum advance of the Illinoian glacier a major drainage change occurred in the area of Beech Plats, a large lowland area now largely drained by Baker Fork. This drainage change was noted by Fowke

(1 8 9 5 ) and described by Tight (1 8 9 5 ) in some detail. Prior to the ad vent of the ice advance, drainage from Beech Flats was northeastward in to the preglacial Paint Creek. During the maximum advance, ice invad ing Beech Flats from the north blocked its drainage and formed a pro glacial lake (figure 2 6 ). An outlet for the lake was established over a low col, at an altitude of about 960 feet, between Fort Hill and Reeds

Hill at the headwaters of the preglacial valley. Drainage from the lake followed the present course of Baker Fork southward to Ohio Brush Creek.

Ice-contact drift was deposited in the area just east of Cynthian in

Beech Flats during the maximum advance. This stand was probably of short duration, however, as deposits are limited in size and extent.

Following the maximum advance, the Ice front retreated a short dis tance and made a stand of substantial duration. The Ice front extended east-west across the northern edge of the Beech Flats area and still blocked its preglacial drainage route. The ice front was just west of

Cynthlana in the small valleys of Heads Branch and Factory Branch

(figure 2 7 ). Abundant outwash and ice-contact drift was deposited at this time. Meltwater deposited extensive amounts of sediment into the proglacial lake which occupied the area and filled it to an altitude of 118

Boss

County

Highland

County

Pike

County

M a m s

County

Proglacial Lake

Meltwater Drainage

Illinoian Ice Margin

Figure 26. Map of Beech Flats area showing the position of the

Illinoian ice margin during maximum advance. H 9

Boss

County-

Highland

County

Pike

County

Mams

County

Proglacial Lake

Meltwater Drainage

Illinoian Ice Margin

o ij l Illinoian Glacial Boundary

Figure 27. Map of Beech Flats area shewing the position of the

Illinoian ice margin during a retreatal stand. 120 about 960 feet, forming a large flat plain. In places the preglacial valley floor was aggraded as much as 21*0 feet. Local kame deposition formed morainic topography with heights up to !+0 feet above the plain

(see figure 20). Deposition of drift in the Beech Flats area was so extensive that the reversal of drainage became permanent even after retreat of the ice dam. The valley of Ohio Brush Creek iwas the major I ! drainage outlet for meltwater issuing from the ice front in southeast- I ! ern Highland County at this time.

i Following this stand, the Illinoian glacier retreated a short dis-

j tance and made another stand (figure 28). The ice margin extended from li The Point in Paint Creek valley westward along the Mississippian out- 1 liers to Carmel, and then to Marshall. Abundant ice-contact drift was deposited along this margin, largely as kames. j

The north-south trending esker just north of Carmel was probably deposited at this time. The continuation of the ice raabgin south- | westward from Marshall can not be determined with confidence. Only isolated morainic deposits are present and topography i 3 largely bedrock controlled. Probably the margin extended across t1 le headwaters 1 of Elm Bun and then southward towards Fairfax. Outwashj which forms | the terraces along Elm Run and much of Ohio Brush Creek was deposited during this stand. The kame two miles south of Berrysville was pro bably deposited as an ice marginal feature. The ice front had re treated sufficently during this stage to open another drainage out

let, this one to the east along the distal edge of the Mississippian i outliers to Paint Creek. |

As the Illinoian ice withdrew from this stand, a proglacial lake i BROWN COUNTY Figure 28. Map of Map showingposition of Highland County the the 28.Figure BROWN MILES Illinoianice stand. a margin retreatal during Meltwater Drainage Drainage Meltwater Illinoian Glacial Boundary Glacial Illinoian Illinoian Ice Margin Ice Margin Illinoian COUNTY FYTECOUNTY FAYETTE / 121 182

formed in the depression of Roclty Fork valley. The lake stood at an

altitude of about 92° feet. The preglacial valley of Rocky Fork in

large part had been filled by drift and the large esker which crossed

the valley north of Carmel formed the eastern boundary of the lake.

The outlet for the lake was across Silurian bedrock at the south end

of the esker at Beaver Mill. The ice front had retreated to a posi

tion north of Rainsboro, and meltwater deposited extensive amounts of

sediments east of the lake forming an outwash plain. The ice front

made a stand at this position (figure 29). Extensive outwash deposits

rapidly filled the proglacial lake and began building a valley train

in the valley.

Several isolated patches of morainic drift along the northward < sloping surface south of Rocky Fork show that the ice front trended

from northeast-southwest to east-west during this retreatal phase. Ex

tensive ice-contact sediments were deposited in the preglacial lowland

area of Rocky Fork valley just south of Hillsboro at this time. Large

portions of ice were probably detached from the glacier in this area

as it downwasted over the bedrock highs. A large kame terrace built

along the west slope of Clear Creek valley just northwest of its mouth

represents the ice edge in this locality. East of Clear Creek valley

the ice front trended northeastward, north of the outwash plain, to

wards Greenfield and into Fayette County.

Maj or changes in meltwater drainage occurred during this stage of

ice recession. Ohio Brush Creek no longer received meltwater from the

glacier as the ice had retreated west and north of its drainage basin.

The drainage system of White Oak Creek received all the meltwater for 133

FAYETTE COUNTY

0 1 2 -- 4 5 • MILE*

BROWN COUNTY |

Meltwater Drainage

Illinoian Ice Margin

Illinoian Glacial Boundary

Figure 29. Map of Highland County showing the position of the

Illinoian ice margin during a retreatal stand. 12h that portion of the glacier in Highland County vest of the Niagaran

Escarpment. The sands and gravels forming terraces along its valley were deposited at this time.

According to Fowke (1 8 9 5 , p. 1 7 ) , the valley of the present Rattle snake Creek was followed by a preglacial stream to a location about a mile northwest of The Point; from here it continued southeast where it joined the present Paint Creek. Thus the old channel cut across the present prominent loop of Paint Creek north of The Point. Rogers (1936, p. 1 9 ) recognized that the diversion of meltwater around the loop was caused by Illinoian morainic material blocking the former channel. How ever, he believed that the channel was occupied for a time by Wisconsin marginal drainage. According to Williams and others ( 1970) , Illinoian soils are developed in the gravel material occurlng in the channel.

Altitudes of Wisconsin terraces mapped during the present study show that Wisconsin meltwater flowed around the loop.

The preglacial drainage of Paint Creek was suggested by Rogers

(1 9 3 6 ) to have been to the north. He states (page 19 ):

"The fact that the valley widens to the north suggests that the preglacial drainage was in that direction, . . • The widen ing of the valley to the north is even more pronounced, however, from Greenfield northward, and its headwaters converge, in go ing upstream, with those of North Fork of Paint Creek and other southeastward-flowing streams."

Fowke (1 8 9 5 , p. 22) demonstrated that the upper part of North Fork drained northwestward from a col near Frankfort in Ross County. How ever, during this stage of ice retreat drainage was blocked to the north by Illinoian ice and meltwater escaped southward through the bed- t. * rock hills north of the juncture of Rattlesnake Creek with Paint Creek. Thus establishment of the present course southward occurred at this time. Initially, meltwater flowed through the hills at an altitude of about 850 feet, and has since cut a gorge 70 feet deep into Silurian dolomites of the Bisher, Lilley, and Pebbles formations.

Continued retreat of the Illinoian glacier placed the ice front at a position just west of Hillsboro In the headwaters of Clear Creek and

Rocky Fork Creek (figure 30). A stand of the ice front probably occurr ed at this locality as shown by the morainic topography produced by nu merous kames. Continued deposition of outwash during this stand built extensive valley trains in the valleys of Rocky Fork and Clear Creek.

