SDMS US EPA REGION V -1
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THE GLACIAL GEOLOGY OF CHAMPAIGN COUNTY, OHIO
A Thesis Presented in Partial Fulfillment of the Requirements for the Degree Master of Science
Michael John Quinn, B.S.
The Ohio State University 1972
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M.A. Deft. ,f Ge,l.,y Frontispiece .
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I wish to express my gratitude to the Ohio Division of Geological Survey for financial assistance during the field investigation. Additional thanks go to Mr. Marcus EoyesL and Mr. John Muskopf for their aaiuL^tance in laboratory analyses* . > To ny adviser, Dr. Richard P., Croldthwait,, ray oincero thanks for .continual guidance durj.ns all facets 01" this study. I wish to express appreciation, to Dr. Georgs Moore and Dr. Sidney V/hite, both of 'Dhe Ohio State University, for help in bhe final preparation urid critica reading of the aanuscript. Special appreciation, is extended to my vrife, Anne, for her help in prep TABLE OP CONTENTS Page FRONTISPIECE...... ,.*...... i ACKNOWLEDGMENTS...... ii LIST OP TABLES...... v LIST OF ILLUSTRATIONS...... v Plate...... v Figures...... 7 INTRODUCTION...... 1 Regional Setting...... 1 Previous Investigations...... 5 Economic Geology...... *...... 6 Purpose of Investigation...... 7 Procedures...... 5 Bedrock Geology...... „„ 10 PrC'glacial Surface and .Drainage...... 15 H OF GLACIAL 'FEATURES...... 16 Introduction...... 16 Miami Sublobe End Moraines...... 18 Springfield Heraine...... 16 West Liberty Moraine .«>...... 25 .Farmersvilie Moraine.*..„...... » 25 Hianii Sub lobe Ground Woraino,,«,..., ...... 27 Scio?:o Sublobe End Moraines*....,«...... » 29 Cable Koraine .....,r.«>.,.*,.*...... 29 Powell Moraine•,.><...«...... »»...... •. 31 iii Related Outwash Deposits. ...*<,....,....,«,..,. 33 Kennard Outwash...... c.^...*...... ?3 Urbana (Intermediate) Outwash...... 36 Mad River Valley Train...... *. 38 Ice Contact Features...... 39 Kames...... 39 Eskers...... a...... 43 Boulders...... 43 Lacustrine Deposits...... Directional Indicators...... Striae...... Till Fabrics...... Surf aco Coils...... '1S Till-soil Associations. „.*..*...... «. 49 Loess Cover.,...... ,....,..,.,».... 53 Buried "Soils"...... 5* HESULTS OP FIELD AND LABORATORY ANALYSES...... 57 Stcnecoiinbs...... »,...*.»....<.. 57 Galcite-Dolonite Percentages..^...... 59 Grarxulometric Distribution,...... 6"; DISCUSSION AND CONCLUSIONS...... 6?. GIACIAL HISTORY...... P...... o? « T^O""•M-'TV T"' KFPrJJJ^IX ...... ,.....>.».<.^....o.*.lr.r..*t.>. / f Sample Locations,„.,..,...... »...... >.. 77 EIBLICGRAPHY...... ,.... - 91 LIST Oi1 TABLES Table Jt-age 1 Stratigraphic sequence of rocks forming the bedrock surface of Champaign County, Ohio...,.,. 10 2 Significant characteristics of the major till-soil associations in Champaign County..... 51 5 Stonecount percentages of tills and cutwash.... 83 4 Chittick Gasoinetric limestone and dolomite percentages...... 87 5 Particle-size distribution of bulk samples, 39 LIST OP ILLUSTRATIONS Plate Plate Page 1 Map of the glacial deposits of Chanpaign County — in Docket Figure Page 1 Map of Ohio showing location of Champaign County...... 2 2 General geologic map of Champaign County...... 12 3 Bedrock contour map of Champaign County...... * 14 4 Principal drainage stagas of west-central Ohio. '15 5 Depth of carbonate leaching in Champaign Goun?jy...... 22 6 Three-component diagram show mean particle- sise distribution for tills. ....*...... 32 7 Photograph of Xennard Outwash and Cable Moraine 3^ v figure Page 8 Photograph of Kennard Outwash at the Cable Pit of American Aggregates Corporation...... 34 9 Photograph of buried kame and kettle topography east of Springhills, Ohio.,..„... 42 10 Photograph of kames north and east of Mingo. 42 11 Boulder concentrations in Champaign County.. 44 12 Photograph of boulder concentrations on the Farinersville Moraine near St. Paris...... 4? 13 Photograph of lacustrine plain northeast of Urbana...... 47 14 "Rose" diagrams of till fabrics...... 50 15 Map of Cable Moraine chowing crests...... 66 16 Map of sample locations in Champaign County. 78 1? Map of stonecovnt locations in Chanpaign County...... ,...... <...... 84 Segional Setting Champaign County is in wsst-centrsl Ohio (Fi;_;ure 1); Urbana, the county seat, is about 40 miles wsst-northwest of Columbus. The county of approximately 4-33 square miles lies entirely within the glaciated Till Plains section of the Central Lowlands Physiographic Province (Fenneman, 1958). Relief ranges from smooth very gentle slopes en the outwash terraces to gently rolling hills on the end moraines. The highest elevation in the county is 1J35 feet on a crest of the Cable Moraine near Middletown iu northeastern Champaign County. The lowest elevation, 950 feet, is on scroll terraces of the Mad Rive,? in south- central Champaign County near where the river enters Clark County. The major, central, area of the county is drained by the Ifed River and its tributaries, The southerly flev/ing Mad River enters the Kiemi River at Dayton. Streams in the eastern quarter of the county flow easterly or south- easterly as part cf the Scioto P.iver drainage basin. In a narrow portion of western and northwestern Champaign County, o'3vsr3..L streans drain westerly or northv/estorly as niiuor tributaries of the Miaai Kiver. Chaapai^n County lies entirely within the deciduous forest reg.ion of the Eastern Central States. The original vfiKOtaticn is clashed undsr ^oree priia:.'-y gr-cups: oak— Figure 1. Map of Ohio Showing Location of Champaign County. hickory, beech.--iiis.ple, and oak-maple; ana two secondary groups: 3v:anp forest and grassland ("tfitchie aud Fcv.ell, '1971)« The county has an average s^nnual precipitation of 5Q inches with a humid, temperate., continental cli^are. Previous Investigations In 1835 J. L. Riddell, a medical doctor, was appointed by the Ohio Legislature to determine the feasibility of a geologic survey o£ the entire state. During nis prelim- inary investigation, Riddell (1837) visited Champaign County. He noted "... partially rounded blocks of primitive stone" ("bowlders")» the calcareous nature of the r.oil. and the warer quality and flow rate of ^evei-al s>prince;. Hi; was especially intrigued by an exanole of or^aj'ic asL-isr;- ance in the mechanical breakdown of bedrock ac tie not so. "... the roots of herbs and tree" insimiat-Ln^ cho^sclve.s into every chink and crevice?, seem to pry the pieces asunder and contribute to their complete disinto-jration," Franklin Hill (1878) reported "The Drift overlies the v;hole country, srrceptinsr those lowlands where i^s own v/aste and the sv-amp growth have covered it v/ith a.lltiv.iai soil." Hill noted that the "bowlde.;"-." and gro.vols varied litholop;ioal.ly and attributed this variation to a differ- ence in source area and transport mechanism. Us v;as the first to report on the general geomorchology of the entire county. In his report on the glacial deposits ox the mid- western and eastern United States, T. C. Chainberlir. (1835) observed and mapped the moraines of the "Scioto and Maumee Glaciers" including the interiobata area of Champaign and Logan Counties. He speculated on the relative ages of some outwash deposits in noting that scnae gr-aveis can be traced to specific ice border positions. Orton (1838) discussed drift thicknesses taken from logs of test boles drilled in studying the Trenton Lime- stone. One hole near St. Paris encountersd 530 feet of drift without reaching bedrock, the maximum depth of drift then reported ia Ohio* Orton. felt that the driller- had ?ncide-r.ly found an ancient channel of the Miami "River. The most comprehensive report on the glacial deposits of Champaign County is Leverett's monograph (1902) in which he discusses the deposits and associated glacial features of the Miami and Scioto Lobes. Leverett, relying heavily on topography and morphology, recognized the composite nature of the moranic belt of eastern Champaign County (Cable Moraine) without distinguishing individual \ Moraine members. He noted the thickness and structure of the drift ar-u. some interrelationships between the moraine.s and outwashes. Fox* nearly half a century following Leverett, Ohio geologists turned their attention to bedrock geology and little v.'cxs addsd to the knowledge of the glacial geology of Champaign County. Stauffer (1909), Carman (1927), and Busch (1959) each produced a bedrock nap that included. Champaign County. Forsyth (1956), in her dissertation on the glacial geclogy of Logan and Shelby Counties, mentioned cany glacial deposit's in Champaign County. Sciying- heavily on soil profiles, she attempted to correlate moraines between the Miami and. Scioto Lobes through the nose of the interlobate area in Logan County. Reconnaisance mapping by Goidthwait during the fifties resulted in a brief discussion and map of the glacial deposits of Champaign County in an unpublished Ohio Division of Water report by Feulner (I960). Gyldthwait treated selected areas of the county in more detail in many field conference guidebooks (Goidtb'.vait, 1952, 1955 > 1962). The Pleistocene deposits of adjacent and associ- ated counties v/ere discussed in s. series of Ohio Division of Water Bulletins (Goldthv/ait, 19^3, 19.50, 1952). Janssena (1964) contributed substantially to rhe Jcnowledge of thn glacial stratigraphy of the county. He used geophysical methods, well logs, and drill hole data to establish sfcratigraphic relationships in chree, east- west-bands acrcns the central portion of the county. Bitcbie and Pov/ell (19V'1) incliide a brief discussion of the glacial deposits of the county and their role as parent materials for aoi.l formation. b Economic Geology The glacial deposits of Champaign County provide a strong foundation for the local economy* Glacially derived sand and gravel are the pritnsry aquifer materials that yield excellent water supplies to most of the county. Till and outwash represent parent materials for very rich soils. These soils, coupled with the abundant v.'ater supply, establish a sound base for agricultural productivity. Sand and gravel for aggregate is presently being extracted from the Kennard Outwash two miles west of Cable { and from Urbana and Mad River Oucwashes .just southwest of 5 i Urbana. Both operations are owned by the American 1. Aggregates Corporation and consist of dragline or shovel * extraction and primary sorting and crushing. The bulk I materials are then shipped to Columbus or Dayton for secondary processing. Unprocessed sand and gravel that is i used directly as road fill in being, exploited from buried kames south of Springhills, and locally from gravels exposed under thin tills on t;he moraines. Scone quarrying for building scone nnd aggregate took place sporadically on a limited scale until th° 1920's. Qu;irryin3 operations centered two miles northeast of Urbe.na in southeastern Salem Toiinship. New exposures of Tyrnochtea dolomite in the Cable Pit of the American Aggregates Corporation offer the possibility of future o.uarryiag fcr cmshable aggregate materials. Several minor industries enjoyed limited success in the middle to late 19th century, but have long sines dis- appeared. Local clay accumulations provided the basis for numerous potteries that supplied brick, drain tile, and housewares. Peat v/as used locally as a fuel, and marl from swamps in kettle holes was once a minor source of lime. Purpose of Investigation Devonian bedrock of the Bellefontaine Outlier under- lies eastern Logan County and extends southward into northern Salem, Wayne, and Rush Townships of Champaign County. This bedrock and topographic "high" was of sufficient elevation to impede the advance of the conti- nental ice sheet. This impedenco resulted in the splitting of the ice flow, forming the Scicnc Sublobe oast of the outlier and the Miaai Sublobe to the vest. Extensive deposits of both sublobor; are present in Champaign. County, thus a. unique opportunity exists fox- determining correlative ice margin positions between the sublobos. This deternvination can be based, on location of ice contact features and associated outwesh deposits, occurrence of Loess with consequent variations in soil developr.ant, boulder concentrations, stonecoiurts. ana position of moraina crests, Knowledge gained fro^a this study can be employed to interpret better the glacial history jiot oruy of Champaign County, but of all sreas in 3 which deposits of eicher sublobo exist;. Procedures Field Methods Most of the field investigation was carried out during the summer of 1971« Every road in the county was examined and stops made at nearly every road cut. Areas not readily accessible by road were visited on foot. The field area v/as revisited in late fall and early spring to plot boulder occurrences and map moraine topography. Crops and foliage present during the sumser and early fall hinder a comprehensive survey of these features at those times. A soil auger was used extensively in areas of limited expo-suites. Several hundred auger borings were made to delineate depth of silt cover, depth of leachinp. p?.rsnt materials, and the soil profile. Samples for laboratory analysis v;ere obtained by augerin^s and hand sampling in road cuts and pits. Febbie counts were made at many exposures of till and gravel. One hundred washed, one to three--irich pebbles '.vere broken and identified at- each site. This procedure £ivss a consistent rock identification, especially in separating limestone and dolomite. Till fabric was determined at 1? locations by measur- ing the preferred long axis orientation direction of 55 to 50 scenes greater than one inch long. Only atones with a length-to breadth ratio of greater than 3-0 were neas-jrod. Drake (19'S1^) has shovm than an A:B axial ratio of ^'!.7 coupled v;it.h JO to 100 azimuth measurements gives a high degree of reliability in till fabric determinations. Mapping was done on 7.5 minute topographic maps (fJ, S. Geological Survey, 1960-1961). Plate 1 is a composite of these naps reduced to half size. Quadrangles used in mapping Champaign County are: Port -Jefferson, DeGraff, North Lev/iscurg, Beliefontaine, Fletcher, St. Paris, North- ville, Kingscreek, Milford Center, Christianburg, Thackery, Urbana West, Urbana East, ana Mechanicsburg. The "Soil Survey of Chaapaign County, Ohio" (Ritchie and Powel.l, 1971) proved very beneficial in determining parent roaterial.s, associated wit;h specific soil profiles. Office and Laboratory Procedures Over 600 v/ater-v/ell logs and several bedrock tes» hole records, which are on file with the Ohio Division of Water, were analyzed for information concerning the thick- ness and nature of the glacial deposits in the county. Particle-sise distribution was determined for 51 till samples. 