DESCRIPTION OF THE PATOKA QUADRANGLE.

By Myron L. Fuller and Frederick Gr. Clapp.

GENERAL RELATIONS. many of the smaller streams underwent important In addition to the high upland level just very uniform, being a little over 400 feet above the modifications in consequence of the obstruction of described there appear to be traces of old land sur­ sea in the higher portions of the Wabash flats at the The Patoka quadrangle is located in southwest­ their valleys by the ice sheet or of the deposition faces at lower levels, for there are a number of northern edge of the quadrangle, and about the ern Indiana and southeastern Illinois. Its southern of glacial materials by the ice or by streams associ­ rather extensive crests or flats shown by hills at same in the White and Patoka river bottoms. boundary is only about 2 miles from the Ohio ated with its occupancy. In fact, the Wabash and elevations of 480 to 520 feet, especially at 500 feet. There is, however, a gentle slope southward to & River at Evansville, and its northwest corner is White rivers and Bonpas, Flat, and Big creeks Many of these flats have been found to be com­ 370-foot level at the southwest corner of the about 17 miles west of the Wabash River, which are the only large streams in the quadrangle that posed of stratified marl-loess overlying a rugged quadrangle. The low rate of fall has led to the marks the boundary between the States of Indiana follow their pre-Glacial valleys, and the positions of topography, as in the regions south of New development of meanders, which, because of their and Illinois. It embraces the area between lati­ all these except the latter have been more or less Harmony, while others have proved to consist of resistance to the free flow, cooperate with it in tude 38° on the south and 38° 30' on the north, modified by glacial or other Quaternary deposits. till or other drift deposits. There are apparently, giving rise to annual overflows that cover all but and between longitude 87° 30' on the east and 88° however, many more or less flat rock surfaces at or the higher portions of the adjacent flats to depths RELIEF. on the west, and includes one-fourth of a square near the same elevation, which may indicate a of several feet. This frequent overflow leads to degree of the earth's surface. Its north-south The Patoka quadrangle exhibits four rather dis­ second and later plain that was formed at an ele­ many changes in the courses of streams, and length is 34.5 miles, its breadth 27.2 miles, and its tinct types of topography: (1) Rugged uplands, vation of from 100 to 150 feet below the first. If bayous and abandoned channels are common. area about 938 square miles. It comprises four (2) rolling uplands, (3) upland plains, and (4) such a plain existed it was probably much less per­ 15-minute quadrangles the Mount Carmel, Prince- river flats. The last two resulted from the accu­ fectly developed, and it seems likely that in this GEOLOGY. ton, New Harmony, and Haubstadt and includes mulation of unconsolidated material in relatively region it was generally confined to the areas bor­ STRATIGRAPHY. by far the larger portions of Vanderburg, Posey, recent geologic times, while the first two, which dering the main drainage lines. and Gibson counties and part of Knox County, in embrace by far the greater part of the area, have Rolling uplands. In this class are included the Derivation of the rocks. The rocks exposed at Indiana, and nearly the whole of Wabash and resulted from the action of stream erosion upon lower and less rugged upland surfaces. The hills the surface of the Patoka quadrangle are of two parts of Edwards and White counties in Illinois. the hard rocks. The resistance of these rocks to are generally much smaller than in the previous types. They include not only those firm, hard The principal cities and towns included in the area erosion has been very nearly the same throughout group. Their altitude seldom exceeds 550 feet, beds which every one at once recognizes as rock, but are Princeton, Mount Carmel, Grayville, New the quadrangle, the consequent relief depending, and they usually exhibit smooth, gently rounded also the loose, unconsolidated deposits of silt, sand, Harmony, Owensville, Hazleton, Patoka, Fort therefore, upon the relations of the surface to the forms. The valleys are broad and relatively shal­ glacial till, etc., likewise considered by geologists as Branch, Haubstadt, Cynthiana, and Poseyville. drainage lines. low, showing gentle curves in cross section, and are rock, which occur as fillings in the valleys or as a The name of the quadrangle is taken from Patoka The general rule that the larger the stream the characterized by the low pitch of their streams, and mantle of greater or less thickness over the general one of the larger of the towns whose names have more will the surface of the adjoining areas suffer by broad, flat divides. The rolling uplands are surface of the quadrangle. not already been used for the smaller quadrangles. reduction to low and rounded forms holds good best developed in the vicinity of the older drainage The materials of which the harder rocks are within the quadrangle, except where alterations lines, especially in the region west of the Wabash composed were in the main originally derived, in TOPOGRAPHY. were effected in the drainage system through the River. The Claypole, Gordon, Mumford, Foots the form of gravel, sand, mud, etc., from the wear­ influence of the Pleistocene ice invasion. Among Pond, and other hills projecting above the Wabash ing away of some old land mass under the action DRAINAGE. exceptions of this nature is the narrow valley, with flats are to be classed in this type in part, although of streams or waves, the resulting waste being car­ All of the drainage from the surface of the rock outcrops at short distances on either side, the flatter portions of their tops belong to the ried to the margin of the seas then existing and Patoka quadrangle finds its way to the Ohio River. through which the Patoka River flows near Patoka, group next to be described. The sand hills along there deposited as stratified, sedimentary, or frag- A small area in the southeastern part of the quad­ and the narrow valley south of the Illinois Central the eastern border of the Wabash flats, the rock mental rocks. As time has elapsed these beds have rangle is drained directly into the Ohio by Pigeon Railroad, through which flows Big Creek. On the hills southeast of Hazleton, around Owensville, been gradually solidified by the chemical deposi­ Creek, but the remaining portions of the area are other hand there are broad and deep rock valleys, and along Big Cr^ek, and the morainal ridges tion of matter about the grains of which they are drained by streams mat flow first into the Wabash, now obstructed by drift or sand, in which streams between Princeton and Fort Branch, southeast of composed, the material thus deposited acting as a in the western portion of the quadrangle, and are insignificant or wanting. Such valleys occur Owensville, and near Poseyville and Cynthiana cement to bind the grains together into a solid thence south to the Ohio. The Wabash River is among the rock hills lying south of Hazleton and belong in the main to the rolling uplands, though mass. Besides the materials derived 'from older a broad stream, in some places over a third of a north of Patoka, southwest of Princeton and north­ the steeper portions approach the previous class in land masses, beds of shells and marls, sometimes mile wide, and next to the Ohio River is by far east of Owensville, and north and south of Cyn­ ruggedness. many feet in thickness, were formed beneath the the most important drainageway in the region. thiana. Both phases of discrepancy are due to the Upland plains. The upland plains consist of sea, and beds of peat accumulated in the swamps It enters the quadrangle from the north at a point closing of old valleys by drift during the ice invasion broad, flat, or gently sloping surfaces standing at and basins along its borders. The former, like the about 4 miles east of the center and flows in a gen­ and the consequent deflection of the streams into an elevation of 500 feet or less and composed of fragmental rocks, were cemented largely by the eral southwesterly direction to Grayville, near the new courses, where they have not yet materially deposits that accumulated during the period of the chemical deposition of matter between the compon­ middle of the western border, whence-it runs in a widened their valleys. ice invasion or of loess or marl-loess deposited at a ent grains, while the latter gradually became hard­ very irregular course so nth ward and southwest- Rugged uplands. In the group designated rugged later period. The drift deposits are limited to the ened to their present form through the loss of their ward, finally passing out of the quadrangle "a little uplands are included the highest hills and ridges sloping drift plains east of the Princeton-Fort volatile and unstable portions by oxidation, only the ov^r 3 miles from its south west corner. The next of the quadrangle. The type is developed on both Branch moraine, the similar drift plains southwest carbon and its more stable compounds remaining. most important stream is the White River. This the drift and the rock hills, the former being most of Fort Branch, and a few flat hilltops of the The materials of the unconsolidated or surficial river enters the quadrangle near its extreme north­ conspicuous in the region north of Patoka and the Mount Carmel quadrangle, where the rock is at no rocks were derived from the underlying consolidated east corner, and flows with a course about S. 60° W. latter in the region north, northeast, and east of place far from the surface. rocks or from other rocks lying north of this area, until it joins the Wabash near Mount Carmel. It Princeton and (in the area between Big Creek The most conspicuous of the upland plains are some from sources even as far distant as Canada. receives no tributaries of importance within this and the eastern e'dge of the quadrangle. In the the broad level or gently sloping marl-loess flats In part these materials were laid down by streams area. The Patoka River, which in size comes next latter area ridges several miles long, with moder­ along the east side of the Wabash Valley south of and rivers, and in part by the direct action of an to the White River, enters the quadrangle about 5 ately uniform crests, are numerous. As a rule, the Black River and the smaller flats of the same ice sheet which was similar to that now covering miles south of the northeast corner, and flows in a they are sharp and narrow and are characterized by material southwest of Mount Carmel, on Mumford, the surface of Greenland, arid which in the early general westerly direction, joining the Wabash steep slopes, which are cultivable only .with diffi­ Foots Pond, and Claypole hills, and at points near part of the present geologic period started in the. about a mile south of the mouth of the White culty. The minor channels, which are exceedingly Owensville and Hazleton. These marl-loess flats far north and spread out over nearly the whole River, near Mount Carmel. Like the White numerous, are usually more or less V-shaped and lie at a maximum elevation of 500 feet above sea of the northeastern portion of North America. River the Patoka receives few tributaries of import­ are separated from one another by equally sharp level or about 120 feet above the Wabash bottoms. The Patoka quadrangle is located at the outer ance in the quadrangle. Of the minor streams divides. In their upper courses they exhibit steep They frequently exhibit floor-like flats at this alti­ limit reached by the ice sheet in this region, the Black River, entering the Wabash from the east descents. tude, although sloping terraces, as in the Mumford boundary entering it from the east near Pigeon about 3 miles north of New Harmony, Bonpas In the Ditney quadrangle, which is immediately Hills and along the north side of Big Creek, are Creek, and passing southwrestward to a point about Creek, entering the Wabash from the north at east of the Patoka, the higher points of the more common. 