The glacier has retreated north of the White Oak Creek drainage basin during this stand. Meltwater west of the Niagaran Escarpment es caped westward by way of the East Fork of Little Miami River valley.

After this stand the Illinoian glacier retreated northward out of High land County and the subsequent Sangamon Interglacial followed

Wisconsin Glacial Stage

The Altonian or "early" Wisconsin glacier did not advance south into Highland County as had been proposed on the bases of soils found in the county. However, drift believed to represent this glaciation is found at several localities in Ohio (Forsyth, 1961, p. 6l). During the "early" Wisconsin loess was deposited upon Illinoian drift in the county. The loess was derived from outwash that was deposited along the little Miami River to the west. The nearest dated drift (Gahanna

Till with Lockbourne Outwa.sh; Goldthwait and others, 1965 ) suggests it BROWN COUNTY Figure 30* Map of Highland County showing the position of of the position showing ofCounty the Highland Map 30* Figure BROWN J>' r "uf Illinoian Glacial Boundary Glacial Illinoian "uf "Sw. Meltwater Drainage Meltwater "Sw. Illinoian ice margin during a retreatal stand. a retreatal iceduring Illinoian margin ONY | COUNTY Illinoian Ice Margin Margin Ice Illinoian I FAYETTE COUNTY 126 127 is b6,000 to 52,000 years old. A detailed study on the loess deposit in southwest Ohio showed that I* 5 percent of the loess cover of the area was deposited prior to the Late Wisconsin Stage (Goldthwait,

1 9 6 8 ). Loess up to 55 inches thick has been found covering Illinoian drift in the county.

According to Teller {lSSk, p. 61+), "early1* Wisconsin ice extended as far south as the central part of Clinton County. Till from this advance is not known to be present at the surface, but outwash deposits are found along several streams south of the Late Wisconsin border in this county. Since none of the drift assigned to this age has been dated, it may be Late Wisconsin drift and equivalent to the Boston till in Highland County.

Late Wisconsin Substage

The Late Wisconsin glacier advanced into Highland County about 21,

000 years ago and at its terminal position covered the northern third of the county. The ice front extended across the county from just north of Rainsboro on the east to a position three miles south of New

Vienna on the west (figure 3l)» While the glacier stood at this posi tion, the Mt. Olive moraine was built, and outwash was deposited in the valleys of Clear Creek and Paint Creek. The latter valley has deposits extending well into Ross County. During this stand meltwater escaped across the outwash plain near Rainsboro and eroded the narrow valleys of Puncheon Run and Plum Run into the Illinoian deposit.

Following the stand at the Mt. Olive moraine, the ice front re treated northward an unknown distance before re advancing to a new posi- 1 2 8

| FAYETTE COUNTY

0 I 2 j 4 9_• WILES

\ r

BROWN COUNTY |

Meltwater Drainage

— -—I - Late Wisconsin Ice Margin

Illinoian Glacial Boundary

Figure 31- Map of Highland County showing the position of the

Late Wisconsin ice margin during maximum advance,

the stand at the Mt. Olive moraine. 129 tion about 18,000 years ago. At its maximum readvance position (figure

3 2 ), the ice front made a stand during which two essentially parallel belts of end moraine were deposited, separated in places by narrow stretches of ground moraine. Collectively, the moraine is called the

Cuba, and locally distinguished as the Inner and Outer Cuba. The Inner

Cuba probably represents a minor retreatal phase. During this retreat and readvance of the ice margin, a thin blanket of loess, averaging about six inches in depth, was deposited upon the freshly exposed

Boston drift as well as the Illinoian drift to the south.

While the ice margin stood at the Cuba moraine, meltwater escaped southward by way of the East Fork Little Miami River, Clear Creek, Fall

Creek, Rattlesnake Creek, and Paint Creek. Meltwater channels were cut along the margin of the Outer Cuba moraine a mile northeast of New Peters burg, through a segment of the Outer Cuba south of Careytown, and through the Inner Cuba moraine two miles east of Samantha (plate I).

Outwash was deposited along the valleys of the main drainage routes at this time.

Following this stand, the ice front retreated and made a stand a few miles north of the Cuba moraine. While the glacier maintained thiB new position, accumulation of drift along its margin built the Wilming ton moraine. Its form is best developed in Clinton County, and can be distinguished for only a distance of two miles in Highland County. How ever, scattered morainic topography continues eastward paralleling the course of Bridgewater Creek, and probably represents the position of the ice front during this stand (figure 33). The Wilmington moraine probably represents a retreatal position of the glacier that was of BROWN COUNTY Figure 32. Map of Map Highland CountyFigure showing32. positionthe of the Late BROWN Wisconsin icemargin during standat the Cuba moraine. COUNTY Meltwater Drainage Drainage Meltwater Late Wisconsin Glacial Boundary Boundary Glacial Wisconsin Late Ice Margin Wisconsin Late Illinoian Glacial Boundary Glacial Illinoian FAYETTE COUNTY 130 131

I FAYETTE COUNTY

BROWN COUNTY kOM*S

Meltwater.Drainage

Late Wisconsin Ice Margin

Late Wisconsin Glacial Boundary

Illinoian Glacial Boundary

Figure 33* Map of Highland County showing the position of the

Late Wisconsin ice margin during the stand at the

Wilmington moraine. 132 short duration. The major route by which meltwater escaped at this time was by way of Bridgewater Creek to Hardin Creek, then to Rattle snake Creek and finally into Paint Creek.

The Scioto Lohe then made a significant retreat northward to a position at least midway into Fayette County, possibly much farther, and then readvanced to a position a few miles inside Highland County.

The Reesville moraine was built while the ice front made a stand at this readvance position (figure 3*0* Organic material obtained from a silt unit (Melvin Loess?) beneath Darby Drift in Fayette County

(Moos, 1970) dates the readvance at 17,3^0 years B.P. (QWU 2 5 6 ).

Major drainage for meltwater at this stand was by way of Lees

Creek, Rattlesnake Creek, and Paint Creek. Outwash forming many of the low level terraces in these valleys and associated tributaries was de posited at this time. Drift had previously filled the preglacial val ley of Lees Creek northeast of Leesburg and meltwater was diverted south of its former course over Silurian dolomite. Since then a gorge has been eroded into bedrock that is over a mile long and 80 feet deep.

Following the stand at the Reesville moraine loess deposition essen tially ended in this area.

With continued retreat the glacier receded into Fayette County.

It made a stand of short duration about three miles north of the Rees ville moraine. Here it built a low undulating moraine about 20 feet high. The moraine^ is unnamed and trends northwest from western Fayette

County into Clinton County, where the town of Sabina is located on its crest (figure 35)* Meltwater escaped south from the glacier during its retreat and cut channels through low cols in the Reesville moraine just BROWN COUNTY | puD^3

Meltwater Drainage

I —1• Late Wisconsin Ice Margin Late Wisconsin Glacial Boundary

-lu-* Illinoian Glacial Boundary

Figure 3^. Map of Highland County showing the position of the

Late Wisconsin ice margin during the stand at the

Reesville moraine. 13k

Fayette County L*

Clinton

County

Highland

County

Meltwater Drainage Late Wisconsin Ice Margin

Late Wisconsin Glacial Boundary

JU JU- Illinoian Glacial Boundary

Figure 35. Map of Highland, Clinton, and Fayette counties showing the position of the Late Wisconsin ice margin during a. stand at an unnamed moraine in Fayette and Clinton Co. 135 north of East Monroe and northwest of Leesburg. The present course of

Middle Fork Lees Creek was thus established. The low level outwash in

Lees Creek valley was deposited at this time.