'j?he total sand fraction was removed by wet sieving and then separated into fractions by dr^ sieving. Hyd.rcajoter analysis was used to quantitatively determine- the silt (0.062 - O.OG2ism) and clay (<0.002nm) fractions according to procedures described in American Society for Testing Materials (1964, p. 95-106). I Chit-tick gasometric determination of the calcite and dolomite- percent ages of 61 till samples were ?iade. Samples were ground to <0.07*Ham and analyzed in accordance with techniques described by Breiraanis (1962). Bedrock Geology Bedrock is exposed in only a few localitiesjLn....north- central Champaign County, owing to the extensive cover of glacial drift. Although the bedrock surface is composed of rocks ranging from Upper (?) Ordovic.ian through Upper Devonian age, exposures are limited to Upper Silurian and younger formations (Table 1). 1.. Stratigraphic sequcmoe of rocks forming t.be bed- rock surface of Champaign-County, Ohio. Series Fomia/jjion a-cal ur.ar^ccer Uppsr Ohio Sh. Black to brov/r* pyritic shale. Lower Columbus Ls. Light gray to brown thin bedded to ua.scive nodular c:ierty f o G s ilii' e.rous Is, Cayugan Bass Island Gp. Liu;hfc graj' 'to t^n Tynochtee Dol. ripple--roar>ed del, Gr-eonfield Del, v;ith shale pc.rtiags. Sh^le cino. Ii.mo.it:one. Clu.nt.on Brassfield Ls. 5'ine silty pyritic glaucon.itic Is,/dol. Richmond Soft ca3.car?;ous Maysville bluisn shales vrith Grclovicic.ii Eden tnin inteiobeddcd undiffer- entia^ed. Figure 2 is a genera 1 ^f-olo.sic map of Cbanpaxg-n County. Ordovician rocks coaoir:^ -prir.arily or so.i'S; shales interbedded vith fcnin. fosGilirorous argillaceous Lime- stones. 1'eo't drilling has shovn. that these rocks fern the bedrock surface only in the deeply incised, buried valleys of the preglacial Teays Hiver snd its tributaries (Norris and Spicer, 1958). Silurian rocks, consisting of limestones, dolomites, and thin shales, form the bedrock surface of most of Champaign County. Lower Silurian (Clinton) bedrock is exposed only in the buried prerrlaoial valleys. K.iagaran (Middle Silurian) rocks are prodoiiinant on the crest of the Cincinnati Arch in the v/catein portion of the county,, ?his arch is a northv;ard~plunr/;ir..^. broad regional ilexturv whose axis traverses Chaniiaiyn County from the diddle; of Jackson Township to the northeast corner of Adams T-ov;n- ship. Rocks on the east flank of the arch dip 15 feet per mile easterly, whereas the dip on the western'flask is northwesterly at five feet per m.ile (Stout et al., 'i9--'-?). Lfppor Silurian (Cayugan) rocks fcnr the bedrock surface of most of eastern Chairpaigri County. Exposure? of Devonian bedrock are limited ars^lly to rorthern wa;yne anJ. i'Jciiem Tov/nships in the norch-central portion of the county. These shales and limestones represent i;he southerruaost linit of t.he Pellc-fontaine Outlier. Champaign County, Ohio. Silurian rugan) dolomite Idle Siiurian i.Kiar : and limestone ddla jJe<.rc iniosrtone ia\\ shales Preglaciai Surface and Drainage Figure 5 is a bedrock contour nap of Champaign Coumrv modified from Norris and Bpicer (1953). The map shov/s a preglacial surface of moderate relief except where the Teays drainage system was deeply entrenched. The Teays is a general term introduced by Tight (1903) and later modified by Stout et al. (194-5) to indicate "....the ;vorlc of streams during that general period of erosion before glaciation. " The Teays River system may have had its headwaters in the Piedmont Province of North Carolina and Virginia. The main Teays River floifed northwesterly across West Virginia and Ohio (Figure 4-A). Near the vie st- ern border of Ohio, in northern Mercer County, the Teays River swung to a more westerly coarse. Horberg (1950) <"-nd V/ayne (1956) have traced the buried course of l-he Teays Valley across northern Indiana and central Illinois and indicated that the drainage reached the Gulf of Mexico erabayoient by way of the ancestral Mississippi Valley. Test drilling in west-central Champaign County indicates a Teays stream gradient of approximately one foot per nilf? (Norris and Spiocr, '1955). This is consistent v; ifti values derived frcia southern 0:i.Lo ar.d V/e&t Virginia (Stout et al., 194-5). A lev streaa gradient in a deeply incised, broad, flat- floored valley coupled with well- rounded bordering upland;.-:, indicates that the Teays ranage system hr;/t r-f/y.cued ^-o^n.D.fpi'.c maturty before 5. Bedrock Contour Map cf Champaign County, Ohio (siodifieci from Norris and Spicer, 1953) I-ro'oahle course of buried Teuyss Valley Contour Interval 100 feel I I i'igurs 4-. Principal Drainage Stages of West-Central Ohio, Champaign County indicated by stripes, I I A. Teays Stage Drainage (after Stout et al.t I I I B. Deep Stage Drainage (after Stout et al., I Generalised. Present rainage •If;.- onslaught of continental glaciation. In the Teays Valley and ibs tributaries sour/n. of the glacial boundary in south-central Ohio, are deposits of finely laminated clays known as the Minford Silt. Accord- ing to Morris and Spicer (1953), the Teays drainage cycle was brought to a close in the early Pleistocene when the Teays system was damned by pre-lllinoian ice. This resulted in flooded valleys in which the Minford S.ilic was deposited. The damming initiated the Deep Stage drainage which developed in topographic and structural bedrock troughs (Figure 4-B). Old Teays valleys were also incorp- orated, either in noraal or reversed directions. Clay- rich sediment that quite possibly is aii equivalent of the Hinford Silt has been discovered through test drilling in a deep buried va?tley in western Champaign County (ilorris and Spicer, 1958). Description of Glacial Features Introduction Deposits of three distinct glacis-ticns, Kaasan (?), lilinoian, ar-d V/isconsinan, blanket v;<5stern o.r/3 central Ohio. "Due i:o a more subaued bedrock topography in v;estarn Ohio, as contrasted to eastern Ohio -and Pennsylvania, the continental ic.s sheets penetrated to more southerly oosirions in the wastoi-n portion of the state. Bedrock d.iffi?r-jrices gave ris-2 lo conypicuous lithologic «nd 17 texvaral variations in the resultant deposits. Due to che dil'i'srencas in parent materials, the consequent soil variations have proven to be an important tool in delin- eating 3;-re and compositional differences in the glacial drift of Ohio. Deeply weathered tills that are restricted to inter- stream uplands near Cincinnati and large crystalline boulders in north-central Kentucky have been speculated to be deposits of the earlier, Nebraskan glaciation* Ecvrever, stratigraphic similarities with exposures in Indiana. (V/ayne, 1958) suggest the till to be of Kansan age. These Xansaa deposits have been described by Durrell (1961) a:id Toller '1964-). The lone crystalline erratics further south in Kentucky remain an enigma, •In Ohio, Illinoian drift is exposed in a continuous belt south of the I'/isconsinan glacial boundary except in the area of the Killbuck Lobe in northeastern Ohio. This drift is generally blanketed with loess, probably of Wicconsrmaa age (Go3.dtiiwait, 1963; Goldthwait et al.? 1965)• D'ollov:ing a problematic "early" Wiscor.sinan glacia- "cicr., v;hich now seems not to have aclv?.:-.ee soutii of Piqua or ColunbuH (Dreirnonis and Gcldthwait, in press), "late" //iccon:>.inar; glaciers deposited the drift v:hich mantles :2GS:; of glaciated Ohio, including Che.rvpaign County. Bvblobe End. Moraines Springfield Moraine The north-south morair.ic band of high huraniocky topography that crosses Champaign County through Salen and Urbana Townships is known locally as the Springfield Moraine (br.o-.vY-, 1y-:-3). 'Hhi.3 easternmost end moraine 01 the Miami Sublobe is continuous except near Kingscreek where youngsr outwash and the present drainage have cut across it. Local relief on the moraine is moderate. Moraine elevations range from 1230 feet in north-central Champaign County to approximately 1100 feet near th.? Clark Cc\mty line. The Springfield Moraine consists of thin sill veneered on thick deposits of bedded outwash. ri.v:.e " V:':;:lnuit:/ ;.4'Vi S'.irface elevation of the buried outv/ash. ssovn by •..'i'.tcr- i v;ell lojra ?.nd rjeopbysical ce&sv~*eF;erxb£?. (Jsnsseiis, '•/^• !-)1 coupled with, stonecoun't: data :Lyi',-.i.cates that •J'..-.:- out^'j^ih is a ouj?i3cl continuation of the K-->£;-n:-ird :'>.,i;v.vasli. Best ex- posures of tbc- moraine stratigraphy aiv o? the: proxiT.al or western cide of the end morai.no. Gravel pits af.cl road out 43 on the western Ef-r^in of the moraine alonrr Dallas Road, Iiickory Grove P.cad, Ohio Rout- 2 ^'.-^ and Hsnnonit>: Church P.oad, all sxpose four to seven feet of till cverl thick, stratiiisd saucl and gravel. In a burial, cre-^.cn \r- the Ur-b^r.u Ssvnivtiry Landiill I 1.6 miles northeast of Urbana, four fee* of till, leached co 30 inches, overlies eight feet of finely laminated silt and clay. This unit is not present in gravel pits 0.75 miles further south on the end moraine. I'he laminated unit lies approximately 15 to 20 feet higher tliaa the lacustrine plain located, cne mile to the east. It appears this unit resulted from sedimentation in a local pond, perhaps a kettle., prior to or during formation oi' the end moraine. Beneath the clay-silt laminations is thick, coarse gravel interpreted as the Kennard Outv/ash. Elevation of this gravel surface is approximately 114-5 feet. J'xnryyT-s (';-;::-!-) described a reddish leached aons? a oossi'ole pa.lecs-~l. in the upper 1> inches o.f the buried gravel. A sisrij.ar trench exposure today does not exhibit this r'bur;.3d soil". Over 75 water-well lo^s in that portion cf the Spring!iold Moraine south of the Kings Cre:-]c Valley indicate that the Kennard level outv/ash continues benoatn tae eru? moraine but with ?. surface that dscre&aes in eiovation xvesterJ.y and southerly. In southern LTrbana 'rcvmchip, the elevation of tho buried gravel surface varies from an averag-3 of 1090 feet on the eastern ed;Te of the norains to 1050 feet on the western vaaryin. Taa chiclcneso or t'c.a overlying till rangers from five to 2[~, Teen without a noticeable trend, In central Gaarnpaign Bounty (northern Urbana Tcv/nship -and southern Sal en Tcv,;:ship ; the buried gravel suri'ac-''- r. I opes vresterly .f.'.'on- -:-.ppro>:vriacc'.v 114-5 to '10^0 feet. Jyi^i^ a"orao;e cl^rations, l;a.c ^ouuhv/^rc ^ of the buried Kennard Outwash is approximately eight feet per raile. The younger Mad River Valley Train has a southerly gradient of about ten feet per mile. Well log data indicates "clay" (till) beneath the upper Kennard Outwash in almost every hole. The elevation of this "claytr unit varies between 1060 and 1110 feet. The "clay" averages 20 feet in thickness and is always underlain by pre-Kennard bouidery gravel. Well data from over 25 sites in that portion of the end aoraine north of i the Kings Creek Valley indicates Kennard Outwash beneath six to 20 feet of till. Elevation of the buried Keruiard surface decreases southerly with a slope of about 14- feet per mile, Sparcity of v/ell data along the western edge of the end moraine makes east~west gradient deter- minations difficult. Road-cut exposures in the noi'th- cervtral part of the county, along Kenhon.ite Church Hc.ad and Kanaga Road, indicate the Kennard Outwash surface lies about 20 feet lower beneath the western portion of the end noraine as compared to more easterly areas. As in the southern portion of the moraine, an average of 18 i'eet of "clay1' lies beneath the buried Kennard. Outwash at elevations betv/een 1075 and 1150 feet. This "clay" is also underlain by sand ani gravel. Well log Saleci 29 a"c the .junction of Kanaga and C-ama Parrs Roads indicates 20 feet of till over- lying 20 fast of coerse Kennard gravel. Beneath the out- wash is 18 feet oC "clay" (till). Similar stratigraphies :•»*• ^; li are displayed in well records from drillings ,lu3u north ol" Kingscreek. In several deep wells throughout the end moraine, a third, buried "clay" zone is found with a thir. (three to five feet) sone of gravel separating it from the next higher "clay". Quite likely this could represent oscillations of the ice margin during formation of the till and thus both the lower two tills and the interbedded out- wash are contemporaneous. Twenty-five augerings indicate a cean depth of leach- ing of 29 inches for the Springfield Moraine. Depth of leaching values are very similar for all tills in the cov.nry ' ""'i-Tut-ft 5)» Hitchie and V-owell •;''i7v1.' u?scl auger- ir*.