14 miles north of the southwest corner. The south­ Grayville, Fox River, joining the Wabash from uplands rise, to nearly uniform elevations of from River fiats. All of the rivers and large streams, ernmost point reached is in Illinois some distance the west near New Harmony, and Big Creek, 600 to 640 feet, and are believed to be the remnants and also many of the minor streams, flow through west of the quadrangle. The materials deposited which drains the south-central portion of the of an old surface, almost a plain in character, broad, flat plains of silt or of sand and gravel, by the ice or by the water flowing from it probably quadrangle, are the most important. which once extended over the whole of this region. which are generally overflowed, at least in part, do not anywhere in the quadrangle reach a thick­ Before the advent of the great ice sheet which, In the Patoka quadrangle, however, owing to the each spring. Wells sunk for water show that the ness of much more than 200 feet, while the depos­ in relatively late geologic time, covered the north­ greater maturity of the drainage, the reduction is thickness of these silts and sands ranges from a few its laid down since the disappearance of the ice ern portion of the quadrangle and the region to more complete, only an occasional peak rising to feet in the minor valleys to 150 feet or more in the are of slight importance, except the marl-loess the north, the rivers showed in their broader rela­ the 600-foot level. The hills on which the Prince- valleys of the Patoka and Bonpas Creek. No deep deposits along the eastern borders of the Wabash tions a noticeable conformity with the geologic ton standpipe is built rise to 610 feet, those on the wells are known in the portion of the Wabash or Valley and the plains and dunes of the Wabash and structure. The Wabash River flowed, in a general Petersburg road, 2 miles north of the same city, to White River flats lying within the quadrangle, but White river valleys. Even these are supposed to way, near the center of the broad, low, synclinal 645 feet, those north of Maxams station, southeast the thickness of the deposits is probably 200 feet have been connected with later invasions which, trough constituting the coal basin of Illinois and of Princeton, to 625 feet, and that northeast of St. or more. In the process of the upbuilding of this though furnishing material to the waters of the Indiana, while the Ohio and the tributaries of the Joseph to 605 feet. The development of the plain considerable thickness of sediments the minor region, did not actually reach the Patoka quad­ Wabash in Indiana followed courses roughly of which these hills are supposed to be remnants is hills and valleys have been entirely obliterated, rangle. parallel with the dips. The pronounced drainage considered in detail under the heading "Geologic only the higher prominences rising as "islands" The older consolidated rocks reach a thickness features have survived to the present time, but history," p. 6. above the flats. The general level of these flats is in southwestern Indiana of several thousand feet, though probably not more than 400 feet are nearly 120 feet of the formation is exposed. The from a compact to a fossiliferous fragmental texture.- section, measured along the railroad south of the exposed in this quadrangle. These strata exhibit coal is here reported in wells at 50 feet below the The bedding planes are frequently 3 or more feet deep cut northeast of this town, shows the charac­ many alternations of sandstones, shales, limestones, flood plain, making the total thickness of the for­ apart, giving rise to large blocks on weathering. ter of the formation at this point very perfectly: and coals, but they may be grouped by their litho- mation about 170 feet, or 20 feet greater than at It has undergone some solution along joint planes, Section of Inglefleld formation near St. Joseph. Lynville, Warrick County, where one of the best the widening being sufficient in cases to cause a logic characters into five formations, which, in Feet. ascending order, are the Millersburg, Somerville, exposures is found. The name is that used in the settling of the overlying shales into the cavities, Unexposed interval below Parker coal ...... 40 Ditney, Inglefield, and Wabash. Certain beds of Ditney folio. forming "dikes" of shale fragments (fig. 7). Sandstone, soft and sometimes shaly...... 20 Clay shale, bluish ...... 5 the last named, though not warranting designation This appears to be one of the most variable of Ditney formation. The Ditney formation Sandstone, soft, buff ...... 10 as formations, are nevertheless very persistent, espe­ the formations of this region, the wells or borings, embraces all beds from the top of the Somerville Sandstone, highly ferruginous and honeycombed with cavities left by solution of calcareous fossils...... 11 cially in the southern portion of the quadrangle, even where close together, often showing marked formation to the base of the Inglefield sandstone. Shale, light argillaceous to sandy...... 3 and in the case of the coals, are mapped. All variations in character of materials penetrated. It appears to be composed of the ordinary succes­ Shale,sandy...... 3 of the formations belong to the Pennsylvanian or Complete sections of the formation are afforded by sion of sandstones, shales, and coals, so character­ Sandstone, light, micaceous, and shaly...... 5 Shale, bluish gray...... 8 "Coal-Measure" series of the Carboniferous system. the borings and shaft at Princeton (see section istic of all Carboniferous formations, although in Sandstone, white...... 1 Their general characters and relative thickness are sheet), but in the southern portion of the quad­ general the shale predominates. A typical section Shale, light, argillaceous ...... 10 described in some detail in the following para­ rangle, where the formation is at the surface, no is shown by the following well record at St. James: Sandstones, light, and friable, coarser near bottom... 40+ 146+ graphs, and are shown graphically in the geologic detailed sections could be obtained. The following Section of Ditney formation in well at St. James. column at the end of the folio. section, taken at the Ingleside mine, Evansville, Feet. Owing to the massive character of the sandstone General geologic relations. While in a broad about 2 miles south of the southern border of the Shale 30 Rotten coal...... 1 beds in its lower portion, outcrops of the Inglefield way it is possible to consider the geologic basin of quadrangle, gives all but the upper few feet of Good coal (Ditney coal) ...... 2 formation are more common than those of most the Mississippi region as coextensive with the the formation, while the generalized section shows Clay shale...... 12 other formations. In the valley east of St. Joseph physiographic basin, the former has less unity than the character of the upper 86 feet. In the northern portion of the quadrangle, east it outcrops as a series of cliffs showing an aggre­ the latter. During very early geologic time, how­ Section in Ingleside shaft, E-oansmlle. ] of Hazleton, sandstone begins within a short gate of 60 feet of sandstone. The faces of these ever, and throughout many subsequent geologic Thickness. Depth. interval of the limestone, the Ditney formation, if cliffs are frequently vertical and are often marked periods, the larger part of the south-central portion Feet. Inches. Feet. Inches. Clay and alluvial sand...... 29 0 29 0 present, being limited to a thickness of a few feet. by cavities and other sculptural effects resulting of North America was covered by a sea which Clay and shale...... 61 0 90 0 At Townsend's quarry, north of Princeton, and in from disintegration due to the action of the weather. extended from the region of the Gulf of Mexico on Shaly coal and fire clay ...... 3 0 93 0 the wells in and near the town, a considerable The sandstones are, in large part, of a buff color, Sandstone ...... 4 6 97 6 the south to that of the Great Lakes on the north Siliceous clay shale ...... 12 9 110 3 thickness of the Ditney shales is found, together though gray or even nearly white varieties were and from near the eastern limits of the Appa­ Shale and ironstones...... 5 8 115 11 with an included coal, as at St. James and else­ noted. Some of the beds are brownish, but the lachian Mountain system on the east to the Rocky Fire clay...... 10 116 9 Ferriferous sandstone ...... 7 9 124 6 where. East of Haubstadt the formation is about darker red, brown, or purplish tints are usually Mountain region on the west. Over the bottom Fire clay with sandstone iron.... 12 3 136 9 50 feet thick, but its thickness decreases rapidly of local occurrence and are evidently the result of of this broad basin there were deposited beds of Sandstone (ferriferous) ...... 12 1 148 10 weathering. The name of the formation is taken Shale...... 1 0 149 10 southward, being 45 feet near St. James, 40 near sedimentary rocks, including limestones, shales, Sandstone ...... 7 5 157 3 Staser, and 20 at Inglefield. A mile and a half from Inglefield, a station on the Evansville and sandstones, and conglomerates, the limestones pre­ Millersburg coal ("Coal VII" or south of Inglefield the Inglefield sandstone rests Terre Haute Railroad about 7 miles north and 3i " Little Newburg")...... 2 11 160 2 dominating among the lower beds and the sand­ directly on the limestone, and from here southward miles west of the southeastern corner of the quad­ stones among the upper, and the whole probably Generalized section of upper part of Millersburg formation. to the southern limit of the quadrangle it continues rangle, just south of which the sandstone, with reaching a total thickness of from 4000 to 5000 Thickness Depth probable basal unconformity, is well exposed in the in feet. in feet. to hold this relation, except at a few points where feet. These rocks were originally deposited in a Light clay shale ...... 10 10 4 or 5 feet of the Ditney shales intervene. West railroad cut (see figs. 2 and 6). It has been corre­ horizontal position, but were afterward subjected Fine brownish sandstone...... 7 17 lated by the State survey with the Merom sand­ Sandstone (reported in well)...... 5 22 of the Illinois Central Railroad, however, the shale in places to broad, gentle warpings, giving rise Clay shale...... 5 27 is more persistent, though it is usually not over 5 stone, formerly quarried near the village of Merom, to broad, low rock domes, from which the beds dip Greenish clay shale...... 5 32 to 10 feet in thickness. Sullivan County, Ind., and this name has been gently away into basins that, are equally extensive Clay shale (reported in well)...... 