Following this stand, the ice front again retreated a short dis tance and took up a new stand, during which the Glendon moraine was built. Meltwater escaped southeast along the distal edge of the gla cier and then flowed south into Highland County through the Reesville moraine following the meltwater channel that was already established

(figure 3 6 ). Since then a gorge, 70 feet deep and half a mile long, has been cut into Silurian bedrock Just southeast of East Monroe.

Meltwater deposited the low level outwash along the upper stretches of of Rattlesnake Creek, Walnut Creek, and Paint Creek at this time.

The Scioto Lobe then continued its northward retreat and made two additional stands while in Fayette County, forming the Esboro and

Bloomingburg moraines. Meltwater from both these stands escaped south by way of Paint Creek, however, separate outwash deposits are not dis tinguishable for them in Highland County. Retreat of the Scioto Lobe north of the Bloomingburg moraine allowed meltwater to escape eastward and westward around Highland County and down the major drainage valleys of the Scioto River and Miami River, respectively.

The Wisconsin glacier subsequently retreated out of Ohio about

12,500 years ago. By 8,500 years ago a warm climate had come to Ohio, for bogs at this time preserved pollen of oak, elm, poplar, ash and maple. 136

Fayette

County

Clinton

County

~ U

Highland

County

Meltwater Drainage Late Wisconsin Ice Margin

_u—- Late Wisconsin Glacial Boundary

-no. MX** Illinoian Glacial Boundary

Figure 36. Map of Highland, Clinton, and Fayette counties showing the position of the Late Wisconsin ice margin during the stand at the Glendon moraine APPENDIX

Section A

Section with Significant Stratigraphies

Distances are straight line measurements from town centers used as reference points. Abbreviations used below for various analyses per

formed on samples are as follows: CM, clay minerals; MA, mechanical

analysis; PC, pebble count; C/D, calcite-dolomite ratio; HM, heavy minerals; F, fabric. locality

Al^ 1.3 miles NNE of Leesburg on west bank of tributary to Lees Creek; Fairfield Twp.

feet description

0.5 silt, dark grayish brown (lOYR h/2)

2.3 till, leached, dark yellowish brown (lOYR l|-/lf)

7 Till oxidized yellowish brown (lOYR 5/*0; MA" Darby I Till (Allfut)

22 till, slump

3 till, gray (7*5TO 5/l)> upper 5” oxidized; MA, PC, Creek (955*) 2.2 miles ESE of East Monroe on north bank of tributary 5 0 ' north of railroad track, and 25* west of Jury Road; Madison Twp.

137 138

feet descriptions

lU till, oxidized, brown (lOYR 5/3)> upper 12” leached;

1 till, unoxidized, dark gray (lOYR ^/l); CM, MA, PC, C/D, HM, F - Darby I Till (A£0ut)

1.5 silt, massive, unoxidized, dark gray (7*5^® M A - (A£0)

. 3 - 5 silt, laminated, strongly oxidized and local cementa tion with liraonite, strong brown (7»5YR 5/8) * 0.5 silt, massive, oxidized, dark brown (lOZR b/S)

0.5 gravel and sand, oxidized, dark brown (lOYR ^/3) 2 till, oxidized, dark brown (lOYR V3); MA, PC, C/D- Caesar Till (AoObt) Ditch (930*)

Locality

A 75 2.1 miles HW of Greenfield on S "bank of Holiday Hun, 800' N of Hew Martinsburg-Greenfield road; Madison Twp.

feet description

13 till, oxidized, yellowish brown (lOYR 5/h), upper 2/5' leached; CM, MA, PC, c/D, F - Darby X Till (AT5ut)

.5 sand, silt, partially leached, dark yellowish brown (10YR k/k)

7 till, oxidized, yellowish brown (lOYR 5A)i MA, PC, C/D analyses - Caesar Till (A75btOx)

6 till, unoxidized, gray (lOYR 5/l); MA, c/D, F - Caesar Till (A75bt) Creek (932')

B9 2.0 miles SW Greenfield on W bank of Duncan Hun; Madison Twp.

feet description

5.5 till, oxidized, yellowish brown (lOYR 5A)

1.5 till, unoxidized, gray (lOYR 5/l); PC, Darby Till (B9) * » 139 feet description

b~6 gravel, well sorted, calcareous Creek (900') Till, unoxidized, dark gray (10YR k/l); Caesar T1117

Locality

B^7 2.2 miles NNW of New Petersburg at gravel pit on W wall of Rattlesnake Creekj Paint Twp.

feet description

0-k silt, leached, strongly oxidized, dark brown (7 »5YR h/k);

0-5 till, oxidized, upper 2.3 feet leached, weakly com pact, brown (lOYR 5/3)5 - Caesar Till

50 gravel, poorly sorted to sorted, calcareous, occasion al bed of stratified silt and/or sand 1 * to 3 ’ thick, upper 5' oxidized; PC - Boston gravel (3^7) Bedrock (820')

B72 0.9 miles SW of Boston on S bank of tributary to Clear Creek, 15’ VT of Carper Road; Liberty Twp.

feet description

12 till, leached 5 ’-6 *, very compact, oxidized yellowish brown (lOYR 5 A )j common vertical joints with clay films, light reddish brown (57R b/6) MA, - PC, Dan ville Till (B72ut)

6-10 sand and gravel, oxidized, thins southward; PC - (B72)

3-6 till, lower 3' unoxidized,dark gray (7 .5YR h/o)} MA, PC, f - Danville Till? (B72bt) Ditch (9^0’)

B76 2.0 miles SE of Boston and E slope of inlet to Rocky Fork Lake, 600' S o f ‘Rittenhouse road; section taken during Park site construction; Paint Twp.

feet description

8 sand, stratified leached, highly oxidized, light yellow brown (lOYR 6/k) and yellowish brown (lOYR 5/6 - 5/8), and reduced, light gray (lOYR l/l), upper 2' is silt, brownish yellow (lOYR 6 /6 ) iko

feet description

7 silt, stratified, leached, strong brown (7 »5W 5/8 ), local cementation with limonite, abrupt change to

25 till, upper 5 ' oxidized, calcareous, remainder un oxidized, gray (2, 5YR 5/o); PC, MA, - B76t, Dan ville Till lake (8 8 0 *)

Locality

B 89 3-2 miles NNE of New Petersburg, 0.1 mile SW of Cedar Run at Ohio Highway 138 road cut, N side, Madison Twp.

feet description

0-13 till, oxidized, yellowish brown (lOYR 5/h), upper 2.5'-3 * leached, top 1.5 silt; MA, PC, c/D, HM, F - Caesar Till (B8§ut)

0 .5-2 silty clay ( "paleosol”), leached, highly oxidized, yellowish brown (10YR 5/6-5/8); Sangamon

5-8 till oxidized, calcareous, yellowish brown (lOYR 5/b), with common, fine and medium distinct brownish yellow (lOYR 6/8 ) and yellowish brown (lOYR 5/8) mottles; MA, PC, C/D, CM, HM, F, Danville Till (B89bt) Road (925*) C^7 2.2 miles SSE Samantha on S bank of tributary to Little Rock Creek

feet description

13 till, oxidized, yellowish brown (lOYR 5A)# upper h-5 feet leached, top 1 .5 ' silt

