PLEISTOCENE EVOLUTION of the OHIO and WABASH VALLEYS William J

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11-1952 PLEISTOCENE EVOLUTION OF THE OHIO AND WABASH VALLEYS William J. Wayne University of Nebraska-Lincoln, [email protected]

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Wayne, William J., "PLEISTOCENE EVOLUTION OF THE OHIO AND WABASH VALLEYS" (1952). Papers in the Earth and Atmospheric Sciences. 425. http://digitalcommons.unl.edu/geosciencefacpub/425

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WILLIAM J. WAYNE Indiana University

ABSTRACT Studies of drift thickness and character currently in progress in Indiana indicate changes in drainage that have occurred in Indiana and some adjoining states since the beginning of the Pleistocene epoch. After late Tertiary (Lexington) peneplanation the master-drainage line, the Mahomet-Teays Valley system, became entrenched about 200 feet below its former level before it was ponded by Nebraskan ice and diverted into a new course. During the Parker cycle, which was interrupted by glaciation, the present physiographic features of southern Indiana and their now buried extensions to the north became recognizable. Static rejuvenation then was a major factor in erosion of the "Deep stage" of the Ohio Valley. Reversal of the pre-Illinoian Miami Valley probably resulted from this glaciation also. Further ponding of the Mahomet by Kansan ice and diversion of its drainage down the Wabash Valley is suggested as the origin of the "Deep stage" along that stream. Present drainage in central Indiana is a result of modifications produced by Tazewell and Cary glaciers.

INTRODUCTION for the northern fourth of Indiana have Differences of opinion concerning pre- not been studied. glacial and interglacial stream courses in This investigation is part of a survey the states drained by the Ohio River and of the mineral resources of Indiana and is its tributaries from the north have long being made under the direction of W. D. existed. Recently, a report on the bed- Thornbury, chief of the Glacial Geology rock topography of Illinois has been pub- section of the Indiana Department of lished, in which the evolution of present Conservation, Geological Survey. drainage is discussed and figured (Hor- berg, 1950, fig. 21). A similar study for PREGLACIAL DRAINAGE Indiana currently in progress by the MAHOMET-TEAYS VALLEY writer shows the existence of many pre- Indiana viously unrecorded buried valleys and The main preglacial river of supplies additional data for interpreta- was the Mahomet-Teays, which probably headed in the Piedmont of North tion of the erosional history of the region. This report presents the writer's views Carolina (Stout and Schaaf, 1931, p. 671) of the sequence of changes in the drain- and flowed across West Virginia, Ohio, Indiana, and Illinois (fig. 1). An early ice age basins of the Ohio and Wabash val- sheet caused the first derangement of the leys that resulted from Pleistocene glaciation. Approximately 4,000 water- and river by severing the part called the oil-well records in central Indiana have Teays Valley (Tight, 1903, pp. 50-57, pl. 9) from that downstream. been collected and studied, the thickness Thornbury (1948, p. 1359) suggested of glacial drift plotted on county maps, using the name "Kanawha Valley" for and isopachous contours drawn from this preglacial drainage line. In the opin- these data and outcrop information. Re- ion of the writer the name "Mahomet," fraction seismograph data and well logs proposed by Horberg (1945, p. 349) for 1 Published with the permission of the state geolo- the lower part of the valley which crosses gist, Indiana Department of