8 40 Soft, sandy, greenish to bluish shale with nod­ The sudden replacement by the massive Ingle­ used in the reports of the Indiana survey since and equally shallow. The Patoka quadrangle is ules of iron ore...... 10 50 field sandstone of the thick shale bed that persists 1870. Recent field work, however, has served to situated a little to the east of the center of such Blue clay shale...... 8 58 Clay shale...... 5 63 from north of the Patoka River to Inglefield a throw grave doubts upon the exactness of the cor>- a broad, shallow basin, which lies between a broad Hard, gray sandstone ...... 3 66 replacement that takes place within a horizontal relation, and the name Inglefield has therefore been dome known as the Cincinnati anticline on the east Sandstone (reported in well)...... 20 86 given to the formation. In the southwestern por­ Blue shale...... 10 96 distance of not more than 75 to 100 feet in the and a similar low, flat dome in Missouri. This railroad cut south of Inglefield (fig. 2) and the tion of the State it appears to have an average basin is known as the Illinois-Indiana coal basin Somerville formation. The Somerville formation thickness of from 110 to 150 feet. (fig. 1), and into it the rocks dip gently from all in general is essentially a double bed of hard lime­ Wabash formation. In this formation are stone with a parting of shale. The name is that included all of the shales and sandstones, with an used in the Ditney folio. The formation outcrops occasional thin limestone or coal, lying above the FIG. 2. Sketch section showing probable erosion uncon­ along the eastern border of the quadrangle from formity between the Ditney and Inglefield formations in top of the Inglefield formation within the limits its southern limit to the vicinity of Pigeon Creek railroad cut at Inglefield, Ind. of the Patoka quadrangle. The generalized sec­ east of Haubstadt. From here there is a break in Cd, Ditney formation; ci, Inglefleld formation. » tion given below, measured from the top down­ the rock hills to a point east of Princeton, and patchy character of the shales throughout the south­ ward, indicates the character of the formation. again from the Patoka River to near Hazleton. eastern portion of the quadrangle (fig. 3) lead to The Parker coal, with overlying black shale and The limestones outcropping in the creek bottoms the belief that there was probably an erosion inter­ limestone, though each is occasionally absent, con­ 2 miles northeast of Princeton and at the foot of val between the deposition of the Ditney and the stitutes a persistent horizon which has been chosen the bluff about the same distance east of Hazle­ overlying Inglefield sandstone. This erosion inter­ as that of demarcation between the Inglefield and ton probably belong to the Somerville formation, val has been correlated by the Indiana geological Wabash formations. Its outcrop outside the drift although the beds can not be actually connected survey with the marked unconformity at the base area is shown on the geologic map, but inside the with the undoubted outcrops of the formation of the Merom sandstone in Parke, Fountain, and drift limits it is difficult to trace. The thin coal found farther south. Vermilion counties, 111., but the correctness of the about 70 feet above the river at Patoka, the coal at

Inglefleld formation. Ditney formation.

Somerville formation.

FIG-. 3. Sketch section showing relations of Somerville, Ditney, and Inglefield formations in exposure 1 mile northwest of Zipp, Ind. The Ditney formation here has a sandstone parting with irregular or unconformable relations.

The following sections show the character of the correlation can not be determined until the inter­ Generalized section of the Wabash formation. formation at different points: mediate area has been mapped in detail. Feet. Inglefield formation. The Inglefield formation Sandstone ...... 15 FIG. 1. Outline map showing the relations of the Patoka Section in Kurtz well, northeast of Princeton Shale, etc. with 6-inch local coal ...... 20 quadrangle to the Illinois-Indiana coal field. (sec. 5, T. 2S.,K. 10 W.). includes the prevailingly sandy beds lying between Sandstone, heavy bedded...... 15 The coal field is represented by the obliquely ruled area. Feet. the top of the Somerville formation and the Shale, part not seen ...... 25 Limestone in bands...... 15 Shale, siliceous ...... 8 directions. In the Patoka quadrangle the rocks Clay shale...... 8 Parker coal, at the base of the Wabash formation. Shale, blue and argillaceous...... 8 Gray limestone...... 2-J belong to the upper (sandy) portion of the great At the base there is always a massive sandstone, in Limestone, soft and shaly to very hard ...... 4 Aldrich coal ...... 1 series of sediments occupying the Mississippi Basin, Section in Hoffman well, Fort Branch. some places having a thickness of at least 60 feet, Feet. Coaly shale ...... 2 and present a dip to the west averaging about 17 Limestone ...... 8 as in the series of bluffs in the valley east of St. Fire clay ...... 1 ~ , , , , , . , , } Sandstone of ( 0 Clay shale and fire clay...... 18 Joseph. This basal sandstone, however, is fre­ Sandstone, soft and sometimes shaly / HT * -, \ 8 feet per mile. c, , , ' ,, .. .,.,. - Mumford -< on Limestone ...... 8 quently replaced by a number of thinner beds Sandstone, locally poikihtic...... I , , / 20 Carboniferous System. J ^ } Hills, etc. t Section along creek 3 miles east of Staser. separated by a few feet of shale. In most of the Limestone, hard, gray, and fossiliferous...... 3 Feet. Shale, black...... 3 Millersburg formation. The Millersburg forma­ Limestone ...... 10 exposures the upper portion of the formation is of Friendsville coal...... 2 tion includes the sandstones and shales between Covered, sandstone fragments...... 2 a shaly character, although, in some instances, as Fire clay ...... 1 Limestone ...... 21 c, , , . , , , , ) Sandstone of ( OA the bottom of the Millersburg coal and the base near St. Joseph, the formation is sandy through­ Sandstone, massive or cross bedded //-,., \ 20 Section in quarry, l mile northwest of Zipp. Sandstone,cijx lightTTJ. gray and^ micaceous Ir .,,Gordon , Silurian and Carboniferous limestones to the GLACIAL AND IJSTTEKGLACIAL DEPOSITS. Unrecorded ...... 36 last-mentioned region is marked locally by the Coal (lignite)...... 1 northeast. Definitions. The glacial deposits consist of mate­ Gravel at top, remainder unrecorded...... 60 The soft sandstones and shales that underlie the occurrence of poikilitic crystals of calcite that is, Limestone (first consolidated rock) ...... by areas of rectilinear outline in which a calcite rials that have been picked up by the ice sheet till in this region and that probably furnished the cement has been deposited, inclosing instead of or dragged along its bottom during its southward In almost every instance the lignite, muck, larger part of the material of the finer portions of replacing sand grains and giving the rock a por- movement, or transported by its associated streams. and leaves are found just below the variable "blue the till are not commonly represented by pebbles phyritic aspect on fresh fractures. In the northern The material has all been moved from its original mud" of the drillers and beneath the ligniie there or bowlders, though a few fragments of somewhat half of the quadrangle the sandstone is found in location, and is therefore known under the name of is generally a water-bearing gravel. Most of the massive sandstone and of limestone have been many of the wells, shafts, and borings that reach drift. This drift was frequently deposited directly wells stop in this bed and therefore afford no infor­ noted. The pebbles known to have been derived the Friendsville coal, but its occurrence is not so by the ice, being either set free by the melting of mation as to the depth and character of the bed from the Great Lakes region or beyond are almost persistent as in the southern half of the area, and the portion into which it had been frozen, or simply rock, but in a few records, as in that of the Keens­ universally well rounded, but the flinty pebbles it is more frequently replaced by shale. left behind as a sheet beneath the ice, as the friction burg well, a considerable thickness of unconsoli- from the limestone areas, -though they have lost The Aldrich coal or the overlying limestone between it and the overridden surfaces became so dated material intervenes between the vegetable their sharp edges, still present a rather angular forms a rather persistent horizon, the outcrop of great as to cause lagging and lodgment. The drift matter and the solid rock. No samples of this appearance. The local bowlders, being of rela­ which in the region south of the drift border is liberated by either of these methods usually con­ underlying material have been seen, but from tively soft and friable materials, generally exhibit shown on the geologic map. It may be recognized sists of a heterogeneous mixture of all grades of descriptions it appears to be similar in character considerable rounding. The weathering of the also along the Wabash bluff at New Harmony and material, ranging from clay to large bowlders, and to the deposits near the surface. This suggests granite and diorite pebbles and bowlders varies southward, in the Mumford Hills, at the Illinois is known as till. Drift which was not deposited that the time of origin of the lower beds was not greatly, some being hardly stained even on the Central Railroad bridge south of Grayville, in the directly from the ice, but which was taken up and very much more remote than that of the upper exterior, while others are almost completely disin­ river bluffs at that town, in a bluff facing Bonpas transported by glacial streams and finally deposited beds, and would seem to indicate that the lower tegrated. Most of them show a weathered zone Creek 3 miles to the northeast, at McClearys Bluff, in more or less stratified masses, is known as strati­ beds belong simply to an earlier portion of the that reaches an eighth or a quarter of an inch in the bluff at Rochester, and probably at a num­ fied or modified drift. Illinoian stage. This is borne out by the apparent inward from the surface. It seems probable that ber of other points. The limestone appears to be Glacial stages. While subdivisions of the drift absence of the lignitic zone separating the surficial the variation in the extent of weathering is due absent in the region north of Grayville. are not usually apparent from superficial study, a deposits in the region south of the recognized limits largely to differences in composition or to the stage The portion above the Aldrich coal and lime­ detailed examination of its structure and its general of the ice invasion. to which incipient weathering had advanced at the stone is nowhere shown in its entirety, this portion distribution and associations shows that, instead Absence of pre-Illinoian drift. In the survey time of the removal of the fragments from their of the generalized section being made up from of there being a single sheet formed by one ice of the Ditney quadrangle, adjoining the Patoka parent ledges. exposures in the bluffs at Grayville and in the advance, there are in reality several distinct drift quadrangle on the east, considerable quantities of The texture of the finer portions of the till high hills northeast and north of