5 till, unoxidized, dark gray (lOYR ^/l), Picea sp., MA, PC, C/D - Boston Till (C^7)

2 clayey gravel ("paleosol’1) leached, oxidized, yellow ish red (5^R 6 /8 ); Sangamon Creek (960*) C51 2.9 miles N of Hillsboro, 0.8 miles W of U.S. Highway 62 on bank of Clear Creek; Liberty Twp. 141

feet description

0-10 till, oxidized, yellowish brown (lOYR 5/4); MA, PC, C/D, HM, P - Danville Till (C51ut)

2-4 sand and gravel, highly oxidized, yellowish red ( O T 4/8-5/8)

1-3 till, oxidized, yellowish "brown (lCYR 5/4); C/D, HM - Danville Till (C51mt)

2-8 gravel, oxidized, thins eastward

6-13 till, lower 3* unoxidized, gray (lOYR 5/0 ), abundant vertical fractures with dark brown (7 .5YR 4/4) clay coating MA, PC, C/D, HM - pre-Danville (C51bt)

4-5 clayey gravel (’'paleosol”), leached, yellowish red (5YR 4/8); upper I 1 mixed with till, partially cal careous; Yarmouthian?

3 Sand and silt, stratified, oxidized, brownish yellow (lOYR 6/6 -6/8 stratums, yellowish brown (lOYR 5/4) sand stratums, calcareous 0 -5 ’ from top

3 silt, massive, oxidized, light yellowish brown (lOYR 6/4), changing to unoxidized, light gray (lOYR 6/0 in lower 0-5 feet. Creek (950') C58 2.1 miles E of Boston and 0.1 miles S of U.S. Hwy. 50 OB bank of Blinco Branch; Paint Two.

feet description

1-2 silt, leached

6-10 till, leached 36" to 80” below surface, oxidized, yellowish brown (lOYR 5/4), pH 4.9 at 2” below sur face; MA, PC, C/D, HM, P - Boston Till (C58ut)

3-5 clay loam ("paleosol”) leached to 3 ' sandy loam, partially leached another 2' (Sangamon), gradually changing to . . .

6-10 gravel and sand, well sorted, oxidized; PC - Danville gravel (C5 8 )

6-2 till, unoxidized, dark gray (lOYR 4/l), (upper 0*5'- 1 ' oxidized, thickens westward at expense of overly ing gravel, Picea sp.; HI-1, MA, PC, C/D, CM, P -

I lh2

feet description

Danville Till (C58bt)

C8*f ^.0 miles ESB of Hillsboro in road cut on E side of "Airport" road, 0.1 miles north of Ohio Hwy. 12k; Liberty Twp.

feet description

0 -l8 sand, leached, well sorted, cross-bedding in lower 6 * highly oxidized, yellowish red (57R k/6-k/Q)

5-7 silt, and clayey silt, laminated, upper 2 '-3 f ox idized, calcareous, dark brown (lOYR k/3), lower 3’-V unoxidized, dark gray (lOYR U/l); MA - (C8U)

3-30 till, unoxidized, dark gray (lOYR U/l); (thickness southward at expense of overlying material) MA, PC, C/D, HM, F - Danville Till (C8U)

C95 ^.2 miles E of Eainsboro to The Point, then 1.5 miles N to the S wall of Paint Creek valley at site of Paint Creek Reservoir Dam excavation; Paint Twp.

feet description

10-25 gravel and sands, leached, highly oxidized, yellowish red (5YR 5/8 ) and strong brown (7 »5TR 5/8 ) r 2-7 till, leached, dark brown (7*57R k/k)

1 day, residual soil, yellowish red (5YR 5/8) Bedrock (8001)

0.5 miles WSW of Rainsboro, 0.1, miles south of U.S. Hwy. 50, on S bank of Puncheon Run; Paint Twp.

feet description

5-7 silt, leached, dark brown (7 -5YR k/h) to yellowish brown (lOYR 5/6); locally lower 1' is laminated and calcareous.

0.5 sand, leached, dark brown (7-57R ^ A )

1 gravel, calcareous, yellowish brown (lOYR 5/6 )

k till, calcareous, dark gray (7 .5YR k/0 - 10YR k/l); upper and lower 5" oxidized, yellowish brown (lOYR 5A)j C/D, F - Danville Till? (C99ut) 1^3 feet description

1 sand, oxidized, light yellowish brown (lOYR S/k)

1.3 till, oxidized, dark brown (lOYR lf/3)

7 gravel, poorly sorted, oxidized, yellowish brown (lOYR 5/6 - 5/8); PC -Danville gravel (C9 9 )

2 till, center 1¥ unoxidized, gray (lOYR 5/l)> very pebbly; PC - Danville Till (C99mt)

2 gravel, unoxidized

1-2 silt, laminated, unoxidized, dark gray (lOYR k/l); MA. - (C99) Creek (890') till unoxidized, dark gray (lOYR V ^ ) : C/D - Danville Till? (C99bt)

1 0 0 ' to 500 east of above location on south bank is gravel terrace•

feet description

25 gravel, leached 55" to 80" and dark brown (7 -5YH oxidized below to yellowish brown (10YR 5/8); PC analysis - Danville gravel (C99tr) Creek (890*)

D 8 0.2 miles N of intersection of U.S. Hwy. 62 and Ohio 138 (Leesburg) on west side of road cut; Fairfield Twp.

feet description

25 till, upper 1 0 ' oxidized and yellowish brown (lO¥R 5/if) till; MA, PC, C/D, HM, F - Caesar Till (D8ut) change abruptly to . . .

■ if till, oxidized, yellowish brown (lOYR 5/*f - 5/8)> lower 1* unoxidized; CM, MA, PC, C/D, HM, F - Caesar Till (D8bt)

3 sand, oxidized Ditch (1000') bedrock 2 f-3f below

D35 1*8 miles HU of Hew Petersburg, 500f HE of road on S bank of Big Branch; Paint Twp. 144

feet description

3 colluviura, oxidized

3 f gravel and sand, leached

6 ’ till, unoxidized, dark gray (2.5Y 4/0), Picea sp.; MA, PC, c/D, HM, F - Caesar Till (D35) Creek (855')

D3& 2.9 miles SE of Samantha, 900' E of Ohio Hwy. 138 on south hank of Fall Creek; liberty Twp. * feet description

0-12 till, oxidized, yellowish brown (lOYR 5 A)* leached 2.5’ CM, MA, PC, C/D, HM, F - Caesar Till (D36ut)

0 .5-1 rubble and gravel, partially leached, clay accumula tion in upper 3"> abrupt change to . . •

8-10 till, calcareous, yellowish brown (lOYR 5 A)* lower 2' to 3" unoxidized gray (lOYR 5/l)> small pieces wood common, Picea sp,; CM, MA, PC, C/D, HM, F - Boston Till (bjSnrt)-

5-6 silt, leached, ("paleosol"), upper 6 " dark yellowish brown (lOYR h/h / 3A)> lower silt grades to brown (7.5YR 5A)j m ~ Sangamon (D3 6 )

3-4 till, lower I 1 unoxidized, all calcareous; CM, MA, PC, C/D, HM, F - Danville Till (D36bt) ; Creek (1020')

D39 2.7 miles M E Hew Petersburg in cut bank on S side Cedar Run, 150' S Rowe Rd.; Madison Twp.

feet description

0-l4 till, oxidized, yellowish brown (lOYR 5A )

14-22 till, unoxidized, gray (lOYR 5/l), Picea sp.; MA, PC, F - Caesar Till (D39) Creek (860') 1^5

Section B

Sample Locations

All* see Section A

A56 1.3 miles ESE East Monroe in N "bank of railroad cut 300' W of Dunn Rd., elev. 9^0', Madison Twp.