Conservation, Geo- Illinois to its discharge point on the pre- logical Survey. Manuscript received October 19, 1951. glacial Mississippi, could appropriately 575 576 WILLIAM J. WAYNE be used for the valley across Indiana as former divide near Madison, Indiana. well (fig. 1). The entire preglacial river The Ohio River Valley is extremely nar- valley might well be designated as row there, and the adjacent upland is the "Mahomet-Teays system," but the undissected (Fowke, 1925, p. 87). The shortened interglacial valley of Illinois, upland on the Muscatatuck regional Indiana, and western Ohio (fig. 2) should slope near Madison shows a lack of bevel- be called the "Mahomet" to distinguish ing toward the Ohio River, but beveling it from its longer pre-Pleistocene an- does occur along the Kentucky River and cestor. its supposed continuation northeast from One of the major tributaries of the Madison (Fowke, 1925, p. 89). Beveling Mahomet-Teays system in Indiana ap- toward the Ohio does occur below Madi- pears to have headed in southeastern son (Malott, 1922, p. 138). Many of the Indiana and flowed northwestward to streams which join the Ohio above Madi- join the Mahomet Valley near Lafayette son exhibit a barbed pattern, but those (fig. 1). The name "Anderson Valley" is that enter the Ohio below the old divide suggested for the course of this preglacial show normal relationships (Malott, 1922, river, as Anderson, Indiana, is situated p. 138). "Lafayette" gravels are present on the till plain above it. in quantity along the Kentucky River and along the Ohio downstream from OHIO VALLEY New Amsterdam at the mouth of Indian The pre-Pleistocene Ohio River was a Creek in Harrison County (Leverett, relatively insignificant stream, which 1902, pp. 111-112). The upland is so well probably headed on the Silurian lime- preserved in the Madison area that it is stones2 that underlie the area of the remarkable that they are not now present Muscatatuck regional slope (fig. 3) south- there, if they ever were deposited west of Madison, Indiana. Leverett (Malott, 1922, p. 138). The presumed (1902, pp. 116-118), Fenneman (1916, southwesterly slope does not take into pp. 118-119), Ver Steeg (1938, pp. 657- account the possibility of uplift to the 659), and others thought that the Ohio north following glacial unloading (Ma- headed upstream from Cincinnati. They lott, 1922, p. 138) or the possibility of based their conclusions mainly on the interglacial reversal of drainage in south- fact that the Miami Valley bedrock floor ern Ohio. has a southwest gradient, whereas it In view of the fact that the Mahomet- should have a northeast gradient if it Teays Valley system apparently skirted flowed toward the Mahomet-Teays. Ma- the Cincinnati uplift on the north in- lott (1922, pp. 136-138) and Fowke stead of flowing directly across it, as does (1925, p. 87) favored the view that the the present Ohio River, it would seem Ohio headed near Madison, Indiana, and likely that other drainage also would that the Kentucky River flowed north- have become adjusted to that structure. eastward through the old Miami Valley, The parts of Kentucky, Ohio, and In- which emptied into the Mahomet-Teays. diana underlain by Ordovician lime- Considerable evidence has been of- stones and shales constitute essentially a fered to support the hypothesis of a shallow topographic basin. The lower part of the Kentucky River lies entirely 2 J. B. Patton (personal communication) indi- cates that the formation which generally forms the within this basin and enters the Ohio divide is the Laurel limestone. River above the probable old divide at EXPLANATION -- Accurately located drainage lines ---- Probable drainage lines