that town. sheets, each of which represents a separate ice reddish stratified and sometimes partially cemented varies greatly, probably depending upon the nature advance. The intervals* of deglaciation or disap­ sand and gravels, with slightly stained chert and of the rock from which it was principally derived. Tertiary System. pearance of ice between the advances are made quartz pebbles, and an occasional crystalline frag­ Where shale appears to have furnished the larger The only beds intermediate in age between Car­ apparent by the presence of soils, by beds of peat ment, were found outside the limits of the till sheet portion of the material the till is generally very boniferous and Quaternary are the bright-colored and marl, and by the weathering of certain zones proper. These were mapped as outwash gravels, clayey, and is of a gray or bluish-gray color in its sands and gravels capping the two high knobs now buried in the midst of the drift deposits. The though it was suggested, because of their oxidized unoxidized portion. Where sandstones have fur­ about 2 miles north of the court-house at Prince- sheets themselves differ markedly in extent, and and somewhat weathered characters, that they nished much material the till is sandy, and varies ton. The section here is given in the next column. often in color, composition, and other physical might possibly belong to an invasion preceding the in color from a rather deep buff in the moderately The coarser material of the gravel bed consists properties, and these differences, together with the Illinoian. The more extended studies made in oxidized portions to a deep red in the upper and entirely of chert and quartz pebbles from 1 to 3 morainal ridges marking the various positions of connection with the survey of the Patoka quad­ more strongly weathered parts. The limestones in Patoka. the Patoka quadrangle appear to have been of too ridges are very generally deeply trenched by Lake deposits of the first halt. At its maximum character have been reported beneath the thick limited development to have had a marked influence ravines in which the semi-consolidated sand fre­ extension the ice margin probably lay several miles marl-loess deposits of the Patoka quadrangle at a upon either the color or the composition of the till. quently stands as vertical walls. east of the limit of the quadrangle at the latitude number of places. The following well section The till within the quadrangle is usually oxidized Deposits of this class occur in greatest develop­ of the Patoka River. At this time deposits that (SW. i sec. 10, T. 5 S., R. 13 W.) is typical of the to a depth of 7 to 10 feet, or even more, the unoxi- ment between Patoka and Hazleton and near formed broad plains were laid down in a glacial occurrence: dized portions being rarely seen, except in unusually Princeton, where they reach an elevation of 170 lake, which has been called Lake Patoka, occupy­ Section 4 miles west of Wadesmlle. deep cuts. In the oxidized portions the color is feet above the adjacent plains. In many places ing the upper valley of the Patoka River, but it Feet. Marly soil ...... ) T 3 ordinarily deep buff to brown, but reddish tints they lie from 100 to 130 feet above the lowlands. was not until the ice margin had fallen back to a , , , , , > lowan Clay (marl-loess)) 30 are very common in the sandier varieties. The red They are evidently the same as the kame moraine point about 2 miles east of Patoka that the lake Rich soil, logs, etc., (Sangamon) ...... 3 Blue mud and gravel (till) ) Tll . . (...... 10 type of till frequently gives evidence of incipient mentioned in the Ditney folio as occurring 2 miles was extended downstream into the Patoka quad­ r\ -i ^ f j. X-.G j j .'V Illinoian < ., Quicksand (stratified drift) ) ( ...... 1+ cementation by iron oxide, but the solidification is southwest of Wheeling, and are probably the gen­ rangle. The deposits at the lower end of the usually less marked than in the stratified sandy eral equivalent of the patches of outwash gravel of extended lake were laid down during the first Weathered zone. Though important deposits of layer formed as an original deposit by the glacial that quadrangle. recorded halt in the ice retreat, and consist mainly the Sangamon stage are lacking, the interval streams or from the reworking, by water, of the red Outwash gravel plains. While the ice front of silts and fine sands. The accumulations do not between ice advances is nevertheless well repre­ till. rested along the moraine between Princeton and rise much above the 420-foot level, indicating that sented by the Sangamon weathered zone. This Sections giving accurate measurements of the Fort Branch more or less water was continually the deposition failed to reach what must have been zone marks the top of the Illinoian drift, and is thickness of the till are uncommon, and are gener­ set free by the melting of the ice, and on flowing the water level if the overflow was over the 460-foot recognized by the leached and weathered character ally so located as to give only minimum thick­ away carried with it a considerable portion of the divide near Francisco, as it appears to have been. of that portion of the deposits. Where the over­ nesses. Wells have afforded data of great value as detritus previously held by the ice. In this manner Lake deposits of the second halt. After the dep­ lying loess and especially the marl-loess is of con­ to depth to the rock, but usually little information the broad, sloping drift plains bordering this osition of the above silts the ice fell back a few siderable thickness its lower part is usually but can be obtained as to the exact nature of the moraine on the east were built up, as were probably miles and halted along a second line, now marked little oxidized and its appearance is in somewhat material penetrated. In general the thickness of the similar plains at Haubstadt and vicinity. by the ridge of morainal and similar deposits marked contrast with that of the weathered zone the till, though showing great variation, may be There appear to have been two stages in the extending with a few breaks from near Hazleton upon which it rests. said to be slight, and usually ranges from 2 to 15 development of the plains bordering the moraine. southwest to a point beyond Cynthiana. In front lOWAST DEPOSITS. feet, though occasional exposures show much In the earlier stage the ice front probably lay about of the new ice margin four small glacial lakes accu­ greater amounts. A typical exposure is shown in li miles east of and parallel to the present line of mulated. The northernmost of these was a lakelet Following the formation of the weathered-zone fig. 8. The broad plateau-like plains that stand at the Evansville and Terre Haute Railroad, its posi­ lying just south of Hazleton, now marked by allu­ soils, and possibly silts, of the Sangamon stage, a considerable elevations above the valleys and that tion being marked by isolated drift knobs of buried vial flats composed of materials then deposited. considerable thickness of fine silt known as loess are so conspicuous in the Ditney quadrangle, to the moraine that project above the outwash plain. In A second and much larger lakelet accumulated was deposited as a mantle over nearly the entire east, are not represented in the area under discus­ the second stage the ice rested along the main between the ice along the morainal ridge that surface of Iowa, Illinois, and Indiana, and in por­ sion. In the moraines and other thick drift depos­ ridge between Fort Branch and Princeton, the area extended from near Mounts to the highlands tions of many other States to the east, south, and its, stratified sands and gravels predominate almost, between the two ridges being then filled up by the southwest of Princeton and the moraine that was west. This loess has been traced as far back as the if not entirely, to the exclusion of the till. later outwash materials and the two plains prac­ formed during the first halt of the ice and extended edge of the drift sheet of the lowan ice invasion in Drift plains. At many points within the quad­ tically united into one. from the vicinity of Princeton southward to beyond northern Illinois, but stops at or near its border, rangle, especially at the lower levels, there are more The Henry Whitman well, 3 miles east of Fort Fort Branch, probably damming the valley south apparently indicating that the deposition took place or less extensive drift flats that usually stand a few Branch (NE. i sec. 16, T. 3 S., R. 10 W.), gives a of the latter village. In this lakelet was deposited during the stage of glacial occupancy. feet above the older and highest stream silts. typical section of the deposits: a considerable thickness of silts, sands, and fine Previous to the present survey of the region no Because of their low relief exposures are rare and gravels, with an occasional bowlder or erratic Section 3 miles east of Fort Branch. attempt had been made to differentiate the silts, but usually indecisive, but the flats generally occur in Feet. geode. They reach an altitude of about 450 feet, evidence is now at hand for separating them into positions unfavorable for lake deposition and Soil...... 2 the probable level of the ponded waters. The two types: (1) thick, yellowish, calcareous, and fre­ Loess (possibly some sand in lower portion)...... 18 appear to merge into the sloping till plains of the Sand, fine and of varying color ("quicksand"), prob­ outlet was over the morainal barrier south of Fort quently stratified silts along the immediate borders upland hillsides. They are, therefore, thought to ably stratified../...... 65 Branch which was thereby greatly reduced and of the Wabash Valley, which are designated marl- Gravel...... 