A 60 see Section A

■ A75 see Section A

A 8l 1.6 miles W of Greenfield in N "bank of road cut along Ohio Hwy. 28; elev. 930'# Madison Twp.

B9 see Section A

T£ik 0.2 miles W of Samantha in N bank of road cut along Hightop Rd; elev. 1150*, Penn Twp.

B31 2,2 miles SSW Leesburg in road cut along U.S. Hwy. 62,0.2 miles SW Leaverton Rd; elev. 1 0 6 0 , Penn Twp.

B^5 1 . 6 miles SSE Centerfield, in S side of kame,0.2 miles W of Cope Road; elev. 9301, Fairfield Twp.

Bkj see Section A

B62 1.5 miles SW Rainsboro in road cutalong Rittenhous'e Rd., 0.2 miles W Ohio Rt. 70; elev. 920', Paint Twp.

B76 see Section A

B 87 1.1 mile W New Petersburg in W side of kame, 500* N of Petersburg Road; elev. 1050*, Paint Twp.

B 88 2.0 miles ENE New Petersburg, in road cut along Paint Creek Rd., 0.2 miles W of Ohio Rt. 753; elev. 870*, Madison Twp.

B 89 see Section A

Clj-7 see Section A

C51 see Section A

C5k if.7 miles NNW Hillsboro in W bank of new road cut along Ohio Rt. 73; elev. 1 0 9 0 ', Union Twp. Sample Location

C55 3*1 miles KB Hillsboro In W tank of Little Rock Creek, 300’ SE of barn; elev, $k0f, Liberty Twp,

C58 see Section A

C80 3*5 miles SSW Buford in Ebank of North Fork White Oak Creek; elev. 925 f> Clay Twp, C8l 3.5 miles SSE New Vienna, in W ditch in road cut along Ohio Rt. 73, 0.1 mile S of Powell Rd.; elev. 1150# Union Twp.

C8lf see Section A

C92 1.5 miles S Sugar TreeRidge in E bank of road cut along Ohio Rt. 136; elev. 1010', Concord Twp.

C93 1.6 miles HE Mowrystown in W bank of tributary paralleling Ohio Rt, 321; elev. 9 6 0 Concord Twp.

Cyk 3.0 miles NW New Market in gravel pit just S of juncture of Holladay Rd. with Ervin Rd.; 1000* elev., New Market Twp

C99 see Section A

D6 1*3 miles SW Fairview in quarry 400’ S of Roush Rd.; elev. 1060', Hamer Twp.

D7 1.8 miles SSW Gath in E bank of Flat Run; elev. 9^5** Clay Twp.

D8 see Section A

D9 1.6 miles E Rainsboro in S bank of road cut along U.S. Hwy. 50; elev. 880f, Paint Twp.

DIO 2.0 miles NNW Rainsboro in N bank of road cut along Deer Park Rd., 0.1 mile E of Plum Run; elev. 9^0', Paint Twp.

Dll 2.0 miles SE Hillsboro in gravel pit of esker, 0.2 miles W Ohio Rt. 73; elev. 1000’, Liberty Twp.

Dl^ miles NNW Hillsboro in W bank of road cut along Ohio Rt 73, 0.1 mile N of Crosen Rd.; elev. 1090', Liberty Twp.

D15 2.5 miles NW Willetsville in bottom of Newly Rd., 0.1 miles S of Fettering Cem.; elev. 1080', Union Twp.

Dl6 k.l miles NNW Hillsboro in W bank or road cut along Ohio Rt 73, 0.2 miles S of Crosen Rd.; elev. 1030’, Liberty Twp. lVr

Sample Location

D19 0,3 miles W The Point in N bank of road cut along U.S. Hwy. 50; elev. 8 ^ 0 Paint Twp#

D20 0.6 miles W The Point in road cut 0.2 mile N U#S# Hwy 50; elev. 890’, Paint Twp.

D23 see Section A

D25 0*9 mile N Samantha in E bank of road cut along U.S. Hwy# 62, 0.1 mile N of Pall Creek; elev# 10^0f, Penn Twp.

« D31 1*7 miles M U Boston in ditch on E side of Point Bd.; elev. 1020*. Liberty Twp.

D32 1.0 miles SW Bridges in bank of tributary to Big Branch, 200* S of farm pond; elev. 980', Paint Twp.

D31* 0.8 mile E Bridges in S Bank of Hardin Creek; elev. 8 8 0 Fairfield Twp.

D35 Eee Section A

D36 see Section A

D39 see Section A

D^O 1.5 miles W Leesburg in E bank of South Pork Lees Creek; elev. 1 0 2 0 Fairfield Twp#

Dlf-1 2.0 miles S Eainsboro in gravel pit of esker along Ohio Rt, JO; elev. 990f> Paint Twp.

J)k2 0.7 mile N East Monroe in cut bank on E side Eattlesnake Creek; elev. 960f, Madison Twp# 1*8

Section C

Results of Analyses

Clay Mineral Analyses

Pebbles in samples were removed by using a number 10 mesh sieve.

About 60 grams of the fine earth fraction (< 2mm) passing the sieve was used in the clay-size fraction. Despersion was accomplished by adding approximately 2 grams of NagCO^ and 60 grams of the material to a 500 ml bottle, filling it half full with distilled H^O and shaking for 15 hours on a recipicating shaker at 120 cycles per minute. The sands were removed by using a number 300 mesh sieve and the clay fraction separated by an automatic fractionator described by Ruttledge, and others (1967).

Clay ( < 2 microns) was flocculated with NaCl and then magnesium saturated, washed, and decanted as follows with the aid of a centri fuge:

1) three times using 1 normal MgClg solution

2 ) once using distilled water

3 ) once using half water, half methanol

!*■) once using a 9 0/® menthanol solution

Then the magnesium saturated clay fraction was dispersed in distilled water and plated on porous ceramic plates under suction to form oriented clay aggregates. Three plates were prepared for each sample.

One plate was leached with a 10$ aqueous solution of ethyleneglycol and placed in a saturated ethylene glycol atmosphere untilprior to x-ray analysis. It was then heated at lj-0° C for several hous to re- 149 move excess ethylene glycol from the surface. The other two samples were air dried at room temperature for 48 hours. One was x-rayed at room temperature, heated to 400° C for two hours, cooled to about

100° C and x-rayed again. The other sample was heated to 550° C for two hours, cooled to room temperature and x-rayed. During x-ray analyses, each ceramic plate with its thin film of oriented clay was placed on to the Norelco diffractometer (Type 12045 full-wave generator), with settings of 35 Kv and 15 milliamps and using Cu

K alpha radiation. Samples were scanned from 2° to 32° at the rate of

2° theta per minute. A diffractograra was obtained for each run using a linear plot mode. From the diffractograms peak areas were measured for various x-ray diffraction peaks using a planimeter.

The following ratios and area factors were employed for comput ing peak area ratios and clay mineral quantity estimations:

Illite i The area of the 10.0 - 10.2 A peak-ethylene glycol (E.G.) treated clay. O Montmorillonite: The area of the 16.7 - 18.0 A peak for the E.G. O treated clay divided by 4 times the 10 A peak area of the same treat ment O Vermiculite: The area of the 14.0 - 14.7 A peak for E.G. treated clay , o minus the area of this same peak for the 400 C heat-treated clay; O the area difference in these two peaks divided by 2 times the 10 A peak area of the E.G. treated sample.