£ c;o deteiTaire deptl- of carbonate leaching s.\. hi.nJroc's of s;.t:-;? in Cb-aapylTn Covr.r;ty* .Depch to carbonates varies oetween 18 and 50 inches for the Micmi, Brooks ten, Cel.ir.a and Crosby Soil Series which include Kost soils developed in end moraine ls, Numerous kettles are locat'ed in the end niorainet especially in the northeastern quarter of Urbana Tov/nship, tv/o miles east of Ui-bana. 'The concentration of Icettio.s ir, atti'ibuted to t'he ic,^ marginal, iiatoriobats posioior: of the Kftnn^rd Outv/aoh in which the kettles developed. The keti;le3 were formed by the wasting I-Iia^i oublo'ce and were nhus concentrated along the v/estern margin of the t\roa. The overlying till :;orsr did r.ot obliterate, LOG At J CO. w.xvV CLARK CO Depth of leaching of carbonates in inches in Champaign County. but ,1ust covered and subdued, vho izettle roporvraphy, Sirv3rai kettles display a relic, easterly sloping, drainage channel on the eastern edge of the depression. This indicates that ice remained intac- and buried in the out- wash and did not completely meir until tno ovc-riyinf- tk.in till was deposited. West Liberty Moraine Pour isolated conspicuous ridges thatr extend from the western limits of Urbana northward into Logan Count;' comprise the West Liberty Moraine (Gel:!r.;,v-r.:t; '1^55). Augerings and exposures indicate that the s:ean depth of carbonate leaching is 30 inches throughout ths end moraine. Like the Springfield Moraine, this end. nicr-ainc ic ccn;pocci of a thin till covering thick deposits o.f bsddsd outv/ash* Stonecovjits and v/sll lcg.= cu£ges~ tbat this underlying1 sand and gravel i>3 continuous v/ith and at the levol of tho Urbana or Intermediate Outwash, which borders the eastern margi^•^ n of the and sioraine.f ••/ater-v/ell data from ths "island" of ^he end moraine jus^ northi-.rest of Urbana shoxvs chat 0 to 55 feet of till overlies the Urban-?. Outvash surface that ranges in elevation between 106.5 and 101^ feet. The irrc^ulai- gravel surface nlops.o slightly to the south avid v/oat, Kaafjer v;ell r*.ata on. the end norair.e "island'- east of Lic-pincott iudicares up to 60 feet of till overlies s.n irrsgpjinr Urbana Out"wash surf^cer Elevations of tho buried gravel surface range between 1135 and 1090 fee-';. Well logs Salem 14 and Salem 63, drilled one-half mile east of Lippincott, show that as much as ?0 feet of till overlies thick sand and gravel. Only three well logs are on file for the West Liberty Moraine elements southwest of West Liberty (Logan County), in north-central Champaign County. Each indicates 0 to 58 feet of trill overlying -Travel, Gravel surface elevation averages about 1100 feet above sea level. \ boveral well logs throughout the end moraine indicate the presence of till (!lcls.y|: or "hardpan") still deeper beneath tne buried Urbana Gutwash. This unit is irregular in surface ^lovaHon and thickness MO to 1OO feet) and may rep-resent i;he main complete covering of the county by an sarlier ^laciation. interfingerinn; till and outwash is exposed in a Hev; York Central railroad out 1.0 miles south of West -Liberty and in a sand and gravel pit "uj? ailes south-southeast of Lippincott on VJcst Kin^screek Road. Both exposures attest to an oscillating ice margin as tho Urbaaa (IrrcerttecLiate) Outwash v/as bcir^ deposited. This duplicated the conditions that occurred -il.or.v: t'.ie v.'estsfn margin of the Konnard Cut- wash, dur-lnu- its formation. Aveo.ll^r tho west Liberry Moraine appears to have been possibly a contiguous part of the Springfield Moraine. The? inoraine K^rati{jvaphy inAicat^s that the formation of " e: • the West Liberty Moraine probabj.y postdated deposition 01 the Springfield i-ioraine. Although both may bay? fo.nuod during a single retreat of the Miami Suolobe, ±~: appears unlikely that they were ever joined as a single, continuous moraine• Far:ner£3ville Moraine • The Farmersville Moraine (GcO •; ; v.'ai-, i/•••!-) forr-s a nearly continuous norch-south band in western Champaign County. Although end moraine elevations are similar to the sari-cunciing high groimd moraine, the end moraine is distinctive as a more auaniocfcy. continuous belt within the comparatively subdued topography of the su.rround.inec ground tr.oraine. Mean depth oi' carbonate leaching .tor the end moraine is $0 inches, which is also the near- for the entire county. Unlike the Miami Subiobe noraines 1:0 che ec.st, the Faraiersville Horaine is not underlain by thick outvmch. The moraine cay have been too high during stages of glacial drainage, Drill -vecor-ia indicate very chick till accumu- lations v/ith tbir. «and and gravel interbsds or lenses > Sill toiciniors^s of ovrr 100 .1'cet arc- indicated thrcurrhcuf ths iTioraino. Undoubtedly sone of this till v/as suba-lacial ciurinn; vhe niaxir.u." V/isc'oriSinan glacicition. Unfortunately watGr~v;ell logs cor.raln liftrle i.r:ro.ra?Tion coriceraing .the physical nsrnra of taa buried rills. :rhu3 o..i..; : ro.ction of buried ci.lls ao ieooc-'its of '''early'' v;isconn:; r.an cr :»?..flisx% or>s if, p-'obl^atjo. At localities overlying the buried. 'JCeays Riv.?r Valley, drift thicknesses of over 500 feet are kno./n (Norris and Spicar, 1953). Associated with the end moraine is an unusual boulder belt, first noted by Orton (1883). The boundaries ox the boulder belt and end moraine are not entirely coincident, but the similarity in distribution indicates a close!:/ associated origin. Brown OS'48) called related, hummocky topography of ./estern Clark County the Boulder Belt Moraine, noting the coincidence in distribution of ths end moraine and boulders. The boulders are primarily concentrated, on the moraine surface &nd in the upper fev.' foot of till* In IHOST; areas of the boulder belt, fanners have concentrated the boulders along fence lines and ditches. Boulder concentrations in western Ch.anrpal£;.i County are plotted in I?igure '11. Although the hunnocky topography of the end moraine is discontinuous in northwestern Champaign County, the boulder belt is uninterrupted. Th.; more subdued topography is probably a result of the area receiving a lesser till covor than the end rp.orain-i areas to the north 3.rld KC\.YG:U I-Iear the southeastern end of Kiser La5ce ic> a Izavna field that hriadn a tributary deposit of the Hr.d River- Valley Train, The formation of the hemes blocked a. major northwest-southeast r-reudin^ valley that -/?as probably a niajor dre.ina^a '-/ay during prc—Far-nerovil.le Morairie Uiiae. The ^lockage of the valley indicates tlaat the Pa.i?r,ersviile [•ici'aine forced after a readvance of the Miarai Subiobe. Presently two creeks head, in the kaise field; ilettle Creek, which, flews southeasterly into the Had River and Mosquito Creek, which drains northwesterly through Riser Lake into the Miami Hiver. Possibly the Farmersville Moraine formed in pre-'Mata" Wisconsinaa tine. The "late" Wisconsinan ice may have J ovarriden the end noraine prior to formation of the West A Liberty and Springfield Moraines. After a substantial retreat, the Miami Subiobe readvanced and deposited the rhin till capping the Parraersville Moraine, the boulders, and. the Icarte field southeast of Kiser Lake. Miami Subiobe Ground Moraine Bordering most of the distal (eastern) margin of thi .Spriri^field .'-loraine south of th= Kina-s Creek Valley is ground. niorair.o probably-associated with the Miami Subiobe. 1'ill vhickriesses 7. anew* up to 20 feet, ever «h:.ch rr^nuard C.ir'v-.'.^h, Ths patchy nature of the ground, tncraine and tha variability in till thickness, v/hich is best exemplified in '<;hc- ocutheastern corner of Salen Tovmship, suggest •3epo£ri;-Lon 'un.der a thin ice margin, j?etv:ecri the Springfield and V/es^ Liberty Moraines lies irregularly distributsd ground, moraine. T'his moraine co.M^ists of thin, till (4- to '!? feot) overl^-ing iJrbana Outv.'ash. Elevations on the buried gravel surface ranges from 1055 to 1020 feet south of Urbana and from 1O)C to "i075 feet north-northwest of Kingscrsek. This ground moraine seems to be continuous with the till capping tha Springfield Moraine and was probably deposited during retreat from the end moraine. Forming the western margin of the Mad River Valley and extending westward to the Farmersville Moraine is ground moraine deposited during retreat from the Springfield and Y/sst Liberty Moraines. This is the northern continuation of the North Hampton Till Plain (Br Scioto Sublcbe Una Moraines Cable Moraine V The Bellefontaine Outlier probably inpeded the southerly advance of the continental ice sheet and chan.nel.lf3d the Erie Lobe into two discre^tji smaller sublnbes on either side of ~he outlier, Early ir* the thinning of the ice sheet, the xv;o sublobes bscar.ie separate ice bodies and a sarj.^c o;? f-ncl 7110mines v;a? deposited, by each. South and east of OimnpaigT) County, 3o1.r.tc Sublcbs snd. wcraines appear as distinct entities or. the Glacial Map of Ohio (•.Tol-it^i•-•;.--••:.•*: o> al,, 1r;6'i), Thess lioulnct nervines become 30 concentrated into one broad morainic band as the head of tbe interlobate area is approached. The resulting composite end moraine, occupying a broad north-south band in eastern Champaign County, is known as the Cable Moraine f'L(- ^:r^ -:i , The Cable Moraine is compos- el of deposits of the London, Bloomingourg, Esboro, Glendon, Reeseville, and Xenia Moraines. Crests of several of these moraines have been traced northward into the Cable Moraine (Figure J^ ). Pfco Cable Moraine drift consists of thick till inter- spersed with chin sand, or sand and gravel, layers. Well logs in the Mechanic sburg area indicate drift thicknesses of over 200 feet. The drift generally thins northerly in response to the rising bedrock surface (I(1:.tv;:c3 ~)» How- ever, extreme dx-ifc thicknesses, such as 355 i''3Ot 1.2 miles east-southeast of Cable. are revealed by wells in northeastern Cloazipaign County. Thinnest drift (5 to 20 feet) is in the vicinity of tiarth Le'wisbxirg. Water-well data in soui;h-centr£'X Champaign Coanty (oou*;hea.r!-crn Urbana Tovmship) indicates '!•> to $5 i'eet of till ("clay"; beneath the Kermard Outvrash. A Uc 3. Geological Sui^v^.y test; hole drilled in the Gou'l-hv-ostern corner of .lection co-Ton, Urbana Township, penetra.tf.jd. iL6 foot of coarse sand arid travel (Kennard Otrtwash) snd tben 2^ feet of till. A secc-v.3 rill was found 12 .f«-?t below tha upper till, Th.i s well lies ir, t).).e lirjaar trend of tbo, Lualov: Spur of tl": Co.blo Horaine, -Mthcu^h the Fo;vell Mo r a ire The distal edge of the Pcvell Moraine occupies a very small area of the extreme northeastern corner of Cha.T.paig-j County. This Sinali area is the only deposit In the county of the clay-rich till associated with the reacivaace i:o the Pci/ell Kozaine as describe^ I./ Golv'.tb'/ar fc- p. Till samples analyzed b>r St^i.-r^r find ( '9/2) siiov: the Pov/ell Moraine till has approximately ^3/^ clay s.5 compared to 20^ clay in tills 01 the rarmersville , London, and Eeerf^viile Moraines. Till saiuplfts analyuad during this study average appr-oxiinarely 20$ clay, (Pi&urs 6V Figure 6 . Three-coaponent diagram showing the mean particle-size distributions for till samples from Champaign County. CIAY w \ vvv Silt C5TTfr' SAND Q.L.UJI. 0 Cable Moraine O Miami Su'olobe Ground Moraine A West Liberty Moraine 0 Springfield Moraine 33 Related Outwash Deposits Three distinct outwash levels are recognized in Champaign County on the basis of areal position, elevation, and composition. Kennard Outwash The oldest and highest general outwash level occupies a one-to-four mile wide north-south strip across east- '' ".£,!., r ' ^ central Champaign CSQettnjty and is known as the Kennard Out- wash (Goldthwait, 1952). The term Clifton Outwash was applied to this unit in Clarlc County by 3rown (194-8). The outvirash laps onto the older, western portion of the Cable Moraine so that there is a sharp eastern inargin to the deposit (Figure 7). Most of the western nia.rerin of the Kennard Outwash lies buried beneath the Springfield Moraine, as discussed above, and is thus problematic as to its exact original location. Only in a small north-south strip north- east cf [Jrbana does the Keimard Outwash protrude from beneath the proximal edge of the Springfield Moraine, The Kennard Outwash is readily distinguishable by a dark looss cap that, ranges in thickness from 15 to 4-3 inches (Figure 8). The loess cap is not present on top of the buried Kennard Outwash as it is exposed today beneath the Springfield Moraine or on the small Kynnard level exposure vest of the end moraine. Tbs cutv/ash forms a plain with low relief except in Figure 7. Northward view of Kennard Outwash and Cable Moraine (right and foreground); Cheese factory Road, 3-5 ailes southwest of Cable. IT Figure Q. Kef.nard Outv/ash exposed in American Asters^ate -oit, 2.5 siles west-southwest of Cable. Note dark loess cap on the Keriri&rd Outwash. 