5 belong to the unstratified rather than to the strati­ Coal (lignite) through the valley east of Elberfeld. loess, and (2) the more clayey, oxidized, and struc­ fied type of drift. They are best developed near White sand.. The two remaining lakelets of this stage occu­ tureless silts designated as common loess, forming Poseyville and in the region northwest of the Sandstone ... pied the valleys of Flat and Barr creeks. Before the general mantle over the surface more remote Wabash River. Exposures in this region are very rare and show the ice invasion these streams had flowed north­ from the river. The first is believed to be of Drift ridges (probably morainal}. These deposits very little of the character of the material. Sev­ west along the valley of the Black River to the aqueous and the second of eolian derivation. The consist of ridge-like accumulations of drift that eral cuts, however, were noted in which reddish Wabash, but at the second halt of the ice on its evidence on which this conclusion is based is given broaden into wider hilly belts in some places, as in and buff sands were exposed, and in some a few retreat the old valleys were permanently clogged in full in Bulletin of the Geological Society of the region north of the Patoka River. The minor pebbles were found. From a well in the NW. i sec. by the morainal ridge extending from Mounts America, volume 14, pages 153-176. details of their topography exhibit in general 9, T. 3 S., R. 10 W., a sort of stiff, stratified sandy southward past Cynthiana toward Poseyville. In Marl-loess. The marl-loess is a white, gray, or almost none of the normal morainic features, the clay, probably mainly quartz-flour, characterized by front of the combined barrier of ice and drift the more commonly a yellowish silt occurring in rather uneroded portions usually presenting smooth, marked contortions and numberless miniature two lakelets mentioned accumulated. In them definite belts bordering the Wabash Valley on both gently undulating surfaces, free from kettles and faults, was thrown out. Some of the coarsef sands were laid . down .deposits similar to those of the sides. It occurs at all altitudes from the flood conspicuous knobs, though a few rounded knobs are semi-consolidated and are to be correlated with lakelets previously described. In the upper por­ plain to the 500-foot level (120 feet above the and remnants of shallow depressions, now drained parts of thQ lower "outwash" deposits described in tions of the valleys and beyond the ice limits, these river), at which altitude it frequently forms broad by the cutting back of the streams, appear to exist. the Ditney folio. overlie the silts of the earlier lake stages. The terraces and flats (figs 10 and 11), burying a rugged The ridges, however, exhibit an alignment parallel waters escaped along the ice margin and over a col rock or till topography. The thickness of the with the ice margin, and in some places, as, for ILLINOIAN GLACIAL LAKE DEPOSITS. probably located about 2i miles north of Blairsville, marl-loess in these terraces and flats is sometimes 40 example, in the ridge from Princeton to Fort The general drainage of the northern two-thirds so reducing the latter that the drainage persisted in feet or more, but thicknesses of ,10 to 20 feet are Branch, are associated with outwash plains. The of the quadrangle was originally to the west or the channel then established after the retreat of the more common. True marl-loess appears never to ridge east of Owensville is almost esker-like in out­ northwest. When the ice advanced and lay across ice. occur above the 500-foot level in this region. line, a resemblance which is heightened by the the lower portion of the valleys lakes were created Lake deposits of the third halt. This halt was The marl-loess is characterized by a high calcar­ sandy and stratified character of the deposits and in their upper portions in which large quantities shorter than the earlier ones. The lake in which eous content and frequently by a sandy texture. the steepness of the slopes. The width, however, of silts and smaller amounts of coarser sediments these deposits were laid down occupied the upper Calcareous concretions are exceedingly abundant. is probably too great to permit such assumption as derived from the melting of the ice were laid down, portion of the valley of the Black River and the In many instances it is delicately stratified (fig. 9), to origin. Its parallelism with the ice margin is generally accumulating nearly to the level of the lowlands south of Poseyville, now drained in part by and in some cases is interbedded with sands or fine also against this supposition. standing water. Four stages of lake deposits are Caney Creek. The ice margin probably lay across gravels, or even carries scattering pebbles itself. Practically no till has been identified with cer­ recognized in this region: (1) the deposits laid the Black River just north of Poseyville. The Fossils were found in a large number of expos­ tainty in any of the ridges. Wherever the expo­ down at the maximum extension of the ice; (2) the deposits are represented by the thick beds of silts, ures, but with the exception of those from one sures are good the material is found to consist of deposits of the first halt in the ice retreat; (3) the sands, and fine gravels constituting the broad flats locality, were all land forms. About thirty land deposits of 'oxidized sands and gravels containing deposits of the second halt; and (4) the deposits of in the vicinity of Poseyville. species and six aquatic species were identified by rounded pebbles of quartz and fragments of flint the third halt. The materials are usually silts W. H. Dall. The silts are conspicuous only along and jasper, supposedly derived from the older lime­ or very fine sands, but fine gravels are frequently SANGAMON DEPOSITS AND WEATHERED ZONE. the immediate border of the Wabash Valley, and stones to the east and north. Crystalline rock encountered in wells, while geodes and other bowl­ Erosion and local deposition. Studies of the are rarely found at a distance of more than 10 fragments, of Canadian origin, though rare, are ders are reported at several points in the glacial erosion features of the Sangamon stage in other miles from the river. occasionally found. The materal is clearly strati­ lake deposits of the second halt. regions have shown that the streams were broad The perfection of their stratification, their inter- fied and is prevailingly sandy, the pebbles forming Lake deposits of the maximum advance. Previ­ and sluggish, with only shallow and rather poorly bedding with sand and gravel, the presence of a relatively small proportion of the mass. The ous to the ice advance the drainage in the valley defined channels, and that the deposition was very pebbles in them, their terraced form, and their lim­ color of the upper beds is usually a deep red, but now occupied by the West Fork Pigeon Creek was slight in amount. In southern Indiana, however, itations to the borders of the Wabash point to lower down in the sections the red colors give place to the west and northwest, passing into the Wabash the erosion was locally of considerable importance, water as the most probable agent in the accumu­ to browns and buffs. Valley between Owensville and Princeton. During probably removing 80 to 100 feet of Illinoian till lation of the marl-loess deposits, the deposition Notwithstanding the absence of till and the lack the most southerly extension of the ice this outlet from the valley of the White River and possibly probably being in a fluvio-lacustrine body occupy­ of a distinctly morainal topography, the ridges, was obstructed and waters were ponded until they even greater amounts of material along the Ohio ing the lower Wabash Valley, into which the silt because of their location at or near the ice limits overflowed southward into a valley east of Elber- River. Deposition during the Sangamon stage was brought from the lowan ice sheet by the and their alignment with the margin, are believed feld, about 3 miles east of the limit of the Patoka was probably limited to a few unimportant second­ Wabash River. to be essentially morainal in their nature. The quadrangle. In this body of water, which in the ary deposits, produced by the reworking of the Common loess. This is usually a fine, clayey, normal morainal topography, if it ever existed, was Ditney folio was designated Lake Pigeon, silts Illinoian drift by the agency of the streams. buff or brown, but sometimes gray, reddish, or long ago obliterated by the marl-loess or loess accumulated, but these deposits lie mainly east of At many localities in Iowa and Illinois, and to mottled silt, which mantles the hills as a relatively mantles, or destroyed by erosion, which, because of the limit of the Patoka quadrangle. Similar silts less extent in Indiana, peaty beds of black muck uniform sheet having but little relation to the char­ the relative softness of the material and the steep­ also accumulated in the valley at the headwaters which were deposited in this interglacial stage have acter of the topography. It is essentially non-cal­ ness of the slopes, has gone on rapidly until the of Flat Creek. been noted and described. Beds apparently of this careous in composition, differing markedly in this respect from the marl-loess, as the following overlying more or less irregular surfaces, points fact a perfected flood plain, the topography of plains, namely, unequal degradation due to locali­ analyses will attest. The first sample (No. 1) was toward a modified aqueous origin of this class of which is in marked contrast with that of the roll­ zation of the erosion of the flood plain on the one from near Princeton and was analyzed by Prof. silts in a few cases in the Ditney quadrangle, to ing to broken surface of the lower flood plain. hand, and unequal upbuilding of previously Robert Lyons for the Indiana geological survey the east, but no examples were recognized in the They are overflowed in part at periods of excep­ reduced areas on the other. The two processes, and published in its twentieth and twenty-first area now under discussion. The great mass of the tionally high water, but the higher portions along however, have so cooperated that the resulting annual reports. The second (No. 2) was from common loess appears to be undoubtedly of eolian the edges of the valley always remain above water. forms can seldom be differentiated. the land of B. C. Macy (said to be near New derivation, the source of the material being found There is no break between the lower and higher Sivamp deposits. Under swamp deposits are Harmony) and was given in D. D. Owens's report in the marl-loess of the Wabash Valley. portions, the plain exhibiting a gentle, even slope included those deposits of muck, peat, and vege­ on "A Geological Reconnaissance of the State of Older stream silts. In the class of older stream from the edge of the valley to the banks of the table mold which occupy the broad, shallow Indiana," 1838, part 2, p. 66. The two are silts are included the silts occupying most of the streams or to the bluffs facing the lower flood depressions in both the upper and lower flood selected because they mark extremes in the range smaller valleys. They consist largely of reworked plains. The upper flood plains are bordered by plains. They are characterized throughout by a of the content of carbonate of lime (CaCO 3 ). The loess and are therefore of a marked clayey tex­ broad and originally forested dune belts, apparently heavy growth of timber. The thickness of the average sample of the common loess would prob­ ture. A few sandy layers and more rarely gravelly composed of sands derived from the surface of the accumulation is usually 3 or 4 feet, but may reach ably show less than 1 per cent of the CaCO 3 , streaks occur. The deposits are characteristic of flats. 7 to 10 feet. The most notable of the swamps are while the average sample of the marl-loess would overloaded streams, the work of which is to build The muck and a part of the surface silts are those surrounding the Cypress Ponds, near the probably show more than 5 per cent. up rather than reduce their beds. While many of undoubtedly of recent origin, but as important junction of the White and Wabash rivers. Some the bottoms mapped as older silts are no doubt dunes are nowhere forming under the conditions of these ponds, it is said, contain water throughout Analyses of loess (No. 1) and marl-loess (No. 2). receiving additions even at the present time, the now existing in this region it is thought that they the year, and several retain it in all but the dryer

No. 1. No. 2. presence of the earlier Wisconsin dunes upon their represent an accumulation at a period of greater seasons. Most of the cypress has been cut out, Prince- New Har­ ton. mony. surface in the northwestern part of the quadrangle depositional activity, when broad, bare flats, possi­ but enough remains to give a decidedly southern shows that they had in places practically reached bly extending over the greater part of the present aspect to the swamps.