Chlorite: The area of the 14.0 - 14.7 A peak for the 400° C heat- Q treated clay divided by 2 times the 10 A peak area of the E.G. treated clay. 150

Kaolinite: The area of the 3.5 A peak for the 1*00° C heat-treated

clay minus the area of this same peak for the 550° C heat treatment; % 0 the area difference in these two peaks divided by k times the 10 A

peak area of the E.G. treated clay. 0 Quartz; The area of the 3.3 A peak of the E.G. treated clay minus

3/J4- the peak area of the 10 A peak of the same treatment; The differ-

. o ence in areas of these two peaks divided by 4 times the 10 A peak

area of the E.G. treated clay.

To compute relative clay mineral percentages the sum total of all

ratios (illite ratio equal to l) is divided into the ratio obtained

for each mineral species. 151

TABLE 11 RELATIVE PERCENT OF CLAY MINERALS IN THE LESS THAN 2 MICRON FRACTION OF TILLS AS DETERMINED BY X-RAY DIFFRACTION. RATIO OF PEAK HEIGHTS FOR 10 AND IK ANGSTROM AIR-DRY AND ETHYLENE GLYCOL TREATED CLAYS

Relative Percent P

* « • a Q C D • • • ! w Number o

Darby I Till A60ut 82 3 1 10 k .62 • 35 A75ut 79 3 16 0 2 4*6l • 39

Caesar Till DSbt lk 2 k 12 8 .36 • 30 D36ut 75 2 1 11 11 .^2 •31 D^2btox 7k 2 15 0 9 .32 • 1*2 Dtebt 77 3 0 7 13 • 31 • 20

Boston Till C58ut 2 0 78 56 39 3 1-33 C8l 62 7 30 0 1 1 .00 • 69 DIO 58 k 36 0 2 1.09 • 80 Vlk *3 1 ^ 39 0 k 1 .22 1 . 00 D15 55 k 35 0 6 1.23 •86 D31 55 8 35 0 2 1.52 I .03 D 36 mt 55 9 13 8 15 .90 m 55

Danville Till B89bt 70 k 19 0 7 4►79 »51 C58bt 77 6 0 ik 3 •35 D 6 77 k 17 0 2 >6k • D9 82 2 1 11 k ► 55 •k2 D36bt 79 2 1 7 11 I► 30 • Ik TABLE 12 PARTICLE SIZE DISTRIBUTION OF BULK SAMPLES

Percent by Weight (pebbles on total sample; Till sand-silt-clay on less than 2mm fraction) Peb Sand Silt Clay Unit bles and • i 1 i ' i » d tA Jj h a d O O 0 0 O IA ITNCVl OJMD CO a ! « * O O O l T \ ITS CM H OJ H O ■+£ 0 0 LPv OJ 9 0 1 • • • • • • • O m • • Sample CU OJ H HO OO OO OO -P 0 0 V

Darby I Till A5 6 21.0 5-7 5-* 5-5 7-5 7.8 31-9 53-6 . 14.4 A 60 ut 17-7 6.1 6.4 7-7 8.5 7.4 36.1 52.6 11.3 A75ut 10.8 5.6 5.7 7-2 8.5 8.3 35-3 47-5 17-2 A81 10.6 5-5 5.7 6.6 7.7 7.2 32.7 50.6 16.7 tesar Till Al4ut 15-7 5.2 5-3 6.2 7.1 7.3 31.1 51-9 18.0 Al4bt 13.5 4.4 5.0 6.4 8.1 7.9 31.8 51-5 16.7 A 60 bt 12.3 4.6 4.9 6.3 7-1 6.2 29-1 52.6 18.3 A75btox 13-4 6.3 6.2 7.7 8.6 8.0 36.8 42.0 21.2 A75Ut 11.9 ' 5.6 5-4 6.6 8.5 9.1 35-2 50.1 14.7 B24 7.3 3.1 3.6 5-2 7-4 7.3 26.6 50.9 22.5 B31 6.6 4.5 4.6 6.7 9-2 9.0 34.0 48.2 17-8 B89ut 19. 4 8.4 8.5 ll.l 12.2 6.9 47-0 43-5 9.5 D8ut 11.7 4.8 5.0 6.7 8.3 8.1 32.9 51-6 15.5 D8bt l4.l 6.8 7-5 9.8 11.3 9-8 45.2 42.3 12.5 D25 9.6 3.7 4.0 6.2 8.8 8.6 31-3 47-5 23.2 D 32 5.2 2.1 2.7 3.7 5-1 5-0 18.6 54.4 27.0 D34 9-1 4.4 4.6 7-5 10.7 9-7 36.9 44.1 19.0 D35 10.3 4.6 5-3 7.7 9.7 8.8 36.1 48.4 15-5 D36ut 11.5 4.0 4-5 6.5 8.9 8.2 32.1 49.6 I8.3 D39 11.8 5.7 6.1 8.5 10.6 9.4 40.3 46.2 13-5 D40 12.3 5.7 5.6 7-9 10.0 9-9 39-1 45.9 15-0

Boston Till C47 5-9 2.6 2.9 4.8 7-1 7.8 25.2 51-9 22.9 C54 6.6 2.8 3-4 5-2 7-4 6.9 25.7 54.5 19-8 C58ut 7-2 3-1 3-6 6.3 8.8 8.8 30.6 52.9 16.5 C8l 6.1 3-7 3-9 5-4 7-8 8.1 28.9 50.7 20.4 DIO 8.4 4.7 4.9 7-6 10.6 10.7 38.5 43.0 18.5 d i 4 5-1 3-1 3-7 6.2 7-8 7.2 28.0 51-0 21.0 D15 6.0 3*4 3-7 5-1 7-2 7.2 26.6 52.7 20.7 D31 5-7 3-4 3-9 6.4 8.5 8.1 30.3 50.3 19.4 D36mt 4.6 2.3 3.0 5-4 8.2 8.4 27-3 51.2 21.5 Till Peb Sand Silt bles Unit l i I irv U\c3 I o o in tr\ cu cvi VD & o LA OJ CM A HO • * • • • * * » £ ir\ cm CU H o o o o o o Sample cu ■p

Danville Till B72ut 10.0 *f.7 M * 6.2 6.9 5.7 28.if 5^.9 16.7 B72bt 6.5 2 .6 . 3.3 .5.0 6.6 5.3 22.8 59.0 18.2 B76 22.6 7.1 6 .if 7.3 9.5 8.5 38.8 If 8. If 12.8 B89bt 18.0 6.3 6.3 8.6 10.3 8.0 39.5 If If. 8 15.7 C51ut 17.1* 5.8 6 .if 9 .2 10.3 8.8 if0.5 lf6.5 13.0 C58nit 19.1 5.8 6.1 8.0 10.1 9.8 39.8 lf7-6 12.6 C58bt 20.1* 5.7 6 .if 9.1 10.2 7.2 38.6 1*9-7 11.7 C80 17.2 6 .0 7.2 8.If 8.6 7*5 37-7 if if. 5 17.8 c 8^ 22.0 7.5 8.1 10.0 10.6 8.6 if i . 8 lf2 ,6 12.6 C 92 1^. 3 5.6 6.0 8 .0 9.6 8.9 38.1 1*5*9 15.0 C93 11.8 lf.9 5.3 7.0 9.9 9.7 36.8 51.7 11.5 C9^ 13.2 7 .6 ' 7.7 13.0 15.0 9.7 53.0 lfO.O 7 .0 C99ut 11.3 if. 6 if.U 5.9 8.3 8.0 31.2 1*9-3 19.5 C99bt 7.7 3.2 3.0 if.i 5.2 5.1* 20.9 57.0 22.1 D 6 10.5 5.2 5.8 7.5 8.8 8.3 35.6 1*7.9 16.5 D7 8.6 5*3 5 A 7.1f 9.2 8.3 35.6 1*9.9 Ilf. 5 D9 18. if 7.1 7.7 11.0 12.3 9.2 If7.3 1*3.7 9.0 di6 20.9 7*5 7-7 9 .6 10.5 10.6 1*5-9 if if.6 9.5 D23ut 16.7 if. 6 lf.9 7.3 9.0 8.0 33.8 lf8.5 17-7 D23bt 8.5 3.9 if. 6 7*5 9-3 8.2 33.5 1*9.5 17.0 D36bt 18. if 6.9 7.8 11.5 llf.l 9.9 50.2 37.8 12.0 pre-Danville till C51bt 13.8 5.2 5.5 7.1 9.0 8.0 3^-8 1*6.5 18.7