35 areas toa^ have been modified, by recent stream erosion. Elevations on the outwash surface range from 1210 feet at the Logan County line to 1100 feet at the Clari: County boundary. The Kennard surface slopes southerly at approximately eight feet per mile in Logan and Champaign Counties but levels off to about four feet per mile in Clark County (Goldthwait, 1955) • This change in gradient is probably due to the bedroclc constriction and barrier « 1 near Clifton in northern Greene County. Kennard Outwash forms a 33 mile long belt from southern Logan County to Clifton Gorge in northern Greene County. •The narrow, confined, but high distribution of the outwash indicates that the deposit had to form when the Miami Sub- lobe stood near the present we stern margin of the Spring- field Moraine. Only with the Miami ice in thin position could westerly and southwesterly drainage be blocked. Thus, during an early stage of "late" V/isconsinan retreat:, dated at about 18,50.0 years B»P. (Dreimanis and Goldthwait, in press), all iDeltwater of the two sublobes was channelled into a narrow belt between the sublobes. At the southern licit of,..:the Kennard Outwash, Clifton Gorge displays giant potholee in and. above the limits of the gorgs attest- ing to the huge volume of roeltwater and outvash that formed the PCenr.ard level. The Kjennard Outwash can be traced, to aacociated ice contact features near irhe v/e.stera margin of the Cable ftoraine. These kame terra ;ea are located 4-.0 ciiles south- southwest of Kechanicsburg and 1.5 aiiles vest of Mingo. The mean depth of carbonate leaching for the Kennard Outwash is 39 inches. This\is the highest mean value in the county and probably reflects the age of the outwash, porosity of the materials, and the^fehicimess of the loess cap (Rosengreen, 19?O, p. 3*0• Drbana (Intermediate) Outwash Urbana or Intermediate Outwash occurs in two distinct geoxaorphic settings in Champaign County. East of the Springfield Moraine in northeastern Salem Township and in the Buck Creek Valley of southwestern Union Township (Enon Outwash of Brown, 194-8), a higher (PZennard) outwash level has been cut to an intermediate level. West of the Spring- field Moraine and extending beneath the West Liberty Moraine is a continuous Urbana Outwash level. Stonecounts in the two areas indicate the outwash west of the end moraine had a Miami Sublobe origin whereas the excavated levels east of the Springfield Moraine approximate ICennard Oiitwash composition (Table 5)» Ave??age depth of leaching is 29 inches on the continuous portion of the outwash, nearly identical with the bordering Springfield and West Liberty Moraines, in spite of the difierences in permeability. The cut Kennard levels are free of carbonatss ^o an average depth of 32 inches. 37 Unlike the other outwash deposits of Champaign County, TJrbana Outwash has no associated ice contact features yet identified. It is possible that the buried gravel of the till-over-gravel area and the associated buried kame field east of Springhills in northern Harrison Township represents an Urbana Outwash source* This was suggested by Forsyth (1956, p. 161-162), When stripped of its till cover, the buried gravel surface east of Springhills is nearly gradational with the intermediate outwash level east of the Kad River Valley, In addition to stonecounts, areal position suggests a Miami Sublobe origin for* the Urbana Outvrash, If Scioto i^e had supplied. i»pi:*»r.ia] for the Urbana Qutwash, the ics margin would have had to advance over the Kennard Outwash. Some till wo-ald probably have been deposited during the subsequent retreat of the Scioto Sublobe. However, uo till is present on the eastern margin of the Kennard Outwash in east-central Champaign County. Total erosional removal • of rill cover over an area the size of the exposed Kennard Outv/ash seats very unlikely. The time cf formation of the cut Urbana Outwash levels •sack oi' the Springfield Moraine is uncertain. During early stages of retreat from the Springfield. Korains, meltwater i'rom the wasting Miami ice cay have cut the Kennard Outwash to an intermediate level. Formation of the cut terraces may have also occurred, synchronously v,ith the deposition of the Urbana. Outwash west of the Springfield Moraine, Mad River Valley Train The northernmost source of the Had River risea three miles northeast of Zanesfield in Logan County. The Mad River flov;s southerly through Champaign and Clark Counties to Springfield where it swings southwesterly and joins the Miami River at Dayton. Throughout its length, the Had River Valley contains a thick continuous outwash deposit. This most extensive outwash accumulation in Ohio is known as the Mad River Valley Train (Goldthwait, 1952), ilydrologically it is continuous with the Urbana and Kcnnard Outwashes to the east. The Mad River Valley Train forms a north-south, one to three mile vride band through central Champaign County. The mean depth of carbonate leaching is 55 inches, reflecting the well-drained nature of the outwash plain. Stonecounts indicate that materials from both sublobos were contributed during formation of the Mad River Valley Train. Some deposits of both sixblobes are ice contact features that head tributary deposits of the Mad River eut- wash. Tx'acing of these tributaries to rheir sources pro- vides an important tool to correlate ice margin positions between tiie sublobes. The gracLisnt of the Mad River Valley Train is slightly steeper than the Kennard Outwash gradient, ranging between eight, and ten feet per niile. Well logs and geophysical measurements (Janssens, 1964-) indicate the southern portion of the riad River Valley Train in O'haiapaign County is cut into bedrock and averages about 60 feet in thickness. In northern Champaign County, "clay", probably till, is encountered in most water-well holes at depths averaging about 75 feet. Cedar Bog, in sections 31 and 52 of Urbana Township in south-central Champaign County, is a remnant of great swarapy tracts that probably developed soon after the Mad River Valley Train was deposited. Small bogs that have been drained and modified are present elsewhere on the outwash surface, A typical bog is located at the head of the Hast Fork Valley along Ohio Route 4-, 5.1 miles south- west of Mechanicsburg. Ice Contact features Karris s Kucie.rous isolated deposits of ice contact stratified drift are found in Chair.po.ign County. ICa^es southeast of Kiser Lake head the NetUle Creek arm of the Mad River V'fillsy Train, tnuo .defining the Miami Sublobe position during this event. Stratified sand and gravel is exposed ire a s^all sanitary landfill within, the kaine field. Ice nms-; have filled the Kisei- Lake basin while tho kaiaes were deposited. She most extensive area of kame topography in the county is in north-central Ilarrison Township west of the Mad River Valley. This region is the southern portion of a large area of karaes that cover nearly 200 square miles of Logan and Champaign Counties (Goldthwait, 1955; Forsyth, 1956) (Figure 9)« To the east and southeast of this karae field lies a buried outwash. level, possibly coincident with the Urbana Outwash. The kane. field is covered with as much as 20 feet of till. In a small gravel pit, 1.0 miles south of Springhills, a probable Fox B-zorie soil occurs in pods at the top of the buried gravel, la the extreme northeastern corner of Urbana Tov/nship, 2.5 miles northeast of Urbana, the Indian Mound moulin kane (frontispiece and Figure 13) lies surrounded by outwash and lacustrine sediments. Snail borrow pits on the southern •Dortion of the karae expose sand and gravel that is covered with ':0 to 12 inches of loess. A second moulin kame is three miles south-southwest of Indian Mound, within the ground moraine east of the Springfield Moraine. This" kasie has a large gravel pit on its northern flank that exposes 30 feet of stratified sand and gravel capped by two to four feet o-r-till, indicating that the kame was overridden. The trend of the long axis of both moulin Icaaes is approximately i«, 15° E. zztending north of Indian Kound, portions of the ground moraine east of the Springfield Moraine are elongated along a similar trend. This similar- ity suggests that these deposits were developed in association with a ma^Jor fracture system within thin ice as the lobes began to separate. Although stratigraphieally .vthe moulin kames have not been shown to extend beneath the surrounding deposits, their areal position, composition, and exposed stratigraphy suggest that they are the oldest dep-osits of either sublobe present oe the stirface. • Two kaiae terrace's, associated with deposition of the f.r- Kennard Outwash, lie on the distal (western) edge of the Cable Moraine. The northernmost terrace lies only slightly above the level of the Kennard Outwash, 1.5 miles west of Mingo. The southernmost terrace is on the south side of the East Peri: Valley, 4.0 miles southwest of Mechanicsburg. This karae terrace is about 25 feet higher than the border- ing Kennard Outvrash terrace. Both deposits were probably formed synchronously with the Kennard Outwash in .a,thin ice, marginal zone. An isolated kaiae in the East Pork Valley, 3.0 Eriles southwest of lyiechanicsburg, is probably associated with the formation of the East Fork Tributary of the Mad River Valley Trad.ii. This kame contains large masses of well- cemented srj.'avel in a presently well drained position. ICases north and east of Hingo (Figure 10) and Cable head tributary deposits of the Mad Siver Valley Train. ICames buried beneath thin till head the East Fork branch PIgure 9. Locking westward over buried kame and kettle topography, 1.1 miles east-southeast of Springhills, Harrison Township. Figure 10. "Southward view of the kame field (K) that heads the westerly sloping (right) Had River Valley Train tributary at Hingo. Cable Moraine in foreground and background. of the valley train 1*5 rciles southwest of Mechanicsburg. Eskers Two buried ridges of stratified drift in Harrison Township of northwestern Champaign County have been identified as eskers. The smaller esker forms a prominent ridge marking the southeastern extremity of the buried kame field, 1.6 miles southeast of Springhills. Several small borrow pits on the west flank of the esker expose stratified sand and gravel. A. one-mile long sinuous ridge of gravel that is covered with till extends south- southwest from the buried kame field, 1.5 miles south of Springhills. A large gravel pit in the extreme northern end of the es.fcer, west o±' Calland Road, exposes the stratified drift that comprises the esker. To the south, augerings and water-well logs indicate gravel beneath a thin till cap. Boulders Boulder concentrations in Champaign County are plotted in Figure 11. The extensive boulder assemblages associated with the Farmersville Moraine ware recognized by Leverett (1902) and named the ?armersville Boulder Belt. Approx- imately 90 percent of the boulders are Canadian crystalline lithologies, while the remainder- are composed of Ohio bedrock types * The boulders are as much as six feet in ' I Figure 11, Boulder Ooncentratior.a in Champaign Ocmnty, _mlt«§ >99 boulders per acre 12 ~ 99 bould&rs per acre 4-12 boulders per aero 4- boulders' per a.cre diameter. Clearing of agricultural land has resulted in concentration of quantities of boulders along fence lines, woodlands, and ditches (Figure 12). Road and creek-cut exposures and drill records indicate that the boulders are confined primarily to the surface and upper few feet of till. Since glaciers have a very poor capacity for sorting, a selective concentration of boulders must have occurred before the material became incorporated into an advancing ice sheet, i-he boulder display no tell- tale features that would suggest intense eolian v/innowin Lacustrine Deposits Two miles northeast of Urbana, in northeastern Urbana Township, thinly laminated fine sand, silt, and clay indicate the presence of a lacustrine plain. Figure 1J is a picture of this lacustrine plain. -Exposures in drain&rrc ditches, seismic soundings (Janssens, 1964), and v.'ater-v/oll logs show that the lake deposits -ai-e four to 15 feet: thick and are underlain by bouldery clay (till) and outwash. Figure 12. Typical boulder concentration and on the Farmcreville Moraine. Horrauard view 3.0 miles northwest of St. Paris. Figure Eastv/ard view of the lacustrine plain, 2.5 miles northeast of Uroo.na. Indian Wound rnoulin kaiae and. Cable Moraine in background. 48 Augerings and well logs show that the lacustrine beds are stratigraphically younger than the bordering Kennard Outwash. The lake sediments also lap upon the Springfield Moraine and the ground moraine east of the end moraine. The lake probably formed contemporaneously with the Springfield tforaine. Heltwater ponded betv/een the forming end moraine and the westerly sloping Kennard Outwash surface. The lake drained to the south through a cut in the ground moraine. Such ponding probably ceased when retreat of the Miami Sublobe terminated easterly meltwater drainage » Directional indicators Striae Only two exposures of striae have been raeasur-ed. in Champaign County. Leverett (1902) plotted striae with a bearing of "E 10 K" in a now abandoned stone quarry on Stone Quarry Road, 4-.0 miles northeast of Urbana. A bed- rock exposure more extensive than exists today allowed Levorett to deduce that "...eastward movement is.clearly indicated on the rock sux'face, whose prominences show plainly that their v/est side is the stoss side". Poorly developed striae have been recently exposed on the Tymoohtee Dolomite in the bottom of the American Aggregates gravel pit, 2.0 miles south-southwest of Cable. The trend of the striae ranges from H. 38° V/» to N. 31° W. Crag and •"9 tail features are not present 1:0 indicate direction ol" ice movement. Till .Fabric Thirteen determinations of till fabric ai-e plotted as "rose" diagrams in Figure 14-. The till-fabric trends are very similar to directions of movement determined from striae. The channelling effect around the topographically high Bellefontaine Outlier is clearly shown in these plots of long axis orientation. Surface Soils Till-Soil Associations Vive "late" Wisccnsinan till-soil associations are recognizer! in western Ohio (Porsyth, 1965). ?rvese assoc- iations ar-s distinguished due to variation-; in. '!) looss cover, 2) arnovjc of clay in the E-hori^on, 3) amount cf clay in the C-norison, aad ^) depth of the soil profile, i'hese soil groups occur in irregular bauds, generally parallel to the end moraines. Boundaries between most till-so.il associations are caused by major variations in parent inatrsrials usually associated v/irh a significant :?'