0 50 100 150 Miles

FIG. 1.-Principal preglacial drainage systems of Indiana and adjoining states. Compiled from studies by Leverett (1915, 1929), Malott (1922), Stout, Ver Steeg, and Lamb (1943), Fidlar (1948), McGrain (1949, 1951), Horberg (1950), and others.

EXPLANATION - Accurately located drainage lines ---- Probable drainage lines

0 50 100 150 Miles

FIG. 2.-Drainage modifications that resulted from Nebraskan glaciation. Ohio data after Stout, Ver Steeg, and Lamb (1943); Illinois data after Horberg (1950). EXPLANATION

Scale of Miles 0 10 20 30 40 50

FIG. 3.-Physiographic units of southern Indiana, after Malott (1922), and their approximate boundaries where buried north of the Wisconsin glacial boundary. PLEISTOCENE EVOLUTION OF THE OHIO AND WABASH VALLEYS 579

Madison. Leverett (1929, p. 53) indi- LATE TERTIARY EROSION CYCLES cates that the south bluff of the Ohio Indiana and the surrounding area River is composed of glacial till a short were reduced to a gently rolling, old-age, distance above the present mouth of the topographic surface during the latter Kentucky River. On the northwest side, part of the Tertiary, probably in late the basin developed on Ordovician rocks Miocene or Pliocene time. This surface, is rimmed by resistant Silurian lime- the Lexington peneplain, is about 900- stones. Streams that flow westward from 1,000 feet in altitude in the Dearborn up- this scarp enter the Wabash drainage land (fig. 3) of southeastern Indiana, and area; those, such as Laughery Creek and the residual local relief is 100-200 feet. Tanner's Creek, which lie on the eastern The Lexington peneplain sloped north side of the rim of limestone join the Ohio and west toward the major drainage River above Madison (U.S. Geol. Sur- lines. It had an altitude of 700-800 feet vey, Aurora, Indiana, quadrangle). The in Wabash County in north-central In- writer thinks it highly unlikely that a diana (Wayne and Thornbury, 1951, p. small consequent river, such as the pre- 26). The peneplanation probably never glacial Ohio, could have accomplished was so complete that uplands and low- the extensive headward erosion and the lands were unrecognizable. On the con- several piracies necessary to develop a trary, some structural and lithologic con- river that crossed the Cincinnati Arch. trol of topography must have remained. For this reason, in addition to those A new cycle of erosion called the listed above, the writer thinks that the "Parker" began with the late Tertiary preglacial Miami River probably flowed rejuvenation, which caused the streams northeastward and that the Ohio River to entrench themselves 100-200 feet beheaded on the Muscatatuck regional low the level of the peneplain and to de- slope. velop broad floodplains. Lowlands were developed along the outcrop belts of WABASH VALLEY weaker rocks, particularly those tra- Fidlar (1948, fig. 1) considered the versed by major streams. Degradation of preglacial Wabash River to have headed the Scottsburg lowland of southern In- near Covington in Fountain County. diana and its buried northward extension Thornbury (1948, p. 1359) suggested began during this period, as did that of that the Knobstone escarpment formed the Pennsylvanian lowland (Horberg, the preglacial divide in western Indiana 1950, pp. 35-37) of Illinois and Indiana. between the basins of the Wabash and This cycle was interrupted by glaciation. the Mahomet-Teays. The bedrock drain- The present Scottsburg lowland is a re- age pattern which exists in Fountain and sult of degradation throughout the Pleis- Parke counties and the bedrock altitudes tocene. Inasmuch as a major river sys- in the same area indicate that the divide tem, the Mahomet-Teays, crossed north- was more likely about 15 miles south of central Indiana, the northern end of the Covington in northern Parke County lowland should have been eroded more and southern Fountain County. South than the southern end during preglacial of Parke County, the course of the bed- times. Analysis of drift thickness indi- rock Wabash Valley has been described cates the existence of a former broad low- in detail by Malott (1922), Fidlar (1948), land along the outcrop of Devonian and Horberg (1950), and others. Lower Mississippian shales in central In- 580 WILLIAM J. WAYNE diana, where they are deeply buried be- ("Deep stage") took place after the dis- neath Wisconsin glacial deposits. This ruption of the Mahomet-Teays drainage part of the Scottsburg lowland was system and left the Parker strath as a formed between the end of the Lexington terrace above the entrenched rivers. He cycle and the beginning of the Illinoian states (1936, pp. 936-937): "The writer age, and probably the greater part of the believes that the deep, comparatively development took place during Parker narrow valleys buried beneath the glacial time. The southern part of the Scotts- drift of western Ohio and incised below burg lowland has been further eroded an old surface (Parker) were cut during and deepened since the enlargement of Deep-stage time. . . . The Deep stage the Ohio River following Nebraskan lasted from the flood stage of the Teays glaciation. to the advent of the Illinoian glacier." Glaciation caused complications in the Horberg (1950, p. 70) recognized prob- Parker cycle, including drainage diver- able outwash below Aftonian soil in the sions, static rejuvenation, and alluvia- bottom of the Mahomet Valley in Il- tion in the major rivers. The present linois, thus indicating that the erosion rivers in central Indiana follow largely there may have been entirely pre-Pleisto- the courses of Wisconsin or Illinoian cene. sluiceways and in some places show little Thornbury (1948, p. 1359) interpreted or no relation to the bedrock topography. the deep valley across north-central In- Much of the post-Wisconsin drainage is diana as part of the "Deep stage" of the superposed, so that streams now cross Mahomet-Teays drainage system and buried uplands and valleys with little suggested that it was eroded before Il- relationship to either. linoian glaciation by an interglacial river In north-central Indiana the main pre- that headed in western Ohio. glacial rivers appear to have been deeply It is entirely possible that the "Deep entrenched below broad valleys that stage" of the Mahomet-Teays Valley is were about 100 feet below the level of the pre-Pleistocene. Where the Teays dis- Lexington peneplain. The bedrock sur- appears beneath glacial drift near Chil- face slopes gently toward these valleys, licothe, Ohio, its bedrock altitude is 620 the dissected remnants of which have feet (Stout and Schaaf, 1931, p. 665). been interpreted as strath terraces repre- The wide bench above the deep valley in senting the Parker cycle (Wayne and Wabash County, Indiana, which has Thornbury, 1951, p. 29). The writer now been interpreted as part of the same val- thinks that these old-age valleys more ley floor as that in southern Ohio (Wayne likely are simply the broad troughs and Thornbury, 1951, p. 29) is about 600 through which rivers flowed across the feet above sea-level. The length of the Lexington peneplain. valley between Chillicothe and the western edge of Wabash County is at least DEVELOPMENT OF THE DEEPLY 210 miles, and the stream course prob- INCISED VALLEYS ably was closer to 300 miles long. The Several differences of opinion have middle reaches of this river, therefore, arisen concerning the age of the deeply would seem to have had an average gra- entrenched bedrock valleys. Ver Steeg dient of less than 2 inches per mile, a con- (1936, pp. 935-936) suggested that the clusion that is improbable. Differential deep erosion along the major valleys rates of uplift could have caused such a PLEISTOCENE EVOLUTION OF THE OHIO AND WABASH VALLEYS 581 gradient, but, if uplift occurred, its ef- an age. Thwaites (1947, pi. 3) interprets fects should be noticeable in steepened these boulders as Nebraskan in age. gradients of eastward-flowing streams Diversion of so large a river as the and lessened gradients of other west- upper part of the Mahomet-Teays into flowing streams in Indiana. Such phe- the Ohio Valley most certainly would nomena have not been observed. The have caused static rejuvenation to take deepest part of the Mahomet-Teays Val- place and rapid regrading to occur along ley in Wabash County, Indiana, is about that valley (Malott, 1922, p. 170). Glaci- 410 feet in altitude, or 210 feet lower ation of the duration necessary to de- than at Chillicothe, Ohio, which would range the Mahomet-Teays system per- provide a maximum average gradient of manently could likewise have caused re- 12 inches per mile. Horberg (1945, p. versal of drainage in the preglacial Miami 359) calculated the average gradient of Valley of southwestern Ohio, which, in the Teays-Mahomet Valley between cutting in accordance with the deepened Chillicothe, Ohio, and Tazewell County, Ohio River, would have developed the Illinois, as 7 inches per mile; and Stout, observed southwesterly gradient of the Ver Steeg, and Lamb (1943, p. 53) cal- Miami bedrock valley. A narrow but culated the gradient of the valley across deep buried trench that is intersected by Ohio as 12 inches per mile. For compari- the present Whitewater River at Con- son, the average gradient of the present nersville, Indiana, may have been formed Ohio River from the mouth of the Miami at the same time by overflow waters im- River to its junction with the Wabash pounded in Anderson Valley. Well cut- River is 4 inches per mile. tings show that lacustrine clays more It seems rather unlikely that, after than 160 feet thick lie beneath Wisconsin ponding and derangement of the Maho- till in Anderson Valley, but data are in- met-Teays drainage system and diver- sufficient to determine whether this en- sion of the upper part over a divide into tire thickness represents one or more the Ohio Valley (fig. 2), the beheaded re- than one glacial stage. The relatively mains of the Mahomet River somewhere soft Ordovician shales in the Cincinnati in west-central Ohio could have been area would have allowed fairly rapid re- capable of entrenching itself deeply be- duction of interstream areas to conform low its former level. Instead, one would to the new stream orientation. Thus the expect some aggradation by the underfit deep erosion ("Deep stage") of the Ohio river after such a loss of volume. More River seems to be post-Nebraskan in age. likely, little or no deepening of the What appears to be a "valley-in-val- Mahomet Valley could have occurred ley" profile along the Mahomet-Teays in after it was shortened. western Ohio and in Wabash County, In- The precise glaciation that caused the diana, may be a result of only one en- ponding of the Mahomet-Teays drainage trenchment rather than two. The rivers system has not been determined. Lever- that crossed the gently rolling Lexington ett (1929, fig. 3), described partly de- peneplain in late Tertiary time undoubt- composed erratics at various locations in edly flowed through broad valleys and Kentucky. As rafting by icebergs does were somewhat below the level of the in- not satisfactorily account for all the terstream areas. Following uplift, these boulders, Leverett (1929, p. 33) postu- rivers became deeply entrenched below lated an extensive ice sheet of pre-Illinoi- their old floodplains. 582 WILLIAM J. WAYNE