Lacustrine deposits A 60 1.9 8lf.l llf.O C8k 0.6 81.1 18.3 C99 0.9 78.6 20.5 D23 if.3 63.8 31.9

Pluvial deposit D 36 0.1 2 .1 lf.8 8.3 8.1 2lf.lf 5lf.2 21. If 154

table 13 TABULATION OF PEBBLE LITHOLOGIES OF TILLS AND GRAVELS IN HIGHLAND CO,

.d Till Percentage o

»d (U a) 3 Unit a d 2 d o dd * o a s u d 1 Sample i? .d 5 •d •H •3 o S 3 o CQ CO u 1-1 Q Pt £* O

Darby I Till A5 6 6 ' 5 18 71 .25 89 AoOut 3 6 16 75 .21 91 A75ut 0 lif 18 68 .2lf 8!f A8l 5 5 17 . 73 .23 90 B9 7 8 19 66 .29 85

Caesar Till Al4bt 7 10 12 71 .17 83 A6obt 6 if 18 72 .25 90 A75bt 4 6 12 78 .15 90 B24 8 24 22 tf6 .if 8 68 B31 3 3 31 63 .**9 94 B88 11 6 17 66 .26 83 B89ut 9 13 20 58 .35 78 D8ut 5 7 22 66 .33 88 D8bt 11 5 31 53 • 59 8lf D25 if 12 22 62 .36 84 D32 7 5 20 68 .29 88 D34 8 10 22 6o .37 82 D35 12 lif 1 30 ifif .68 74 D36ut If 10 26 60 .if 3 86 D39 lif if 12 70 .17 82

Boston Till C47 8 16 34 lf2 .81 76 05^ 7 13 29 51 .57 80 C58ut 11 26 33 30 1.10 63 C8l 12 10 32 lf6 .69 78 DIO 6 13 51 30 1.70 81 D15 if 2lf 34 38 .90 72 D36mt 2 20 if8 30 1.60 78

Wisconsin gravel B45 7 3 2lf 66 .36 90 B47 8 0 39 53 •74 92 B87 7 3 28 62 .*5 90 155 g Unit nd 0) i and ■pW

Danville Till B62 9 10 21 6o • 35 81 B89bt 9 13 17 61 .28 78 B72ut l* 12 16 68 .2lf 81* B72bt 2 6 12 80 .15 92 B76 6 3 27 6lf .lf2 91 C51ut 6 20 lb 60 .23 71* C51rat 8 2 18 72 .25 90 C55 9 1* lif 73 .19 87 C58mt 10 3 lif 73 .19 87 C58bt 5 7 12 76 .16 88 C80 3 l* Ifl 52 .79 93 081* 7 2 20 71 .28 91 092 5 2 28 65 .1*3 93 C93 9 4 31 56 • 55 88 C99«t 6 8 lif 72 .19 86 C99mt 12 6 22 6o .37 82 D6 11 5 2 6 58 .if 5 81* D7 6 5 1*9 bo 1.22 89 D9 9 8 13 70 .19 83 di6 5 ll* 32 lf9 .65 81 D23ut 6 10 29 55 .53 81* D23bt 7 3 27 63 .1*3 90 D36bt 6 8 22 6lf •31* 86 --Danville till C51bt 2 5 50 !f3 l.l6 93 Linoian gravels B72 5 11 20 6lf .31 81* 051 7 3 18 72 .25 90 058 5 2 20 73 .27 93 C91* 5 5 30 60 .50 90 C99 l* 3 27 66 .1*1 93 C99tr 10 if lif 72 .19 86 Dll 2 8 38 52 - .66 90 D19 5 5 13 77 .17 90 D20 1* 3 32 6i • 52 93 DM 5 3 20 72 .28 92 156

TABLE l1*. TABULATION OF CHITTICK-GASOMTERIC ANALYSES FOR WEIGHT PERCENTAGES OF CALCITE AND DOLOMITE IN THE LESS THAN 2mm SIZE FRACTION OF TILLS IN HIGHLAND COUNTY

Percent by Weight of 2mm Fraction rH—1 *rj-P gj j§ Sample CaC03 Calcite Number Calcite Dolomite Equiv. Dolomite

h A60ut 8 .1+ 21+.8 35.2 .34 to AT5ut 9.6 19.2 30.4 .50 § A 8l 8 .1+ 22.1 32.3 .38 ft * A60ut 5.1 l6.4 22.9 .31 A75bt0x 7.6 l4.8 23.7 • 51 A75Lt 6.7 15-5 23.4 .43 B31 1+.8 15.7 21.8 .31 ^ B89ut 9.8 19-5 31.0 .50 D8ut 8.8 19.1 29.4 .46 1 D8bt 12.6 19.7 34.0 .64 5 D25 6.6 14.6 22.4 .45 D32 13.2 17.5 32.2 .75 D34 6.3 13.6 21.0 .46 D35 8.2 16.9 26.6 .49 D36ut 10.7 18.2 30.4 • 59

CU7 6.7 13.0 20.8 .52 C54 6 .1+ 13.8 21.4 .46 C58ut 6 .1+ 11.7 19.1 .55 & C 8l 7.1 14.3 22.6 .50 § DIO 6.1 14.1 21.4 .43 | Dl4 , 3.0 10.4 14.3 .39 D15 ' 6.0 11.2 18.2 .54 D31 i+.o 11.4 16.4 .35 D 36mt 8.7 13.1 22.9 .§6

B89bt 7.1 16.9 25.5 .42 C51ut 11.9 19.5 32.9 .61 C51mt 10.1 19.4 31.1 .52 C58bt 11.9 20.0 33-5 .60 « C8>f 12.5 21.4 35.7- .58 9 C92 11.6 19.6 34.1 .59 § c^3 11.7 19.3 32.7 .60 § C99ut l+.l 15.7 21.1 .26 o C99bt 13.1 19.4 34.1 .68 D9 11.1 19.9 32.7 .56 D23ut 12.3 17.2 31.0 .72 D36bt 10.8 19.7 32.1 -55 pre-Danville till C51bt 11.9 20.0 33.5 .60 TABLE 15 TABULATION OF HEAVY MINERAL ANALYSES OF THE VERY FINE SAND FRACTION (0.062 - 0.125mm) OF TILIS IN HIGHLAND COUNTY

Heavy Minerals (percent)