.53di.'anc3 of the ice sheet. Th« boundary between the Miami 6A ana Miami 60 soils t.vansects Champaign County through c.eposits of both sub- lobes. Tho sifrnificant characteristics of these till- 50 Figure "Rose" diagrams and locations of till fabrics in Champaign County, Ohio. End moraines are indicated by striping, 51 soil associations are given in Table 2. Table 2. Significant characteristics of the major till- soil associations in Chanroaign County, Ohio (adapted from Forsyth, 1965). Thickness of Depth of Clay percentage Name silt cap Leaching B-horizon C-horizon Miami 6A gen. none 16-30" 40-50# 15-27^ Miami 60 18" 20-40 33-4O 15-27 The soils contactr between the Miami 6A and 6O soils has been placed along the distal edge of the Fannersvilie Moraine and generally along the Beeseville Moraine (Forsyth, 19&5). Forsyth indicates that the age difference between th3 two soils is' not of stadial proportions because: 1) although the coil differences are distinct, they are not excessive and 2) radiocarbon dates in central and western Ohio indicate that a period of only about 4.0OO years was available for the entire "late" V/isconsinan retreat and concurrent deposition of some end noraines. Thus no major time period occurred between deposition of each parent material. Wilding et al. (1964) found no significant differences in composition of parent materials of 5A soils (Darby I Till) and 60 soils (Caesar Till) in western Ohio. Likewise no large scale pedologic variations were detected by Ritchie and Powell (1971) while mapping for the Goil Survey of Champaign County or during the present study, fiosengreen (1970) was unable to distinguish between Miami 6A and 50 52 soils pedologically while mapping Highland County. How- ever, he was able to map a boundary that coincided with the Reeseville Moraine on the basis of significant variations in loess thickness. The Kiarai 60 area of Highland County has an average of 13-1 inches of loess cover while the Miami 6A region lacks the silt cover. In new soil term- inology, areas formerly mapped as Miami 6A and 60 are now included under the term Miamian (for well-drained sites). Forsyth (196?) mapped and named three "late" Wisc- onsinan tills in the East Liberty Quadrangle of Logan and Union Counties. The oldest till, the Pickrelltovm Till, is named for a small town in Logan. County. This till is characterized by a loam textlre, Miami 60 soils, an average depth of leaching of 36 inches, and a brighter v;eathering color (Munsell 7.5-10YR 4-A compared to 10YR 4/3) than in the younger tills. The Bellefontaine Till has a pebbly loam texture and Miami &A soils developed in it. Depth of carbonate leach- ing averages 25 inches. The Bellefontaine Till extends north and east of the Pickreiltown Till to the distal edge of the Powell Moraine., '.Ohe youngest of the three tills, the 1-iarysville Till, is very clay rich and lacks the pebbly nature of the older drifts. Carbonates are leached to a near, depth of 24- inches. This till extends northward from the distal nargin of the Fov/ell Moraine. Forsyth O96?) indicates that the Pickrelltown and 53 Bellefontaine Tills can only be identified by reference to the variations in the surface soils developed in then. All three tills occur both as end and ground noraine in Logan ana Union Counties. Loess Cover Forayth (1965) states that significant accumulations of loess in west-central Ohio are limited to areas characterized by Miami 60 soils. The proximal boundary of this area is the Farmersville-Reeseville fioraine. f In Champaign County, only the expbsred Kennard Cutv/ash surface, east of the Springfield Moraine, displays a thick (15 to 4-5 inches) continuous dark brown (7.5*-R/-L/£*-) loess cap. All Kennard Outwash. including the area between the Mutual and Ludlow Spurs of the Cable Moraine, has this silt cap. The Miami, Celina, and Crosby Soil Series^ napped in ground and end moraine in Champaign v County (Ritchie and Tov/ell, 197^)» <-re developed in eight to 14- inches of dark grayish brown (10YR-V2) to dark brov/n (7.5^£V4-) silty rcatoriai overlying till. These soil series occur throughout the county. No boundary between loess/no loesy areas c?.ri be drawn on till of either sub- lobe. Thus the Farisersville-Reeseville Moraine position as mapped in Plate 1f v.'hich bordez'S thicli loess deposits in southern Ohio (Goldthwait, 1968; P.osengreen, 1970), has no sucb associated loess deposit in Champaign County. The loess cap is not present on Kennard Outwash that is exposed beneath the Springfield Moraine, Two expla- nations are possible. First, loess was deposited on the entire Kennard Outwash surface but was partially stripped when the Miami Sublobe advanced prior to formation of the Springfield Moraine. A second possibility is that the loess episode occurred after the readvance when the Miami ice stood at its easternmost limit. Thus the loess may have been deposited on the ice sheet and later redeposited by surface meltwater as the ice- sheet melted. Buried "Soils" The occurrence of a buried "soil", developed in out- wash gravel, beneath two to ten feet of till has been observed at several localities in western Ohio (Goldthwait, 1952, 1959). The leached, buried "soils" typically exhibit: 1) a distinctive red-brown color, 2) clay enrich- ment, -and 3) "ghosts" of former calcareous materials* In places leached reddish pods of "soil" have been incor- porated into the overlying till. Two explanations have been offered to account for the buried "soils". Goldthwaii; (1952, 1955, 1959) suggested that the leached zones are true paleosols, developed during iiiterglacial periods and thus imply periods of subareal 6f-\ exposure during their development. A second hypothesis holds that these "soils" are areas of. clay concentration, 55 P.ot'd layers, developed synchronously with the present sur- ji'aoe soils, through leaching, movement- dov/n through the till, and concentration of fine materials in the under- lying gravels (Gooding et al., 1959). Four exposures of buried "soils" have been described in Champaign Comity, A snail gravel pit in the ground moraine at Hillard Farm in southeastern Urbana Tovmship, 3.3 miles southeast of Urbana, exposed three feet cf till 7 f •...-,.. .-„•--. . J.H*.-V •' that was leached to 30 inches. Beneath the till, in bedded calcareous gravel (Kennard Outwash}, were patches of leached, red-brown "soil" (Goldthwait, 1955). In-an abandoned gravel pit just south of Springhills in north- westeru Chaapaign County, pods of "soil" have been exposed beneath two to four feet of till. The "soil" is located Just above the gravel surface of a buried karae (Goldthwait, 1955). This is the only buried "soil" locality still exposed in the county, In a burial trench in the O'rbans. Sanitary Landfill, on the Springfield Moraine, Jansssns (1964) described two to five feet of till overlying thick outwash gravel. The upper 15 inches of the gravel exhibited coloration and leaching indicative of a buried soil. A similar exposure of the "soil" occurred along Dallas Hoad (Urbana Township section 2,5) in southern Champaign County. No relic of these buried "soils" is present in either location today. Interpretation of these zones as true palecsols or as areas cf clay concentration profoundly affects the 56 interpretation of the glacial history of west-central Ohio, As suggested above, the Springhills buried kame field and the buried outwash east of the kame field may be associated with the Urbana Outwash. If this is true and the buried "soil" at Springhills is a true paleosol, the Urbana Outwash must be "early" V/isconsinaii. The "soil" probably developed synchronously with the paloesol exposed at Sidney, Ohio. Forsyth (1965) dates the period of formation of the Sidney soil at between 22,500 and 50,OOO years B.P., i.e. "middle" Wisconsinan. There- fore all deposits stratigraphically older than the buried "soil" at Springhills would be "early" V/isconsinan. Thus the Kennard Outvrasa and v/estern portions of the Cable Moraine v/hich are overlain by the Kennard Outwash, must have been deposited before the Sidney Soil Interval. In this study, the buried "soils" v:ill be considered to be loached, clay-enriched zones, primarily due to lack of any positive evidence that the zones are true paleo- sols. Surface soil variations throughout the county are not of sufficient magnitude to suggest a major inter- glacial period of soil formation. Results of Field and Laboratory Analyses Stonocounts Data from seventy-nine stonecounts indicata distinctive compositional variations in till and outwash of Champaign County. Stonecount percentages are tabulated in Table 3. Generally till deposited by tha Miami Sublobe has four to six percent more limestone and crystalline pebbles, and five to six percent less dolomite pebbles than does Scdoto Sublobe till. Percentage of clastic pebbles (siltntones, sandstones, and shales) average two percent higher in the Scioto Sublobe deposits. -Total carbonate percentages are two to three percent higher in the Cable Moraine ~han in the Miami Subloso end moraines. Cable Moraine stonecounts average BO-o dolomite whereas the V/est Liberty. Springfield, and ?ar;p.ar-svillf; Moraines average 73x» Ground r/iorains of the Mic.:si Sublobo averages r}2% dolomite joebc-las. Percentages of limestone p-a'nblss ranf3S from 10>^ in the Springfield Moraine, 13# for the Miami Sublobe ground moraine, and 16# .in the Farmers ville Moraine. Scioto .Gublcoo tills average '^' liriestor.e pebbles, a consistently lov;o~' va3.y.e than riic.nii Sublobe tills. Crystallirjw pebble percGn.tagos ars significantly higher in the Sprirj-^i'ielci (1'1?j) ^nd TParnersvrLlle (10p) Morainss '•thaii in the Cabl^ Moraine (bf-O • Within the Cable Moraine, £ local areas of anomalously ni^li crystalline pebble percent- age exis usucO.ly in acGociat.ion wich hi^h 58 "' concentration. Clastic pebblecounts are consistently higher in the Scioto Sublobe tills. Miami Sublobe tills average about one percent elastics whereas Scioto Sublobe tills contain about three percent clastic pebbles. Chert occurs as approximately one percent of pebbles in all till in Champaign County. Thirty-seven pebblecounts in outwash reflect the relative contributions of material from each sublobe during formation, of each outwash. Kennard Gutwash gravel averarres SO/S dolomite, 9# lime- stone, Sv crystallines, 2% elastics, and 1# chert. Based on the similarity to stonecouuts in Cable Moraine till, it appears the Kennard Outwash was foraed primarily of material associated with the Scioto Sublobe. This is consistent with the location 01' ice contact features known to be associated with Kennard Outwash. In two pits dug in the gravel exposed west of the Springfield Moraine, northeast of Urbana, stonecounts average 79# dolomite, 11# limestone, 6>i crystallines, 3# elastics, and 1/5 chert. Although certainly not definitive, these results surest that this gravel is Kennard Outwash pro- truding from beneath the Springfield Moraine. Urbana Outwash pebblecounts average '1'2.