The steep sides that occur along the Mahomet River was insignificant as a bedrock valleys in east-central Indiana drainage line across Illinois after Kansan probably result from the greater resist- glaciation. Outwash gravels and sands ance to erosion of the Niagaran lime- are extensive along the Mahomet Valley stones of the region as compared with in Indiana and indicate that it was a shales both east and west of that part of sluiceway until late Tazewell time in this the Cincinnati and Wabash arches. The state. A possible explanation for the valley floor had reached a stage of early presence of abundant outwash in Indiana maturity. Strath terraces have not been and its absence in Illinois is suggested by

EXPLANATION - Accurately located drainage lines ---- Probable drainage lines

FIG. 4.-Drainage modifications that resulted from Kansas and Illinoian glaciations. Ohio data after Stout, Ver Steeg, and Lamb (1943); Illinois data after Horberg (1950). found along the upper reaches of the the deep erosion ("Deep stage") along Anderson Valley (fig. 1). In its lower the Wabash Valley that seems to extend reaches, this valley passes through De- north to the Mahomet Valley. At one vonian and Mississippian shales that un- time Fidlar (1943, p. 415) thought that derlie the Scottsburg lowland, and the the deep Mahomet-Teays Valley across river was able to erode a much wider Indiana was a continuation of the Wa- valley than in limestone. bash. Certainly the divide between the Horberg (1945, p. 354) drew general- two drainage systems must have been ized contours on the Sangamon inter- low. Kansan ice may have impounded glacial surface of weathering in central water in the Mahomet Valley above Illinois. On the basis of this map and on Warren County, Indiana, and diverted the lithology of well cuttings along the the drainage of the upper part of the Mahomet Valley, he concluded that the basin into the Wabash Valley (fig. 4). A PLEISTOCENE EVOLUTION OF THE OHIO AND WABASH VALLEYS 583 buried valley that contains considerable mouth time as a result of an increase in outwash crosses the bedrock valley of the volume from diversion of part of the Wabash in northern Vermillion County. Mahomet River. This valley is relatively narrow and is a continuation of buried Danville Valley in LATE PLEISTOCENE VALLEY-FILLING Illinois (Horberg, 1951, p. 71). Static re- The extent of Illinoian glaciation in juvenation would have caused the overfit Indiana has been discussed thoroughly river to begin cutting its course to grade by Leverett and Taylor (1915), Malott immediately. Such a history could ex- (1922), Thornbury (1937), and others. plain the peculiarity of the deeply en- Some of the more important events that

EXPLANATION - Accurately located drainage lines

FIG. 5.-Principal post-Wisconsin drainage systems of Indiana and adjoining states trenched bedrock valley that appears to took place during this glacial age were head so close to a major preglacialriver. the beginning of extensive deposition Presence(reported by well-drillers)of silt along the Ohio River and many of its and fine sand in the Mahomet Valley in tributaries, and continued filling of the Tippecanoe, White, and Carroll coun- Mahomet and its tributaries with till and ties, Indiana, and exposuresof thick out- glaciofluviatile deposits. As much as 160 wash deposits overlainby till in Fountain feet of calcareous lacustrine clay was de- and Warren counties, Indiana, support posited in Anderson Valley, most of it this interpretation, but data are ad- probably during Illinoian time. Malott mittedly inconclusive. Much of the (1922, pp. 140-141) suggested that the "Deep stage" of the Wabash Valley, ac- great volume of Illinoian and Wisconsin cording to this interpretation, would outwash enlarged the Mississippi delta have been cut during Kansan and Yar- and thereby forced the Mississippi River 584 WILLIAM J. WAYNE