Till Opaque Transparent and Translucent •P P P r 0 o (U O *H 0 0 p f-t -P Unit and 0 •d +> 0 0 0 0 O -p 0) Garnet P •rt -P 0 -P ft d •H -p 0 r-i *H 'd £ 0 cu to 0 0 •H H O irt 0 *rt 0 0 ■p d P r-4 rH p P O •p 0 ■8 ■8 p p H a • r i O 0 d •rt s S d p •rt B •H ft 0 •p *d 0 0 d b3 0 S a m p l e d «P -P •P p •c

Darty 1 T in A60ut 11 11 1 3 5 10 15 kk 7 8 4 5 2 89 2.70 A75ut 23 2 25 2 2 9 14 23 37 k 2 1 2 2 75 2.36 A 8l 23 5 28 4 10 8 18 31 6 5 3 4 1 1 72 3-14 Caesar Till A£obt 31 2 33 3 6 13 19 32 3 3 2 2 1 2 67 4.47 B31 22 2 3 27 5 11 11 22 32 3 4 1 5 1 73 3.31 B89ut 30 2 32 1 6 11 17 37 2 2 4 l 2 2 68 5.00 D 8ut 15 8 23 1 1 7 15 22 34 4 4 6 3 1 1 77 2.86 D8bt 29 9 3 4l 2 1 9 8 17 24 2 2 3 2 4 1 1 59 4.42 D24 31 31 2 1 10 15 25 28 2 2 2 3 1 2 1 69 1.97 D32 28 15 43 1 6 9 15 26 3 3 2 2 2 3 57 2.54 D34 32 19 1 52 1 2 6 7 13 20 1 2 2 2 3 1 2 48 2.91 3)35 37 14 51 1 3 6 13 19 l4 3 3 3 2 1 49 1.91

D36ut 20 11 1 32 1 9 19 28 25 4 2 4 1 1 2 68 2.49 3.57 Heavy Minerals (percent)

Transparent and Translucent Till Opaque •S a oj o O «H O 0) C to Jh o3 o a a V*0) o •HO 0) 3 •H § * s 3 •h a -h ft +9 ft3 o j OJ 3 o3 h h 43 a 1 a (0 •H 43 43 ■rt H Sample i—1 >J £ -P ■s o 5 a | o « a & s >» a ft ft 49 ■8 u 01 ft E O +9 a ft O +* 43 cti +9 eJ ■O 43 0) 0J IQ O + 9 Boston Till C$h 18 10 1 29 2 3 5 11 l6 30 6 5 1 2 k 2 71 4.50 C58ut 21 2 23 1 k 7 12 19 32 5 7 3 1 2 1 2 77 2.50 C8l 24 2k 1 k 3 17 20 32 3 7 2 1 1 1 3 76 3.08 D10 2 6 2 28 2 6 17 23 30 k 3 1 2 1 6 72 1.8k Dl4 33 33 3 3 7 18 25 25 1 2 2 1 2 1 2 67 2.20 D15 22 22 1 1 9 11 20 33 3 7 2 1 2 78 2.97 D31 27 27 6 15 21 37 1 1 2 1 1 1 8 73 2.53 D 36mt 26 8 34 1 1 5 15 20 27 k 2 1 1 4 2 3 66 3.28 Danville Till B89bt 45 45 1 5 18 23 15 1 1 1 2 2 3 55 2.10 C51ut 31 k 35 1 1 6 16 22 27 2 5 1 2 2 3 65 3.06 C51mt 30 2 32 2 2 10 13 23 27 4 3 2 3 1 1 68 3.15 C58bt 33 5 3 4l 3 1 5 8 13 31 3 1 3 2 1 59 3.91 CQk 28 6 2 36 4 7 10 17 26 3 4 3 3 1 3 64 4.42 C92 26 12 2 to 1 4 4 14 18 24 4 2 2 2 2 60 3.45 C93 18 12 1 31 2 1 7 9 16 36 6 2 3 1 2 69 3-41 D9 32 13 1 to 1 2 9 11 25 4 2 4 2 2 3 54 2.20 D23ut 22 k 26 3 1 7 19 26 35 2 1 2 1 2 1 74 2.65 D36bt 29 12 41 1 1 7 19 26 25 2 2 2 1 4 59 4.56 pre-Danville till C51bt 30 14 3 47 9 16 22 2 3 3 53 3*54 BIBLIOGRAPHY

American Society for Testing Materials, 19^4, Grain-size analysis of soils, D422-63 in Procedures for testing soils, p. 95-106

Andrew, R. W., JR., i9 6 0 , The relationship of natural drainage and the clay mineralogy of Miami and Brookston soils in central Ohio: M.S. thesis, 15 figs., 9 tables, 6l p.

Bidwell, 0. W., 1949, A study of clay minerals of soils in the Miami catena: unpub. Ph.D. dissertation, Ohio State Univ., 12 figB., 5 tables, 77 p.

Bowman, R. S., 1956, Stratigraphy and paleontology of the Niagaran series in Highland County, Ohio: unpub. Ph.D. thesis, Ohio State Univ. 13 pis., 1 fig. 340 p.

Bryan, K., 1946, Cryopedology, the study of frozen ground and Inten sive frost action with suggestions on nomenclature: Am. Jour. Sci., v. 244, p. 622-642

Chamberlin, T. C., 1883, Preliminary paper on the terminus of the second Glacial epoch: Third Ann. Rept. U.S. Geol Survey, p. 291-402

Dixon, W. J., Massey, F. J, Jr., 1957* Introduction to statistical analysis: McGraw-Hill Inc., Hew York, 488 p.

Dreimanis, Aleksis, 1 9 6 2 , Quantitative Gasometric determination of calcite and dolomite by using Chittick apparatus: Jour. Sedimentary Petrology, v. 32, p. 520-529

Dreimanis A., Reavely, G. H., Cook, R. J. B., Knox, K. S., and Moretti, F. J., 1957* Heavy mineral studies in tills of Ontario and adjacent areas: Jour. Sed. Petrology, v. 27, p. l48-l6l

Droste, J. B., 1956, Clay minerals in calcareous till in northeastern Ohio: Jour. Geology, v. 6 7 * p* 187-190

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159 l6o

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Williams, N., McLoda, N., and others, Soil Survey of Highland County, Ohio: Ohio Dept, of Natural Resources, and Soil Conserva tion Service, (unpublished) EXPLANATION nn Alluvium

Wtr Terrace erosionol, cut In outwash or bedrock

Wot Outwash preserved os terraces SUBSCRIPT DESIGNATIC

Drift related tp specific moral Wk Kame 1 CD Mt. Olive 11] Cuba ■ , Wg Ground moraine s Wilmington 0 Reesvllle 0 unnamed moraine In Clinton W e End moraine and Fayette counties, betwee IIZ|3|4| -the Reesvllle and . Gtendon moraines wt Till □□□□ less than'five feet thick 0 Glendon COUN

Itr Io Outwash preserved as terraces or outwash plain

II Lacustrine

lie Ice contact stratified drift kame, kame complex, kame terrace and esker PLATE I

.1 • EOLOGY OF HIGHLAND COUNTY,

Geology by Theodore E. Rosengreen 1970

GLACIAL FEATURES’ SCALE

Boundary of a mapped deposM

CONTOUR INTERVAL

2 0 F E E T

Limit of a significant' advance or readvance DATUM IS MEAN SE of the.Ice front

BSCRIPT DESIGNATION Limit of a major (stage) glacial advance slated tp specific moraines:

Meltwater channel gton ■■V.

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Itr Io Outwash OHIO preserved as terraces or outwash plain

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