% dolcrnite, 16$ limestone, 9^' crystallines, 2^ elastics, and "\% chert. Although no definite source of this outwash is known, stone- count similarities with tills of the Miarrd Sublobe indicate concentration. Clastic pebblecounts are consistently higher in the Scioto Sublobe tills. Miami Sublobe tills average about one percent elastics whereas Scioto Sublobe tills contain about three percent clastic pebbles. Chert occurs as approximately one percent of pebbles in all till in Champaign County. Thirty-seven pebblecounts in outwash reflect the relative contributions of material from'fcacfr sublobe during formation of each outwash. Ksnnard Outwash gravel averages 80# dolomite, 9# lime- stone, 8>J crystallines, 2% elastics, and *\% chert. Based or< the similarity to stonecounts in Cable Moraine till, i-j appears the Kennard Outv/ash was foraed primarily of material associated with the Scioto Sublobe. -This is consistent with the location of ice contact features known to be associated with Kennard Outv/ash. In two pits dug in the gravel exposed west of the Springfield Moraine, northeast of Urbana, stonecounts average 79/"^ dolomite, 11# limestone, 6# crystallines, 7j$ elastics, and 1$ chert. Although certainly not definitive, these results suggest that this gravel is Kennard Outv/ash pro- truding from beneath the Springfield Moraine. Urbana Outwash pebblecounts average 72^ dolo'nite, 16^ limestone, 9?' crystallines, 2/j elastics, and ^\% chert. Although no definite source of this outwash is known, stone- count similarities with tills of the Miami Sublobe indicate 59 that the primary source of aaterial for the outwash was the Miami Sublobe. Three stonecounts in the buried kame gravel near Springhills average 74$ dolomite, 12# limestone, 11# crystallines, 2Jo elastics, and 1fa chert. Obvious similarity with Urbana Outwash percentages suggests an associated origin.. Stonecounts taken on the cut U:rb€«igr$tttwashlevels, east of the Springfield Moraine, average 81$ dolomite, 1095 limestone, 85& crystallines, 25» elastics, and 1# chert. These values indicate that these intermediate terraces are probably cut Kennard levels-. Kases head Mad River Valley Train deposits in both sublobes. Thus, Had Hiver gravel should have a composition indicative of the comparative amount of material supplied by each sublobe. The outwash averages 81$ dolomite, 5# linestone, 7% crystalline, 4# elastics, and 3# chert. Thus it appears the Scioto Sublobe provided the bulk of the material during formation of the outwash. Chert percentage is consistently higher in the Mad River Valley Train than in the older outwashes. The chert was probably derived from limestones that fornx part of the Belleiontaine Outlier. Calcite-Dolomite Percentages Sixty-one till samples were analysed for carbonate 60 content. The results are listed in Table 4. Although these samples are a minimal number to sufficiently cover Champaign County, significant variations are indicated. Samples analyzed by the Ohio Agricultural Research and Development Center (OARDC) for the Soil Survey of Champaign County (Ritchie and Powell, 1971) are also included in this discussion. Thirty-seven Miami Sublobe till samples indicate a total carbonate percentage that ranges from 24 to 54 per- cent with a mean value of 40.7#. The Springfield Moraine till is the most calcareous in the county, with an average total carbonate percentage of 47.2#. The West Liberty Moraine and Farmersville Moraine average $6.7# total carb- onate, Calcite percentages vary iron 11.7# in the Farmers- villa Moraine to 14. 3# in the Springfield and West Liberty 3E-- Moraines. The average calcite percentage for the Miami Sublcbe is 13.S#. Dolomite values average 25.4$ for the Miami tills, with a high percentage of 29-7# in the Springfield Moraine. Calcine/dolomite ratios average 0.52 Tor the Miami Sublobe tills. Ratios range from 0.59 on the West Liberty Moraine to 0.4S for the Faraersville Moraine, pjrty-seven till samples from the Scicto Sublobe dis- play total carbonate values between 16 and 52 percent with &. ;noari value of 35.0$. The Cable Moraine tills average 10.0;i calcite and 23.4# dolomite, both values lower than the means for t;he Miami Sublobe. The calotte/dolomite 51 ratio averages 0.4-6 in the Cable Moraine tills. Within the Gable Moraine, significant variations between raorainic elements is indicated but the number of samples is insufficient to establish definite trends* For example, four till samples (numbers 36, 37» 43* and 57) taken from the westernmost spur of the Cable Moraine 1.6 miles northv/est of Mutual, average 19# total carbonate, clearly separating the area from the rest, of the end moraine, Granulometric Distribution Plots of average sand-silt-clay percentages (Figure 6) indicate a striking similarity in particle size distribution of tills throughout Champaign County. Particle size distribution percentages for 61 till samples are listed in Table 5. Average till textures for all moraines in the county fall within the silt loam category of the U.S*D.A. textui*al classification. Size distributions of Scioto Sublobe tills fall under a wider range of textural classes (loam, silt loam, silt- clay loam, and clay loan) than do tills of the Miami Sub- lobe (loam and silt loan). Tills of the Cable Moraine average two to three po^cent more clay the.n tills of the Miami Gubiobe. However, this is not a significant differ— ence when magnitude, of possible laboratory errors is con- rsidered. Weight percentages in the 2.0 to 2.5.^-mia. fraction and and .frsctions display no consistent variations i;o 62 allow separation of any till units. Although minor textural variations are present in tills of Champaign County, particle-size distribution appears to be largely independent of compositional variations . Discussion and Conclusions .r....^ij^jyt*'"- Many glacial geologists have attempted to correlate moraines between the Miami and Scioto Sublobes. Boulder concentrations, depth of loess cover, particle-size analyses, end moraine crests, stonecounts, and depth of carbonate leaching have all been used in interlobate correlation. Leverett (1902) recognized that loess cover ended or became very patchy north of the Farmersville and Reese- vil.le Moraines. Gcldthwait (1968) confirmed this relation- ship through hundreds of soil auger sites. Goldfchv/ait interpreted this loess break as indicating loess depos- ition ceased as the ice sheet simultaneously retreated froia the Farmersville and Reeseville Moraines. On the proximal side of the end moraines loess averages less than nine- inches thick, whereas south of the moraines an average of 25 inches of loess is present. This loess boundary has been uraced in Highland County (Rosengreen, '=970) and Clinton County (1964). I A second, less clearly defined loess break occurs at the Cuba Moraine in the Scioto Sublobe and the Camden (Hartwell?) Moraine in the Miami Sublobe. Areas averaging up to 4-5 inches of loess occur south of these moraines,, usually to the east or southeast of major rivers (Goldthv/ait, 1963). The Camden Moraine consists of numerous discontinuous elements. Early tracing of the moraine elements northward through Montgomery and Clark Counties and into Champaign County ijcdicates a probable correlation with the Spring- field Moraine. Thick loess was not found in this study between the Farmersville and Cawden-Springfield Moraines, analogous to the loess between the Cuba and Keeseville Moraines in the Scioto Sublobe. Dreirnanis and Goldthv;ait (in press) indicate that the Cuba and Zenia Moraines may have been in part contemp- oraneous and probably were deposited shortly before and during deposition o.f the Kennard Outwash, Radiocarbon dating (W-91, W-531, Y-448, and OWU-551) indicates the ..related moraines were deposited during an 18,000 to 13,500 L. years 3.P. readvance of the Scioto oublobe. 2his re- i advance overran earlier Y?iscori£inan moraines in Clinton, | .Highland, and Iloss Counties. Thus, by correlation, the I Kiatii Sublobe ice margin must have stood in the general •^position of the Springfield Moraine about 18,000 years B.P. Rp- K^o spurs of the Cable Morains, south ann. v;est of MuUuai, Bfetfere partially buried by tae Ke:.nii::d Cv.«v;si::: e.:id i-.:a: ci'o::e probably represent deposits of the readvance to the Cuba- Xenia Moraine. The narrow, interlobate area in which the Kennard Outwash was deposited received a thick loess cover before the sublobes retreated. Such thick loess is present only south of the Cuba and Caraden Moraines in southwestern Ohio further substantiating the correlation of the Cuba-Xenia and Springfield-Caraden Moraines. Loess thins northward from southwestern Ohio. In Champaign County, only the Kennard Outwash can be delineated on the basis of loess cover. • A boulder belt and associated Farraersville Moraine clearly defines the Miami Sublobe position during deposit- ion of the Mad River Valley Train. Loess deposits of I southwestern Ohio (Goldthwait, 1968) indicate that the %: Farraersville and Keeseville Moraines were occupied synchronously. Therefore kames within the composite Cable Moraine that head deposits of the Mad River Valley Train must mark the Beeseville Moraine position. Wo continuous crest of the Cable Moraine connects these kames. No outstanding analogous Scioto Sublobe boulder belt was found on the Cable Moraine. Boulder concentrations have liniited areal and linear extent and seem to have little relationship to specific raoraine crests. The position of the Blooraingburg Moraine, the most bouldery end moraine of the Scioto Sublobe, is not clearly defined in its continua- tion within the Cable Horaine. However, the single crest 65 with'the most continuous boulder occurrences extends from 1.0 miles northwest of Mechanicsburg to 1.5 miles east of Middletown (Figure 15)« This crest has been mapped as the Bloomingburg crest of the Cable Moraine. Figure 15 shows that the crests of the Cable Moraine display two distinct trends. The majority of the crests trend nearly north-south, especially in the eastern half of the end moraine. In the western portion of the moraine crest trend varies between north-south and northeast- southwest. Several crests, e.g. the crest 1.0 miles east of Mutual, shew both trends. Possibly the northeast- southwest crests represent an earlier period of moraine formation v/hich has been partially overridden by a later readvance with a different direction of ice movement. A minimal number of till fabrics made during this study does not substantiate or deny this idea. Portions of the first crest east of Mutual has been mapped as the Reeseville Moraine (Platel, Figure 15)» This distinction was based on: 1) position of the crest /*' • with respect to the kames heading the Mad River Valley |L... Train, 2) limited boulder occurrences, and 3) tracing of crests from southeast of Champaign Coxinty. The easternmost crest of the Cable Moraine can be traced clearly south- easterly through Clark and Madison Counties to the London 6^,'Moraine . The Giendon and Ksboro Moraines probably do not reform distinctive crests within the Cable Moraine. The 66 "sure 15. Map of the Cable Moraine shoeing crests. Township boundary. End moraine crest. L London Moraine. B Blooajingburg Moraine. G Glendcn Moraine. £ Esboro Moraine. R Reeoeville Moraine. 67 minor crest between the Reeseville and Bloomingburg crests southeast of Cable may represent the position of either or both of the moraines. On the strength of loess information of the r.ynchron- eity of the Reeseville and Parraersville Moraines, ioe contact features heading the same outwash in both subiobes, and tracing of crests from the separated end moraines northward into the Cable Moraine, it appears the Pancers- ville-Beeseville boundary, ac mapped in PlattfeTTi is correct, Glacial History Pre-Wisconsinan Glaciation Deposits of Kansan ana lllirioian age in southwestern Ohio indicate that at least twice in pre-V/isconsinan time, ice sheets spread across western Ohio. No surface deposits of these earlier glaciatious are present in Champaign County. Drift that probably was associated with these ice sheets has been examined by deep drilling in the buried valleys of the Teays River System in the western portion of the county. Forsyth (1965) noted that deposits of Kansan and Illinoian age in southwestern Ohio iacl: a reentrant- area, similar to the interlobate area associated with "late" Wisconsinan glaciation. She suggested that the earlier ice sheets were much thicker than the Wisconsineu. ice sheet, (Therefore, topographic "high?1', such es "-he Beliefo:v;;aine 63 epj had less effect in impeding the ice flow during the Kansan and Illinoian glaciations. "Early" Wisconsinan Glaciation A buried soil, developed in till, has been described from two niles south of Sidney in Logan County (?orsyth, 1955, Forsyth and LaRocque, 1957, LaRocque and Forsyte, 1956). A log, lying on the paleosol was dated at 23,000 i 300 years B.P. (W-188). Nearby, peat has been found between till and the paleosol, indicating cool interstadial conditions (Sidney Soil Interval)(Goldthv/ait et-al., 19650- Forsyth (1965) indicates the peat is 22,500 to 50,000 years old. LaHocque (LaRocque and Forsyth, 1957) studied a fauna of pulmonate gastropods found in a thin.silt some below the till in which the paleosol developed. He suggested an "early" Wisconsinan age for the till, based on the presence of two speciee which are absent from known Illinoian deposits. No finite dates have been obtained below the stratigraphic position of the paleosol in west-central Ohio. Thus, evidence at the Sidney cut indicates "early" and "late" Wisconainan glaciations separated by a long "middle" V/isconsinan period of soil formation. • Dreimanis and Goldthv/ait .(in press) indicate that definite "early" Wisconsinan deposits have been recognized only a far soucli as Columbus in the Scioto Sublobe and the Sidney cut in the aaste-rr>. portion of the Miami Sublobe. Thus, the possibility exists that the "early" Wisconsinan ice sheer did not advance as far south as Champaign County. The through valley, now occupied by Kiser Lake and Mettle and Mosquito Creeks, nay have formed at this time. l?our localities in Champaign County displayed, possible paleosols, developed in outwash gravel. If these leached zonas arc- true paleosols, they may represent soil formation during the Sidney Soil Interval. Therefore, tills lying beneath buried, gravel in Champaign County may represent "sarly" V'isconsinan deposits. "Late" wiscorisiaan Glaciation Although flow of the continental ice sheet was impeded by tne uplands in Lugari C-oun !.,•>, oats ice was of .