Si08 ...... 71.20 1 their present development in early Wisconsin time. width of the valley, were exposed to the sweep of Abandoned channel deposits. The abandoned AI n 18.56 [ 60.00 i The bulk of the filling is probably Illinoian, the winds, and when the rate of dune accumulation channels are of all stages, from freshly-cut bayous Fe3 O 3 ...... 1.34 though the surficial clays doubtless accumulated probably precluded the existence of a vegetable to channels nearly filled and effaced as topographic FeO ...... 15 .80 largely during the lowan stage. For the reason mantle. These conditions are believed to have features. The filling of the channels is at first CaO ...... 14 20.27 CO, ...... 15.93 that their principal period of development termi­ characterized the latter part of the Wisconsin stage,' very rapid because of their connection with, or nated in the lowan stage they are grouped with and possibly extended into Recent time. It is proximity to the rivers. Fillings of silt amount­ Tin .88 1 MgO...... 52 the deposits of that age rather than with the thought, however, that the covering of the flood ing to 6 inches in a season have been recorded. In Y 1.00 ya,3 O ...... 1.26 1 recent deposits, classification with which might plain and dunes with vegetation probably took addition to this, large quantitities of driftwood are K 8 O...... 32 appear to be warranted by their recent surface place immediately upon the subsidence of the frequently washed in, and trees on falling not H 8 0...... 6.30 2.00 silts. This classification was, in fact, made in the floods that are supposed to have attended the Wis­ uncommonly add their remains to the deposit. As Total ...... 100.67 100.00 Ditney folio, in which is described the area lying consin ice retreat, but it is considered safer to class the filling approaches completion the deposition immediately to the east. In the vicinity of the both the flood plain and dune deposits as transi­ is less rapid and consists mainly of a mixture of Mechanical analyses of the loess are given in main drainage lines the older stream silts are tional rather than with either the Wisconsin or silt and vegetable matter, differing but little from the discussion of the soils on page 10. invariably trenched, and are in some places super­ Recent stages. the swamp deposits except in the shape of the Calcareous concretions are relatively rare, and ficially removed or represented only by a few small Later dune sands. These sands, the origin of areas. when they occur are generally of small size. On terraces. which has just been considered, occur principally Natural levees. The natural levees consist of the other hand, small iron concretions, both of as a broad but interrupted belt along the east side overwash sands or fine gravels deposited when the WISCONSIN DEPOSITS. the tubular and the rounded or irregular type, are of the Wabash Valley, though a few small areas current of the overflowing river waters is first abundant in places. The common loess has not The ice sheet of the Wisconsin stage did not are found bordering the river flats on the Illinois checked. They are conspicuous in the quadrangle been found to carry fossils at any point in the reach the Patoka quadrangle, and there are there­ side of the river. The material is usually a coarse only along the Wabash and Fox rivers, and are region examined, nor does it contain pebbles fore no deposits of this stage covering the general quartz sand which in the better exposures shows confined to the banks or near vicinity of the except where the sheet is so attenuated that roots surface of the region. Every stream, however, stratification either of the steep advancing-face streams. In age they are the most recent of the penetrate the till beneath and on the falling of the which led either directly outward from the ice type or of the irregular type characteristic of accu­ deposits of the quadrangle, unless it be some of tree, drag the pebbles upward into the loess. The margin or was fed by tributaries heading at the mulation after vegetation has begun to take hold. the swamp and abandoned channel deposits. They common loess of the region presents no definite ice front carried considerable amounts of glacially Fig. 12, from a photograph taken just west of are found on both the lower and the upper flood evidences of stratification, though an indistinct derived materials, which were deposited as broad, Mount Carmel, shows the former type in the lower plain. banding in planes parallel with the surface, made flat plains of sand or fine gravel. Of the streams right hand portion of the view, while the latter STRUCTURE. visible because of differences in moisture absorp­ in the vicinity of the Patoka quadrangle, only the type is shown on the left. tion of the materials, has been here and there Wabash and White rivers head in the region occu­ The coarse sand is in some places interbedded Local dips, often of several degrees and of noted. pied by the ice, though the Ohio received the with fine or marly sand not much different in com­ various directions, may be seen in some of the Along the borders of the east side of the Wabash drainage of a number of other streams heading position from the marl-loess, though it never exposures of the Patoka quadrangle, and from a Valley loess of the common type is often absent, near the ice front and bringing down quantities of exhibits the perfect stratification of the latter. It superficial examination might appear to indicate marl-loess of typical composition, structure, and glacial sediments, which were deposited as broad carries fine fragments of shells, but no perfect not only that there is a considerable dip to the topography frequently forming the immediate face flats on either side of the river. The Wabash forms, such as universally characterize the marl- rocks of this area, but that there is also consider­ of the bluffs. Though differentiated only with River was also the outlet of a large glacial lake loess, were found. able irregularity in its direction and amount. A some difficulty from the marl-loess where the latter in the region of the Great Lakes. The sand has in places a maximum thickness of closer study, however, reveals the fact that these is weathered, a thin coating of the common type of Wisconsin terrace. Although it is certain that about 100 feet. It is characterized by a typical irregularities usually extend but a few feet or rods, loess usually appears to begin within a quarter the larger part of the sand and gravel filling of dune topography, though somewhat subdued in and that they have almost no effect on the broader or half a .mile of the edge of the marl-loess and the Wabash and White river valleys was trans­ some of the outlines through the reworking of the structural features. By the tracing of coals or increases gradually in thickness for several miles, ported indirectly through the agency of the Wis­ surficial portion by creep or through the influence other persistent beds it is clearly shown that, probably reaching a maximum of 15 feet or more consin ice sheet, and was probably brought nearly of the original forest growth. Large undrained , although the dips are extremely variable and even at a distance of 6 or 7 miles, beyond which it to its present place during Wisconsin times, there kettle-like depressions are common. easterly in places, the general dip is to the west, slowly decreases until, at a distance of 35 or 40 is only one unaltered deposit in the quadrangle Late loess. The sand of the dune belts in some the amount varying from 5 to 40 feet to the mile, miles, it has a thickness of only 2 or 3 feet, or which has been referred to this stage. This is the places becomes finer away from the valley and with an average of about 11 feet. This'dip, slight possibly even less. On the west side of the river deposit between Cowling .and Keensburg, in the merges into a sandy loess. This coating is usually as it is, is sufficient to make a difference of about the conditions of distribution are similar, though northwestern portion of the area. It consists of a so thin that the material has become commingled 300 feet between the altitude of a given bed at the the strip of marl-loess is narrower and the maxi­ thin layer of silts, fine sand, and gravel of fresh with the underlying lowan loess through the action eastern border and that which it has at the western mum thickness of the common type occurs much northern material spread over the upper stream of penetrating roots, and can not be differen­ border of the quadrangle. nearer the borders of the valley. The same thin­ silts. Toward the higher of the late Wisconsin or tiated. In the railroad cut at Mount Carmel and The Somerville formation, the Parker coal or ning of the deposit away from the river is noted, recent terraces on the east it presents a low bluff, in a few other localities, however, there appears to associated limestone, the Friendsville coal, and the the common loess being generally absent, at least perhaps 10 feet in height, but the bluff overlook­ be a surficial loess mantle, a foot or two in thick­ Aldrich coal and associated limestone are the best in recognizable amounts, at a distance of 15 miles ing the abandoned channel near Cowling is about ness, resting upon the loess of the ordinary type, defined beds in the quadrangle and where they out-' from the Wabash. 40 feet high. The surface generally consists of from which it is separated by a weathered zone. It crop or are reached by ordinary water wells dips The common loess is not confined to any one fine sand, which is frequently drifted into low is believed to be contemporaneous with the later may be determined with some accuracy. By com­ horizon, but occurs at all elevations, from the level dunes. The flatter and poorly drained portions dune sands. bining the observations based on each separate bed the structure can be worked out, especially in the of the river bottoms to the crests of the highest are characterized by black muck accumulations. RECENT (POST-GLACIAL) DEPOSITS. hills. Above a certain altitude, which detailed Wisconsin dunes. Besides the low sand dunes southern half of the quadrangle. The general dip observation has shown to be approximately 500 of the Wisconsin terrace, the larger of which are Lower flood-plain deposits. These deposits con­ is northwestward and is greatest along the eastern feet (120 feet above the river), it constitutes the represented on the map, there is a well-defined sist of silts, sands, and fine gravels, with occasional border and least along a line extending from the only silt noted. Below this level, especially near ridge of dunes extending from east of Keensburg areas of muck occupying the shallow depressions as vicinity of Little Rock to the southwest corner of the river, the common loess, though generally nearly to Bonpas Creek. The sand of the dunes, in the upper flood plains. The chief particulars the quadrangle. A low anticline runs from near occurring, is not, as has been seen, necessarily both of the flat and ridge, is