and its tributaries to aggrade their val- Miami. Erosion of the "Deep stage" of leys. This may have been a contributing the Ohio Valley next occurred in post- factor, along with the rising sea-level dur- Nebraskan time (Aftonian, possibly ing deglaciation (Turnbull, Krinitzsky, longer), when the Mahomet became an and Johnson, in: Trask, 1950, p. 210). underfit stream that headed in western Early Wisconsin (Tazewell) ice pro- Ohio. Later the upper Mahomet prob- vided great quantities of outwash, which ably was diverted into the Wabash Val- aggraded major sluiceways, such as the ley as a result of Kansan glaciation, and Ohio and Wabash rivers (Fidlar, 1948, the "Deep stage" was cut along the pl. 3). The upper Wabash apparently lower Wabash in Yarmouth time. Exten- still followed the course of the ancient sive valley-filling in all the "Deep-stage" Mahomet as far as Lafayette. A read- valleys of the Mississippi River and its vance of the ice covered the thick out- tributaries began during the Illinoian wash with till, and, when the ice melted, age. The remains of the Mahomet drain- the upper course of the present Wabash age line in Indiana was obliterated by was established (fig. 5; Wayne and Wisconsin (Tazewell) glacial deposits, Thornbury, 1951, p. 32). and many of the present valleys in north- central Indiana were eroded along melt- SUMMARY water drainage lines established during The deep valley ("Deep stage") of the the Wisconsin glacial retreat. Mahomet-Teays across Illinois, Indiana, and western Ohio was eroded contem- ACKNOWLEDGMENTS.-Thelate C. A. Malott poraneously with the surfaces in the and John B. Patton, chief of the Industrial abandoned reaches of the Teays drainage Minerals Section of the Survey, provided system in Ohio and West Virginia and counsel as the work progressed. Preston Mc- Grain, of Geological probably was preglacial. A lobe of the the Kentucky Survey, permitted access to a preliminary unpublished Nebraskan glacier ponded and diverted regional map which he had prepared of drift the upper Mahomet-Teays into the thickness in the upper Wabash Basin. Leland Ohio Basin, the Minford silts were de- Horberg, University of Chicago, and Karl Ver posited, and the direction of flow was Steeg, College of Wooster, kindly read and reversed in some tributaries, such as the criticized the manuscript.

REFERENCES CITED

FIDLAR,M. M. (1943) The preglacial Teays Valley --- (1915) The Pleistocene of Indiana and in Indiana: Jour. Geology, vol. 51, pp. 411-418. Michigan and the history of the Great Lakes: --- (1948) Physiography of the lower Wabash ibid., Mon. 53, 529 pp. Valley: Dept. Conservation, Indiana Div. (1929) Pleistocene of northern Kentucky: Geology Bull. 2, 112 pp. Kentucky Geol. Survey, ser. 6, vol. 31, pp. 1-80. FowKE, GERARD (1925) The genesis of the Ohio C. A. (1922) The physiography Indiana; River: Indiana Acad. Sci. Proc., vol. 34, pp. 81- MALOTT, of 102. in: Handbook of Indiana geology: Indiana Dept. Conservation, Div. Geology Pub. 21, pp. 59-256. HORBERG, LELAND(1945) A major buried valley in east-central Illinois and its regional relationships: MCGRAIN, PRESTON (1949) Ground water re- Jour. Geology, vol. 53, pp. 349-359. sources of Henry County, Indiana: Indiana (1950) Bedrock topography of Illinois: Acad. Sci. Proc., vol. 58, pp. 173-187. Illinois Geol. Survey Bull. 73, 111 pp. --- (1951) Thickness of glacial drift in north LEVERETT,FRANK (1902) Glacial formations and central Indiana: Indiana Flood Control and drainage features of the Erie and Ohio basins: Water Resources Comm. Circular No. 1. U.S. Geol. Survey Mon. 41, 802 pp. STOUT, WILBUR, and SCHAAF, DOWNS (1931) Min- PLEISTOCENE EVOLUTION OF THE OHIO AND WABASH VALLEYS 585

ford silts of southern Ohio: Geol. Soc. America TIGHT, W. G. (1903) Drainage modifications in Bull. 42, pp. 663-672. southeastern Ohio and adjacent parts of West ----; VER STEEG, KARL; and LAMB, G. F. Virginia and Kentucky: U.S. Geol. Surv. Prof. (1943) Geology of water in Ohio: Ohio Geol. Paper 13, 111 pp. Survey Bull. 44, 4th ser., 694 pp. VER STEEG,KARL (1936) The buried topography THORNBURY,W. D. (1937) Glacial geology of of western Ohio: Jour. Geology, vol. 44, pp. southern and south-central Indiana: Indiana 918-939. Dept. Conservation, Div. Geology Pub., 138 pp. --- (1938) Thickness of the glacial drift in --- (1948) Preglacial and interglacial drainage western Ohio: ibid., vol. 46, pp. 654-659. of Indiana (abstr.): Geol. Soc. America Bull. 59, WAYNE, W. J., and THORNBURY, W. D. (1951) p. 1359. Glacial geology of Wabash County, Indiana: THWAITES,F. T. (1947) Outline of glacial geology, Dept. Conservation, Indiana Geol. Survey Bull. Ann Arbor, Edwards Bros., 119 pp. 5, 39 pp.