-sufficient thickness to cover the outlier, and remain as a continuous ice sheet over western Ohio. After near terminal positions bod been occupied for as long as 4,GOO years (Rosengreen, 1970; Ureiaanis and Goldthv/ait, in press) the ice sheet "began to thin arid retreat. At least-20.000 years ago, the Sciot-o and Miami Sub lobes separated and began to re- treat, forming; the glacial .features that constitute the present li-ulscape. The main flow of I-liaiai and Scioto Sublobe ico was around the Belief ontaine Outlier. CO he tv;o -divergent flows rejoii-ved a Ion;-; a line roughly coincident wi"ch ohe present position of exposed Kennai-d Outwash in east-central Cha^paigf, Oo:ij"v~y. T-ne ^rca o*.' whs covu'ity di:c::C'H.y ^ou'c-ii 70 01 the upland was a zone of thin, probably highly crev.-jneed ice. As the ice in this area thinned, melt-water transpoy-i-e-i material into holes (:-;oulin) in. the wasting ice. This II material was deposited as stratified drift in the form 01 mcujlj.n leases beneath the thinning ice sheet. Further .* melting and thinning resulted in tha physical separation or the two sublobes. Padioearbon dating in southern Ohio (flreiisanis and Go3dthwe.it, in press) indicates that the Sciooo Sublobe deposited the western portions of the Cable Moraine approximately 20,000 years B.P« While the Scioto . i Sublobe stood near the western edp;e of the Cable Moraine, along a line delineated by kams terraces 1.5 miles west of * f$ n Minrco and 'i-.G miles southwest of Mechanic:?burg, Miami S-ablcb_9^J.ce had retreared to a position just west of the present Springfield Moraine, without deposition of anj raoreinlo features. Vast araountr. of meitwater and material from fch-2 xrasti^g ice sheet becama channsiled in a narrov; aone between the ice sublobes and deposited the Kemiard Outwftsh. Th3 ice contact features associated with the western portion of the Cable Moraine and stcnecounts indicate triat the primary source of material for the Kermard Oul.v7asii was the 3cioto Sublobe. Masses of ice up to hundreds of feat in diameter became entrapped ai.'.a buried in i'.n« ih. These .ce masses later melted to .cor.~ the i; under t>ie present Springfield >o'!;tles tha rt -| r- ^ remained buried and unmelted until after deposition of the thin till that caps the Springfield Moraine. Exact position of the Miami Sublobe during deposition of the Kennard Outwash is uncertain because most of the western margin of the outwash level is bui'ied beneath end norainG, Inter-fingering till and outwash, exposed two to eight miles south of Urbana, indicate an oscillating i.ce mai-gin during deposition of tbe Kennard Outv/ash. As the meltwater receded, large quantities cf fine oubwssh material dried and were transported by the wind and deposited as loess on the Kennard surface and moraine •** uplands of southwestern Ohio. Up to 15 inches of silty material caps end moraines in Champaign County. If a thicker loess blanket was ever present on the end moraines cf Givaapaign County, it has been eroded off or concentrated j.r kettles and other depressions by v/asiu ^ Miami Sublobe ice t'len readvanced over the Ksv.nard Outvvash. as far east as the ground moraine east of the present Springfield Moraine. The loess cap mentioned above way have been deposited at chis time. During subsequent retreat the ground moraine v;as deposited. A major halt during retreat resulted in deposition of the thin till forming vhe 3[,rin£.t'ielo. Moraine. Ea?t«rly draining roslc- ^ater becsue 'cen-p'or-arily ponaed in a shallow lake, 2.0 . Eiiles nor"he£.st of Urban?.. Thin lake drained southerly '\ and oroo;;bly ceaseo to exist or\cc His;ni Sublobo re'-roat deprived the lake ox its meltwater. The intermediate outuash level, cut in Kennard Ouwash aast of the Spring- field Morai?ie, may have formed at this time. The Miami Sublobe continued to-retreat to a position west of the present West Liberty Moraine. Exact position of the ice margin at this time is unknown due to extensive valley cutting prior to formation of the Mad Hiver Valley Train. Meltwater, choked with drift materials, streamed, from the wasting Piiami ice and deposited the Urbana Cac- wash. During cutting and deposition of the outwash, rho ice nargin. oscillated, forming interfingering till and gravel which is exposed along the proximal (western) side of the West Liberty Moraine. A final phase of till deposition associated with this ice marginal position resulted in deposition of till capping the West Liberty Moraine. A second, somewhat less plausible, sequence of events can be offered to explain the stratigraphy and relationships derailed above, I'he major readvance before forning the Springfield Moraine and associated gi'ound moraine could have occurred after both the Kennard and Urbana Outw&she-s hao l-een deposited. After deposition of the Konnard Out- v.Tj^h, che Hiarr.il -Sublobe retreated to a position west of the pL-eso'io w'ef.t' ;uj.b-.,-.o"cy I-;oraine. Meltv/ater irou"; the i/^iy::inf- ;:.ce soouroi tlis kermard Outv;ash surlac^ and d^popi'C^ tiie Urbsna Ourv;a.-.;ht o^v^ral minor ice n;a».Tin osciliai,iovic ( '2 in the i-Iiami Sublobe forced the interf in-serine; till r,,1(] gravel found along the wester sdge of the W«st Liboriiy Horai.ie, The Miami Sublobe then radavance as far eua;; as the ground moraine east of the present Springfield Moraine. TLe loess cap on tiie KennarG. Outuash, "lepoc-il.ou before the readvance, suffered complete stripping by the- advancing ice. Buried "clay" (till) layers beneath chc Springfield and West Liberty Moraines lend some ci-odencc to this sequence. However, the expected Increase in gravelly material in the upper till due to overriding of ' the outwash, is not demonstrated. Retreat of the Miami Sublobe exposed the ground ! moraine east of the Springfield Moraine and the chin till forming the surface of the end moraine. The small gluei?.i l^ice 2.0 iiiilss northeast of Urbana, was formed as me'J.t- yjater poivied to the east of the end morsine and before ice vaca-ifcd the Kings Creek outlot. The -JesT Liberty Moraine could have formed at thi-eft distinct intervals: 1) during a halt in KifMni Sublobe :-etreai fter formation of the Springfield Moraine, 2) after the Springfield Kcraice aa a result of a separate rePfivanee oJ asri ice, or 5) before tho ree.dvarice and !"o relation o; ?pr the -•£-.7 ):.-aiiie was overridden. The Uv-ba:: h< ana V/; surface. Thin patchy till overlies Urbana Outwash south and southwest of Urbana. These till-over-gravel areas are probably remnants of a till unit that covered all of the exposed Urbana Outwash. Both sequences are identical beginning with Jilanii Sublobe retreat and deposition of the ground moraine west of the West Liberty and-Springfield Moraines. Formation of the Farmersville-Reesevi3J.eHoraa.ne Following a retreat, both sublobes readvanced to the Farnersville-Reeseville position, six oiiles weet and east of the Mad River respectively. Radiocarbon dating in >;; " southern Ohio (i)reir.anis and Goidtnwait, in press) indicate.- this readvance occurred in riaaison and Greene Counties aboat 17,OOO years B.P. Deposits associated with this r.eadvance are very bouldery, indicating that the drift material vas sorted by an unknown mechanism before glacial transport: and bad anomalous quantities of far-travelled material. Tlie correlative nee margin position of the sublobes is determined by: 1) kanes that head the east and ivest tributaries to the Mad River Valley Train associated with both moraines, 2) soil Voriations (Forsyth, 1965), and i>) vaoiatiors in loess cover further south in Ohio (Go.i&thwait, 1963). Evidence elsewhere in southern Ohio suggests 3 najor period, of loess accumulation occurred, iro to this t.iu;3 (Goldthwait, 196G), However7 loe^s deposits in Cha^pai^n County do not clearly substantiate this event. Certainly \rast quantifies of fine outwash materials were exposed and available for eollan transport. If Ohio:-; loess was deposited., erosion has thoroughly stripped the western Cable Moraine and areas v/est of the Mad River Valley of evidence of its existence. The Miami Sublobe then retreated from Champaign Count 3r depositing the ground moraine west of the Fannersville Moraine. Synchronously, the Scioto SublobeTWs" " retreating v/ith significant halts in forming the elements of the Cable Moraine associated with the Glendon, liaboro. BloomingburgCi and London Moraines. Further retreat of the Scioto ice etisi; of the Cable Ilcraine, resulted in dsposi- cion of the uppermost Darby Till on the Darby Till Plain of v/eat-ceritral Ohio. , Aftor o . a.jor retreat to a position north of the Ohio draj.i"sa.fje divide, an ice front lake formed in which qu3ii'citi'..o of fine sediment acc-u^ulated (Porsyth, 19o>^» A yubsoGuc.nv readvance of the iirie Lobe (Approximately 'l-^P-OO ye-:..rc. B.?., Dreii-anis :-ind Gc3.dthv;ait, ir\ press) incorpora.te'1 the Dilt/ciay-rich lacustrine material and. flepo3.li.ed a distinctive drift sheet as far south t^a tr.e Po-.v^li. ,';o c-aine in. extreme no/.--jheast«rn Champaign County, R^cont exosxon has O:'d;>T cli^iit-l-v :':oiif-j.ed th& p:laciaj terrace formation (two to four feet above the present Had River) due to entrenchment of the present drainage are the primary modifications. 77 APPENDIX Sample locations are plotted in Figure 16. Sample Locations 1 0.1 miles SE function Ohio Route 55-Coffin Station Road in Terra Haute, S bank Storms Creek, elevation 960 feet, Section 19, Ksd River Township. 2 1.1 miles EKE Terre Haute, 0.7 miles WE Stores Creek Road, house excavation 100 feet N Willow Dale Road., elevation 1125 feet, Section 15, Mad River Tov.'nship. 3 2.2 niiles ENE Terre Haute, borrov; pit 150 feet S of Willow Dale Road, upper till, elevation 1050 feet, Section 7, Mad River Township;, 4 Same'as Sample #3, lower till, elevation 1025 feet. 5 1.0 miles SE Springhills, gravel pit 0.1 miles S of Calland Road, elevation 965 feet, Section 20, Harrison Township. 6 0.2 miles S of Logan County line, gravel pit 150 feet E of Mete Read, 0.1 miles SSE Junction 'lets Read- Mt. Tabor 3oad, elevation 1290 feet, £alem-',v'ayne Township boundary. 7 4-.0 miles RE Urbana, abandoned stone quarry, 200 feet E of Stone Quarry Road, 0.6 miles NV.f function of Stone Quarry Roaa-Ludlov; Road, elevation 1140 feet, Saleu Tounsiiip. 8 1.2 ailes SSW West Liberty (Log^n County), west side New York Central RR cut, lower till, elevation 1115 feet, Section 26, Salem Township. 9 Saae as Sample #8, upper till, elevation 1125 feet. 10 1.4- ailec SYJ North Lewisburg, gravel pit 0.1 miles S Erie-Lackawe.na 3Ic, 0.3 niles SW Gilbert Road, t1ust E of township boundary, elevation 1195 feet, KW % of Rusjh Tov/nship. 11 1.0 miles ESE Urbana. gravel pit 150 feet SW Ohio Hou'tr. >'; , across from Oakdale Csmetervj elevation HOC feat, Section 17, Urbana Township 1 12 4-. 6 niles S Drbana, grs-vel 'DJ.t Q.2. miles W Midi Drtanc. Road, 0.^- nileo £SV: J-inctior, Pallivs -iz^- Kiddie Urbana Road, elevati.cv.- -M2-J- i;eu, ur>: 16. Sample -locations in Champaign County.; 79 13 5.8 miles S of Urbana, gravel pit 50 feet N of County Line Road, 0.5 miles E of junction Middle Urbana Koaa arid County Line Road, elevation 1070, Section 24, Urbana Township. 14 2.7 miles SSW of Urbana, borrow pit 100 feet N 01 Hickory Grove Road, 0.1 miles "W junction of Hickory Grove Road- U.S. Route 68, elevation.1035 teet, Section 27, Urbana Tov/nc.hip. 15 1-5 railes II of St. Paris, house excavation 75 feet E Kiser Lake Road, 0.1 miles S junction Kiaer Lake Road-Smith Road, elevation 1205 feet, Section-13, Johnson Township. 16 1.6 miles WSW Urbana, gravel pit 100 feet S U.S. 36, *KX) feet N Pennsylvania KR. elevation "tOJCTTeet, Section 35 > Urbana Township. 17 1.5 miles NW Urbana, house excavation 150 feet_W of Ohio Route 29, Millerstown Road, elevation 1055 feet, Section 3O, Urbana Township. 18 4.S ailes NNW Urbana, gravel pit 100 feet N of West Kingscreek Road, O.S miles E junction. West Kingscreek Road-Upper Valley Pike, upper till, elevation 109? feet, Section 28, Salem Township. 19 Same as Sample #18, lower till, elevation 1085 feet. 20 0.1 railes E Lippincott, gravel pit 250 fest S of Lippincott Road, 75 feet behind barn, elevation 1045 feet, Section 35» Salem Township. 21 2.7 miles ME Lippincott, road cut S side Kennonite Church Road, 0.2 miles W junction Mennonite Church Road-KcClain Road, elevation 1075, Section 19> Salem Township. 22 Same as Sample #6. C.3 miles S of Cable, E side road cut Mutual-Union Road, 0.3 miles N junction Mutual-Union Road-Urbana V/oodstock Road, elevation 1215 feet, Wayne Township. 24 1.8 miles wE Mechanicsburg, road cut N side Ohio Route 54, 1.2 miles 1'IE junction Ohio Route 5'*~Wing Road, elevation '1095 feet, NE % Goshen Township- 25 Same as Sample #5- 80 26 2.2 miles SSE Rosewood, N side road cut Kiser Lake Road, 0.6 miles S junction Kiser Lake Road-Shapp Road, elevation 1125 feet, Section 16, Johnson Tovai- ship. . 27 1.5 miles NW Mingo, ditch SE side Bump Road, 0.3 males NE junction Bump Road-Met?. Road, elevation 1305 feet, NV/X Wayne Township. 28 3.3 miles WSW North Lewisburg, 1.2 miles NE Mingo, y side ditch ."Johnson Road, 0.2 miles NNW junction Min^o North Lewisburg-Jphnson Roads, elevation 1115 feet/ NE % Wayne Township. 29 1.4 miles W North Lewisburg, ditch SW Sheeiie Road, 0.4 miles Wtl junction Sheehe Road-Mingo-Horth Lewis- burg Road, elevation 1160 feet, NWX V/ayne Tov/nship. 30 0.1 miles S North Lewisburg, house excavation 100 feet W Glend.enning Road, 0.2 miles S junction Ohio Soure 245-Glendenning Road, elevation 1095 feet, NW % Rush Township. 31 1.1 miles WSW Woodstock, G side drainage ditch, 100 feet P» Urbana-Woodstock Road, 0.6 niles ENE junction Park Koad-lTrbana-Woods toe]; Road, elevation 1060 fur,L, SW X Rush Township. 