notably finer and in which the lower differs from the upper plain Friendsville southeastward to the vicinity of Mount present, the marl-loess, which normally underlies whiter than that of the more recent dunes border­ are: (1) the low level of its surface, which is gen­ Carmel. Between this anticline and Gards Point, it, forming the bulk of the silts. Eastward from ing the Wisconsin terrace on the south. erally subject to annual overflow and is frequently Bellmont, and Keensburg the dip is low, but the river there is a persistent though gradual separated from the upper flood plain in the case of steepens again in the vicinity of Bonpas Creek. decrease in the thickness of the marl-loess, the WISCONSIN-RECENT TRANSITIONAL DEPOSITS. rivers (or from the older stream silts of the smaller From the southeast corner of the quadrangle to common type becoming at the same time of greater Upper flood-plain deposits. These deposits con­ streams) by an escarpment 5 to 15 feet in height, the vicinity of Kasson the dip is about 15 feet relative, if not real, importance. sist of broad flat plains of sands or fine gravel, with and (2) its undulating, rolling, or broken surface, to the mile, but farther north it is somewhat The apparent presence of pebbles in some locali­ occasional areas of muck in broad, shallow depres­ characterized by numerous bayous and abandoned steeper, reaching about 30 feet to the mile between ties in the common loess, and the occurrence of sions in their surface that occur along the Wabash channels. Two distinctly different processes are Inglefield and Little Pigeon Creek. Northeast flats and silted divides of loess of the same type and other prominent streams. They constitute in involved in the production of the lower flood of St. Joseph the dips are as high as 4° NW. Patoka. 6 for some distance along the railroad, making a Or of shells, corals, etc., which on subsequent solid­ had the Carboniferous beds appeared above the cutting, and there is some evidence, in the shape of very material difference in the elevation of the out­ ification became sandstones, shales, and limestones. surface of the sea by the further uplifting of the divides and flat crests at an altitude not far from crops of the Parker coal and associated limestone At times the region was occupied by wide swamps Cincinnati anticline than erosion set in and began 500 feet, that a local peneplain was developed at on opposite sides of the same hill. The dips are or shallow lagoons, in which accumulated quantities its work of reducing the surface thus formed. It that elevation, and it is possible that there are still steeper here than elsewhere in this region so far as of peaty matter, now changed to coal. Together is probable that erosion did not at first keep pace other levels at which local plains developed. If so, observed. From the ridge between St. Joseph and these beds make up a series of coal-bearing rocks with uplift, and an elevation of some prominence these later peneplains, like the first, suffered uplift Kasson westward to the vicinity of Parkers Settle­ of which those of the Patoka quadrangle are a may have resulted. On the cessation of the and erosion, until broad valleys were carved out ment the dips are about 15 feet to the mile. From part. They are the highest and youngest of the upward movement, however, erosion continued with to the level represented by the rock floors underly­ Lippe to Springfield the dips average only about 6 solidified rocks of Indiana. undiminished energy its work of reducing the land ing the deep silts and glacial fillings of the present feet, while westward from Springfield to the Wabash The thickness of the entire series, from the Cam­ and carrying the materials to the sea, which now valleys. River they are as low as 3 feet to the mile. brian to the close of the Carboniferous, is probably lay at some distance from the Indiana region. The Late Tertiary or early Pleistocene depositional North of the drift area the outcrops are less fre­ 4000 or 5000 feet, of which, in the Indiana region, surface of the land was thus gradually lowered and stage. Following the period of Tertiary erosion, quent and poorer and the dips are more difficult to considerable more than half is limestone, the con­ its prominences were reduced to broad, low, well- during which the land was carved by the streams determine. The Aldrich coal, however, can be ditions being in marked contrast to those existing rounded hills separated by wide, flat, and shallow until it had essentially the form it would now show traced from near Stewa.rtsville to the Wabash River near the borders of the sea to the east, where the valleys. Such a featureless surface is called a pene­ if the overlying silts and glacial deposits were near Grayville, and shows in this interval an aver­ deposits were composed largely of sandy and shaly plain, and there is but little doubt that a number removed, there appears to have been a subsidence age dip of about 6 feet to the mile. At Princeton materials. of successive general or local peneplains were or an overloading of the streams, which caused the the deep wells and the coal shafts show that the The deposition of the sedimentary rocks did not developed one after the other in the region under deposition of bronze-colored gravels at Enterprise, dip is as high as 50 feet, but along the Patoka it take place uniformly over the whole of the basin. discussion, as appears to have been the case with on the Ohio, southeast of the Patoka quadrangle. is only about 20 feet to the mile. From Patoka Even at the beginning of the Cambrian period the series beginning in pre-Triassic time and Whether these gravels, which certainly look much to the Gordon Hills the dip is about 12 feet to the islands existed, it is believed, in the southern por­ ending with the Tertiary plain along the Atlantic older than the oldest glacial deposits, are to be mile. From the latter hills to Crawfish Creek the tion of Missouri, and possibly elsewhere in the coast. The remnants of the latest of the pro­ regarded as the result of a reworking, in late dip is nearly flat, but from the creek westward it great continental sea, and local uplifts, possibly in nounced plains in the region of the Patoka quad­ Tertiary or early Pleistocene time, of older Tertiary rises rapidly to a height of 450 feet in about 2 some cases accompanied by slight folding, brought rangle are preserved even to the present time in sediments, as Mr. Leverett has suggested, or as miles (see geologic map and fig. 4). From the crest similar islands into existence from time to time at the flat-topped crests and isolated hills rising, as undisturbed late Tertiary deposits, as Mr. A. C. of this low anticline the beds dip gently westward other points as deposition progressed. Of these described in the discussion of topography, to ele­ Veatch has urged, is a question that has not been at a rate of from 18 feet to the mile between the one most intimately related to the region of the vations of from 600 to 650 feet. fully answered. It is certain, however, that they Friendsville and Gards Point to about half this Patoka folio was the Cincinnati island, produced No remnants of a topography older than the were deposited much later than the gravels on the rate west of Mount Carmel. In the region about by the broad, dome-like fold known as the Cincin­ peneplain under discussion are known in the peneplain remnants, and before ice-transported Maud and Bellmont the beds, though showing sev­ nati anticline, the maximum development of which Patoka region. The age of the peneplain can not crystalline or other Canadian materials were eral minor undulations, are, on the whole, nearly is in the vicinity of Lexington, Ky. From here be regarded as positively established, though it brought within the reach of the old Ohio drain­ flat. To the south and southwest the dips are this fold extends southwestward to Nashville, appears to form a part of a surface which stretched age system. more pronounced, averaging 20 feet to the mile Tenn., and northward and northwestward through eastward to the base of the Allegheny Mountains GLACIAL HISTORY. between Sugar Creek and Rochester and 15 feet to Cincinnati and into the north-central portion of and southward along their western margin to Ala­ the mile from Bellmont to Cowling. Between Indiana. This broad dome (the uplift of which bama a surface which is probably equivalent to Ulinoian deposits and stream changes. It has Rochester and McClearys Bluff the rocks are nearly began long before the beginning of the deposition the Lexington Plain of Kentucky, and is thought usually been believed that neither the pre-Kansan horizontal. of the beds of the Patoka quadrangle) and the to have been formed in early Tertiary time. nor the Kansan ice sheet reached as far south as GEOLOGIC HISTORY. original island in southern Missouri, which had in Drainage of the peneplain. On two of the this quadrangle. Although some features in the the course of time become considerably enlarged, knobs just north of Princeton and at a number of Ditney quadrangle, immediately east, suggested the PALEOZOIC EVENTS. formed the opposite shores of a broad embayment points in the hills bordering the Wabash, White, possibility of an early invasion, later studies fail to Deposition. The deposition of the great series or strait that extended from western Kentucky and the lower Ohio valleys, deeply stained, bronze- substantiate this view. In the Ulinoian stage, of sediments laid down in the interior sea occupy­ across southwestern Indiana, Illinois, northern colored gravels, composed mainly of quartz and however, the ice reached well into the quadrangle ing the broad Mississippi Basin began in Cambrian Missouri, and southern Iowa, and connected with flint and supposed to be of Tertiary age, are found and remained there for a long time, during which time with a thick bed of sand which was spread the northwestern extension of the interior sea in resting upon the peneplain remnants. Near the till sheet, the extensive morainal deposits, the along the changing shores in waters that were gen­ western Missouri and Iowa. It was in this embay­ Princeton the gravels have an elevation of 610 feet marked outwash plains, and the glacial lake depos­ erally shallow, ripple marks and other shallow- ment that the Carboniferous rocks of the Patoka at their base (determined by level), and at the other its were accumulated. water or shore features being common in the region were laid down. localities of from 550 to 700 feet (barometric deter- In consequence of the obstruction of the estab-

Qd ^ . ..,

Horizontal scale, TysWisi or 1 inch=3 miles (approximately); vertical scale, 1 inch=1000 feet. . 4. Structure section across the northern portion of the Patoka quadrangle along the line A A on the Areal Geology map. Shows the position and extent of the Friendsville coal. Cm, Millersburg formation; Cs, Somerville formation; Cd, Ditney formation; Ci, Inglefleld formation; Cw, Wabash formation; Tr, Tertiary; Qd, glacial drift.