32 2,7 miles NW Wcodstock, gravel pit 0.2 miles N of ICauffman Road, 0.4 miles NE junction Kauffman Road- Corbett Road, elevation 1135 feet, NW % Rush Town- ship. 33 1.0 miles NW Cable, ditch N side I-'latfoot Road, 2OO feet NW junction Flatfoot Road-Ohio Route 245, eleva- tion 126O, SO Wayne Township. 34 1.7 miles WSW Mingo, gravel pit 200 feet SSW junction Kennard-Mingo Road-Gray Road, elevation 1225 feet, V/ayne Township. 35 0.3 mil OR SSE Mi delict own, ditch E side Cable Road, elevation 1290 feet, Wayne Township. 36 2.6 miles SW Cable, road cut N sido Urbana-Woodstock Road, 0.1 miles E junction Urbana-Woodstock Road- Ohio Hcute 245, elevation 1210 feet, SW X Wayne Town- ship. 37 1.7 milsfl W^Tw Mutual, hou.s^ excavation 150 feet E Ludlow Road, 0.2 irales N Onio Route 29, elevation 1205 feet, o2otio;. 29, lu^Lcw IV 38 1.7 miles S Mechanicsburg, ditch N side Wren Road, 0,6 miles ESE Wren Road-Mechanicsburg-Catawba Road, elevation 1175 feet, SC Goshen Township. 39 3-7 miles SW Mechanicsburg, ditch NE side Ohio Route 56, 0.3 miles SE Junction. Ohio Route 56—Brignor Road, elevation 1210 feet, SW JC Goshen Township. 4-0 2.2 miles SSW Mechanic sburg, NW side drainage ditch 100 feet SW junction Mechanicsburg-Catawba Road- Pleasant Road, elevation 1175 feet, SW # Goshen Township. 41 3.1 miles SW Mechanic sburg, house excavation 100 feel; SW Erigner Road, 0.4 miles NE junction Brigner Road- Ohio Route 56, elevation 124-5 feet, SW X Gor.ben Township. 42 1.9 miles E Catawba Station, road cut SE side Brigner Road, 0.9 miles SW junction Brigner Road-Ohio Route 56, elevation 12?O feet, SE % Union Township. 43 1.1 miles SE Catawba Station, N bank stream cut 50 feet E Ohio Route 54-, 0.1 miles NW junction Ohio Route 54-Brigner Road, elevation 1185 feet, SE # Union Township. 44- 3.3 niles ESE Urbana, house excavation 300 feet E of Three Mile Road, 150 feet N Ohio Route 29, elevation 1150 feet, Section 4, Urbana Township. 45 Urbana Sanitary Landfill trench, 0.3 miles S of Childrens Home Road, 0.5 miles SE junction Childreus Home Road-Edinger Road, elevation 1155 feet, Section 18, Urbana Township. 46 3-4 miles HE Urbana, gravel pit S side Jackson Hill Road, 0.2 miles W junction Jackson Hill Road-Mason Road, elevation 1140 feet, Section 8, Salem Township. 4-7 1.2 miles NW Kennard, Oak Grove Cemetery excavation, 100 feet W Ludlow Road, elevation 1175 feet, Section 12, Salem Township. 4-8 1.9 miles S Cable, tiling ditch 100 feet KW junction Mutual-Union Road-Cheese Factory Road, elevation feet, SW X* Wayne Township. 4-9 1.7 miles ENE Cable, ditch S side Blue Road 300 feet W junction Brush Lake Koad-Blue Read, elevabior. 1185 feet, EC Wayne Township. 50 1.5 miles SE Cable, ditch 20 feet SE junction Urbana- Wocdstock Road-Yocura Road, elevation 1280 feet, EC Wayne Township. 51 3.1 miles SE Cable, ditch W side Parkview Road, 0.3 miles N junction U.S. Route 36-Parkview Road, elevation 1205 feet, SW % Rush Township. 52 3.5 miles NNE Mechanicsburg, ditch W side Ohio Route 559, 300 feet S Treacle Creek, elevation 10?5 feet, NW X Goshen Township. i 53 3.8 miles NW Mechanicsburg, ditch N side Rand Road, 0.1 miles W junction Rand Road-Perry Road, elevation 1180 feet, NE %, Union Township. 5^ 3.2 miles WNW Mechanicsburg, ditch E side Talbott Road, 0.2 miles N junction Talbott Road-Ohio Route 151, elevation 1265 feet, NE % Union Township. 55 1.0 miles W Mechanicsburg, borrow pit 250 feet SE Allison Road, 0.3 miles SW junction Allison Road- Ohio Route 29, elevation 1110 feet, WC Goshen Township. 56 2.0 miles IT Mechanicsburg, .road cut N side Ohio —^_ Route 161, 0.9 miles W of Five Points, elevation 114-5 feet, NW X Goshen Township. 57 2.5 miles NW Mutual, gravel pit 100 feet N of U.S. Route 36, below Urbana Country Club, 0.2 miles.ENE junction U.S. 36-Ludlov/ Road, elevation 1080 feet, Union Township. 58 3.1 miles SE Springhills, ditch W side Couchman Road, 0.2 miles W junction Couchrcan-Slide Chapel Roads, elevation 1085 feet, Section 8, Harrison Township. 59 0.1 miles S Carysville, house excavation 100 feet W Ohio Route 235, elevation 1125 feet, Section 29, Adams Township. 60 1,8 miles NE Christianburg, road cut E side Ohio Route 235, 0.1 milos N junction Ohio Route 235-Chrishian- burg-Jackson Road, elevation 1090 feet, Section 20, Jackson Township. 61 1.2 miles W Westville, road cut S side U.S. Route 36, 0.1 miles E junction U.G. Route 36-Eris Road, Section 17» elevation 1065 fs-et. Mad River Township. £5 .TABLE 3 . STOH2CGUH11 PEROEKTAGES OF TILLS AND OP CEA.KPAIGN COUNTY, OHIO. Stoneccunt locations are plotted, in figure ''7. -» Sample & Unit Percent Pebblas Total Dol. Ls. Cxline. Clastic Cheri; •jarb. - - Outwash Keanard 1 70 13 12 1 1 c38 2 81 11 6 2 0 >r ^ SO • 7 12 0 1 37 74 8 16 2 0 5 77 8 11 3 1 85 6 82 10 6 •'•- ^-^i«fP'-i-*--'' T 9? 7 88 6 5 1 C 94 6 84 9 4 3 o 93 9 33 9 6 2 0 92 10 79 11 6 1 5 90 11 82 8 5 3 2 V'A 12 77 10 7 3 ^ 37\ 13 81 8 6 3 2 89 \ 78 3 2 •5G 9 5*/ 15 84 5 8- ^" C - x Urbana 16 75 15 6 C. 2 90 17 67 15 16 3 0 S2 18 76 13 6 3 2 3<:) 19 66 22 6 3 3 88 20 80 12 8 1 0 92 21 59 24 13 3 1 3? 22 72 17 9 2 0 89 25 74 20 6 0 0 94 24 81 11 7 1 0 92 25 73 14 10 s 0 37 26 32 8 10 2 0 90 27 80 10 7 2 1 90 Mad River 23 83 '? 2 5 2 90 29 79 3 9 5 4 52 .30 S3 4 8 2 3 3? 31 80 8 6 4 4 8b 32 79 6 7 5 3 33 84 4 7 3 2 80 34 80 3 o 5 3 B5 35 79 10 6 3 'i 39 Stonecount Locations in Champaign Countv, Percent Pebbles 1 Sample & Unit Dol. Lsfc Cxline. Clastic Chert , .'"-..-iro» .-, -rl V , ] I,'f; J> • 36 78 12 7 37 80 10 6 90 End Moraines Cable 38 86 5 7 0 2 91 39 64 17 9 8 0 81 40 85 9 5 1 0 9'<• 41 S2 12 5 2 1 94 42 78 14 6 2 0 S2 4-3 23 25 12 6 70 44 V_ 85 13 1 0 98 4-5 85 5 6 2 90 46 66 15 9 8 2 71 47 88 4 7 1 1 92 48 34 7 5 2 2 91 49 55 8 4 2 1 93 50 87 4 5 2 2 91 Springfield. 77 10 12 1 0 37 52 79 2 13 1 5 81 53 76 8 14 0 2 84 54 78 9 11 1 1 37 55 75 10 13 2 2 83 56 80 11 4- 3 2 91 57 69 15 9 3 !!_ 84 West Liberty 58 71 11 2 2 85 59 78 10 11 1 0 88 60 75 15 8 1 1 90 61 75 10 15 0 0 95 .Farnersyj-1 le 62 72 13 9 0 1 90 63 69 21 10 0 0 90 64 ?0 13 14 2 1 83 65 BO 13 o 0 0 93 66 68 19 11 1 1 87 67 72 16 10 0 36 Percent Pebbles TI~ — o'; I Sample & Unit J. C1 -.- C* _ I Dol. Ls. Cyline. Clastic Chert- Ground Koraine Miami Sublobe 63 69 20 9 69 77 3 18 0 c. so 70 34- 8 12 0 1 92 71 62 21 16 0 1 72 6? 15 13 2 3 82 Kames 73 86 9 2 0 89 7^ 69 21 7 2 1 90 72 6 19 2 79 76 80 9 6 3 2 89 77 S3 7 8 1 1 90 78 85 7 6 1 1 92 79 82 8 8 1 1 90 P'"' TABLE 4 .. RESULTS 0? CHITTICK-GASOMETRIC ANALYSES FOR WEIGHT PERChllTAGSS Olj1 CALCI'TE AND DOLOMITE IN THE LZ=>fJ TEAM 2mm SIZE FRICTION OF CKAKPAIGH COUwTY TILLS Percent by weight of <2nun frac'c5-cri 1/tvj.CiV'c1 Sample Bolonite CaCO-, ecniiv. Calcite •; ]}o lorr.it i- 1 14.6 26.3 42.9 0.55 2 9.2 26.9 38. 1 0.34 3 17.5 29.2 49.1 0.60 4 14.5 28.1 45.1 0.52 5 12.5 25.8 40.5 r\ /: o 6 7.6 23.3 33.6 6 1 32 7 4.2 14.7 19.9 0.2S 8 11.4 16.3 31.2 0.6^ 9 12.1 25.8 40.1 0.47 10 8.9 23.2 39.4 0.52 11 15.7 30.9 49.2 0.51 12 11.5 24.7 42.2 0^63 13 17.4 28.6 48.8 0.61 14 14.6 r-5.\ *^— *"^ 41.9 O.58 15 15.3 31.4 49.3 0.49 16 15.3 24.3 42.1 0.62 17 2.0 0.0 2.0 -., — .* 18 *--7 12.5 18.3 O.iSS 19 20.9 50.6 54.0 0.68 I 20 15.5 16.9 33.3 0.91 21 7f • .'^ 56.2 46,. 7 0.21 22 12.4 2S.8 43.6 0.45 23 12.5 27.8 42.6 0.45 24 14.3 27.5 43.4 0.52 25 2.8 0.0 2.8 — — — 26 11.5 20.1 35.2 C.57 27 7.0 31.0 40.6 0.25 23 16.0 37.7 54.4 0.43 29 11.4 24.7 38.1 0.46 50 3.2 16.4 21.0 0.20 18.0 23.1 0.20 31 5.7 *•- f- *~ 32 3.5 ^O.7> 32.4 0.13 33 14. () 20.4 56.1 0.69 34 20,2 24.8 47.1 0.81 35 10.3 28.9 42.1 0.3? 36 5.9 6.2 '!0.5 O.SJi 37 9.0 7.4 19.1 1.22 33 4, 5 2.8 oi • s^ 1.5B 39 12.5 31.5 46.9 0,40 40 1&.3 29.5 48.2 0.55 ^••••*<.;.-:tTv.-. W'5: •••':'. •---• ••••'. > ?.&*&••>';.•- ••.':••. • '• .' 08*0 5*917 U9 88 !' TABLE 5 PARTICLE SIZE DISTRIBUTION OF BULK SAMPLE 1— — Percent; by v/eight (pebbles on total sample: j sand-silt-clay on less than 2rnm fraction) I ' ...... i 4 1 Pebbles Sand v.".j.^- XI •-* Oj.a._;r "? a-- . 1 o r-! P. 3« S CO •d iH £ P« American Society for Testing Materials, 1964; Grain- size analysis of soils, D4-22-46;; in Procedures for testing soils, p. 95-106. Busch, D. A., 1939> The stratigraphy and paleontolosj of the Hiagaran strata of west-central Ohio and adjacent northern Indiana £ unpubl. Ph.D. dissertation, The Ohio State University, 2$3P- Brown, 3. M», 1948, The Pleistocene geology of Clark County, Ohio: unpubl. M.S. thesis, The Ohio State University, 73p- Carman, J. E. , 192?, The Monroe divisiorl of rbe&s in Ohio: Jour. Geol., v. 35, p. 481-506, Chaaberlin, T. C,, 138$, Terminal iao?,'aines of the second glacial epoch: U. S. Geol. Surv. 3rd Annual Rpt., p. 291-402. Dreiroanis, A., 19^2, Quantitative gasoraetric determination of calcite and dolomite by using Chittick .'. 3ed. Pet», v« 32, p» 520-529. Breimanis, A. and Goldthwait, R. P., in press, Wisconsin placiatxon in the Huron, Erie, and Ontario Lobes in Black, R., Goldthwait , R. P., and V/illdac, H. "Ceds.) G.S.A. Memoir Dt.;j?rcll, P.. K., 19&1. The Pleistocene geology of the Cincinnati area: G.S.A. guidebook, Cincinnati meeting, p. 4-6-57.. H. M. , 1938, Physiography of eastern United States: McGraw-Hill Book; Co., N.T. , JPeulner, A. J. , I960, Ground-water resources of Champaign County, Ohio: unpubl. Ohio Div. of Water report, S'crsyth, J. L., 1955, The glacial geology of Logan and Shslby Counties: unpubl. Ph.D dissertation, The Ohio State University, 208p. ———————.———, 1965, Contributions of soils to the mapping and interpretation of Wisconsin tills in western Ohio: Ohio Jcur. Sci., v. 65, p. 220-227o 92 ;?orsyt;h, J. L.\ 196?, Glacial geology of ciae East LJ.borty quadrangle, Ohio: Ohio Div. Geol. Surv, Re-st. of Investigation No. 66. Goldthwait, 3. P., 194-8, Wisconsin glacial deposits in The water resources of Montgomery County, QETo: Ohio Water Resources Board Bull. 12, p. 32-36.* ————————————— a 1950, Wisconsin glacial deposits _ia 'I'he water resources of Greene County, Ohio: Ohio Water Resources Board Bull. 19, p. 13-13. ————————————— $ 1952a, Glacial deposits in The water resources of Clark County, . Ohio : Ohio Water Resources Board Bull. 22,.. p. -VI -46.. ————————————— $ 1952b, Guidebook of the 1952 field conference of the (Eastern) Friends of the Pleistocene, printed by Ohio Div. of Geol. Surv. , 14-p. _.———— — .. —————— ^ 1955, Pleistocene chronology of south- western Chic in Guidebook of fifth biennial Pleistocene field conference, pt. 2, p, 35-72. ————————————— , 1959, Leached, clay-enriched zones .ia post-Eanganonian oLcift in southwestern Oiii-: and southeastern. Indiana: a reply: G.S.A. Bull., v. 70, p. 927-928. ————————————— t 1962, The 1962 field conference of the }?riends of the Pleistocene, guidebook, 26p. —— . ———————— —— s 1963, Two loesses in central Jouthv.'ewt Ohio in I'he Quaternary of Illinois: Uviiv. Illinois Special Pub. 15, p. 41-47. —,.- ——————————— f 196;^, Boulder belt moraines (abs.):' Ohio Aca Goldthv/ai/aiti , R. P., White, G. W. , and Forsyth, J. L.t 1961, Glacial map of Ohio: U. S. Geol. Surv., Misc. Geol. Investigation Map 1-316. Gooding, A. M. , Thorp, J. , and Gamble, E. , 1959, Leached clay-enriched zones in post-Sangamonian drift of southwestern Ohio and southeastern Indiana: G. S. A. Bull., v. 70, p. 921-926. Janssens, A., 1964, A contribution to the Pleistocene geology of Champaign County. Ohio: uapubl. M.S. thesis, The Ohio State University, 96p. Hill, P. C., 1878, Report on the geology of Champaign County: Geol. Surv. of Ohio, 2nd- Ser. , Bull. 3t p. Horberg, L. , 1950, Bedrock topography of Illinois: 111. Geol. Surv. Bull. 73, p. 41-111. Leverett, F., 1902, The glacial formations and drainage features of the Erie and Ohio basins: U. o. Geol» Surv. Monograph 41, 802p. Morris, S. E, and Spicer? E. C<., 1953, 'jeolpgrif-al ard geophysical study of the p^ef-rlacial Teays Vallsy in v/esc-central Ohio: U. 3» Gecl. Sui-v. V/ater Supply Paper 14-60-E, p. 199-232. Orton. >-. , 1S8B. Tlie Trenton lime stone as a source oi' oil and GC-S in Ohio: Geol. Surv. of Ohio, 2n;I Ser. , v. 6, p. 101-310. Riddell, J. L. , 1836, Raport no. 60 to the 35th General Assembly of Ohio, p. '13. RitchiOt A. and Powell, K. , 1971 » Soil survey cf Champaign County, Ohio: publ. by U.S.D,A. Soil Conaorv. Service in cocp. v;ith Ohio "Dep'C. of Kacural Res. and Ohio Agric, Res. and Dev. Center, 62p. Rosan^reen, T. E. , 1970, The glacial geology of Highland County. Ohio: vmpubl. Ph.D. dissert at ion., Trie Ohio State universityy 1o3p. Stauffer, C. E., 1909, The middle Devonian of Ohio: Geol. Surv. of Ohio, 4th Ser., Bull. 10, 358p. m>>'.?," Steiger, J. R. and Holowayehuk, N., 19?2, Particle-siae and carbonate analysis of glacial"till and lacustrine deposits in v/estern Ohio in Goldthwait, R. £. (ed.)t 1972, Till/a symposium: , p. 275-289. Stout, W. , VerSteeg, K.r ajjd Lainby G. F., 194-3* Geology of water in Ohio .(.a basic report): Geolfc Surv. of- Ohio, Bill. 44, 694p. Teller, J. T. , 1954, The glacial geology of Clinton County, Ohio: unpubl. M.S. thesis. The Ohio State University, 107p. Tight, W. G., 1903, Drainage modifications in south- eastern Ohio and adjacent parts of West Virginia and Kentucky: U. S. G. S. Prof. Paper 15, 19Sp. Wayne, W. J. , 1956, Thickness o^ drift and bedrock physiography of Indiana north of the Wi&consin glacial boundary: Ind. Dept. of Conserv. Geol. Surv. Rept. of Progress No. 7» 32p. —————————, 1953, Early Pleistocene sediments in Indiana: Jour. Geol*, v. 66, p. 8~15» Wilding, L. P., Shafer, G. M., and Jones, R. B., ":964, Morley and Blount'soils: a statistical sivrysy of certain physical and chemical propei'ties of some selected profiles fron Ohio: Soil Sec. Am. Proc., v, 28, p. 674-679. ,stt-:-f?