resulting sandstone. At the close of the Cambrian Uplift and tilting. The sedimentary beds were minations). A list of localities furnished by Mr. lished drainage lines by the Ulinoian ice, or by the period, there was, in Indiana, a change from con­ originally in an essentially horizontal position Frank Leverett includes the following: (1) South till or various other deposits laid down during its ditions favorable to the deposition of sandstone to throughout the extent of the embayment in which bluff of the East White River 2 miles southwest of occupancy of the region, many important changes those favoring the accumulation of limestone, and they were deposited. At the close of the Carbon­ Shoals, Ind.; (2) bluffs of the Ohio River back of in the arrangement of the streams were produced a 50-foot bed of the latter was deposited at the iferous period there were further uplifts of both Tell City and Cannelton, Ind.; (3) near Stephens- (see fig. 5). beginning of the Ordovician period. Although the Cincinnati and Missouri domes or anticlines. port, Breckinridge County, Ky.; (4) near Branden­ The Patoka River, now a prominent stream there was a partial return to the former conditions The intermediate area, consituting what is now burg, Meade County, Ky.; and (5) near Rosebud, reaching back eastward 80 miles or more from the during the deposition of the succeeding formation, known as the Illinois-Indiana coal basin, partook Pope County, 111. Wabash, was not in. existence as a single stream the St. Peter sandstone (portions of which are cal­ of the uplift, and its deposits were lifted above the It will be noted that these deposits are in, the previous to this ice invasion, though parts of the careous), the deposition of limestone continued, level of the sea, but the amount of the elevation vicinity of the present drainage lines, though from valley through which it now flows were occupied with a few relatively unimportant breaks, through­ was much less than in the bordering region, the 100 to 200 feet or more above the stream levels, by pre-Glacial streams that eventually flowed out the whole of the Ordovician, Silurian, and result being the development in the rocks of a slight while on crests of equal heights in the intermediate northwestward into the White or the East White part of the Devonian periods. Beginning with but persistent dip toward the center of the basin areas gravel deposits are lacking. This is taken River. The original lower Patoka River entered Middle Devonian times, however, limestone gave in eastern Illinois. The coal-bearing rocks form­ to indicate that the gravels were probably depos­ the quadrangle at the same point as the present place to black shale, which in the early part of the ing the surface were doubtless originally connected ited in the broad, shallow valleys of the Tertiary stream, but instead of flowing westward past the Carboniferous period was followed by sandstone, with similar rocks to the south and also to the peneplain, and that the main drainage lines of that site of Patoka turned northwestward and passed and later by limestone, the deposition of which northwest, but subsequent erosion destroyed these period coincided in a general way with those of out into the Wabash Valley at a point about mid­ continued until the close of the early Carboniferous connections and left the coal rocks in the present the present time. way between Patoka and Hazleton. During the (Mississippian). The series of deposits closed with isolated basin. The limits of this coal basin, Late Tertiary erosion. After the reduction of ice invasion this old valley was choked and an interval during which the recently deposited together with the position of the Patoka quad­ this portion of the Mississippi Basin to the pene­ obstructed and a glacial lake formed along the val­ beds were lifted bodily, and without tilting, above rangle, are shown in fig. 1, p. 2. plain described, an elevation took place that lifted ley, the outlet of which was probably near Fran­ the level of the sea, and were extensively eroded the region to an altitude considerably above that cisco, a few miles east of Maxams. Before the ice by the action of streams. MESOZOIC AND EAELY CENOZOIC EVENTS. which it possesses at the ' present time. With the receded from the region the old valley was choked After the early Carboniferous interval of erosion Subsequent to the uplift that followed the depo­ beginning of this elevation the streams, which dur­ and practically obliterated by accumulations of the beds once more sank beneath the waters of the sition of the Carboniferous rocks, and that raised ing the later stages of development of the pene­ thick morainal deposits that were laid down across great interior sea, and deposition continued as them above the level of the waters in which they plain surface had been very sluggish, entered upon its lower portion, with the result that the river was before. The conditions, however, were no longer had been deposited, there appears to have been no a period of active erosion that resulted in the carv­ forced to seek a new outlet, which it found at constant through long periods of time, but .were further incursions of the sea into this region and ing out of broad valleys to a depth of 100 to 150 Patoka. continually changing, the waters of the sea being there is, therefore, no recorded history in the form feet, or more, below the level of the surfaces of their It is believed that the Wabash River at this now shallow, now deeper, and at times, as follow­ of rocks. It is only in the land forms, or the present fillings and the reduction of the general time flowed in the broader valley lying east of the ing the deposition of the Mansfield sandstone and topography resulting from erosion, and in a few surface to a lower level. Here and there, where Claypole and Gordon hills, and that it swerved just before the deposition of the Inglefield forma­ patches of old river gravels that evidence of the the surface was more remote from the active streams southwestward near Lyles, passing north of Foots tion, completely withdrawing and permitting the succeeding events is found. As each new set of or where the rocks were of a more resistant charac­ Pond Hills, west of Mumford Hills, and probably erosion by surface streams of the beds previously the topographic features was developed at the ter, remnants of the peneplain were left in the several miles west of its present position at New deposited. Each change was recorded by differ­ expense of older ones, only later forms are left to form of the crests and outlying hills previously Harmony. ences in the character or structural features of the tell of events that have taken place. mentioned. It is not probable that erosion was Previous to the ice invasion Pigeon Creek flowed rocks, beds of sand alternating with beds of mud, Formation of Tertiary peneplain. No sooner uniformly active throughout the period of down- in a direction opposite to its present course. It 7 entered the quadrangle from the east, where it Much of the material derived from erosion was Wabash Valley were probably formed in late Wis­ stone. A band of sulphur occurs in the middle of now leaves it, and flowed northwestward past the doubtless deposited in the valleys, where it is now consin time or in the early part of the post-Glacial the coal. site of Fort Branch and into the Wabash Valley covered by more recent deposits. A considerable epoch and are in a measure transitional. The older In the Oswald mine the coal is reached at about at a point a little east of Indian Camp Creek. The part of the lower portions of the older stream silts and higher Wisconsin deposits doubtless represent 450 feet, or 30 feet above sea level, and averages 6 obstruction of this creek brought into existence a was doubtless accumulated at this stage. Other an upbuilding during a period when the waters feet 6 inches in thickness. It is a good, firm coal, lake which overflowed a divide east of Elberfeld, deposits of this age now remaining are the muck were heavily loaded with sediment as compared without regular sulphur or clay bands, but thin several miles east of this quadrangle, having an and lignitic deposits which were described (p. 4) as with their condition during the formation of the bands of sulphur are abundant in places. The elevation of about 410 feet. By the outflow from occurring under the marl-loess at various points. later flood-plain deposits. As the upbuilding of roof is a shale, which is spmetimes overlain by this lake the divide was reduced to a little less than That the stage was of considerable length is the fluviatile beds of the valleys continued many limestone. The following analyses are taken from 400 feet and so afforded an easy eastward outlet attested by the extent of the erosion, by the semi- of the low divides of the earlier topography were the Twenty-third Annual Report of the Indiana for the water that was ponded by the ice and the rounded character of the resulting topography, and buried beneath the resulting accumulations, leaving Geological Survey, pp. 1243-1244. The Sunnyside morainal deposits that accumulated across the old by the leaching and weathering of the drift as rep­ a number of the higher points as "islands" pro- mine is just south of the limits of the quadrangle. valley near Fort Branch. resented in many exposures. Analyses of Petersburg coal at Princeton and Evansmlle. As the ice retreated from the Fort Branch lowan deposition. The next event of importance [Analyst, W. A. Noyes.] moraine two more glacial lakes came into existence. was the deposition of the mantle of silt, previously The first was situated between Owensville and Fort regarded as a unit and designated as loess. Reasons Volatile Total Fixed combus­ combus­ Moist­ Sul­ Total have been given (p. 4) for subdividing this silt into Source of material. carbon. tible tible Ash. ure. phur. waste. Branch. Its waters cut an outlet across the moraine matter. matter. at the latter point and passed off to the east and two groups, the marl-loess and the common loess. south through the Elberfeld pass. The upbuilding A study of the characters and relations of the two 59.70 28.90 83.60 7.80 8.00 16.40 of the morainal barrier east of Owensville served types leads to the belief that during the presence of 51.18 22 71 83.90 11.02 5.09 1.38* 16.11 to make the southward drainage a permanent fea­ the lowan ice margin in northern Indiana, a fluvio- 48.14 38.59 86.73 6.83 fi 44 1.85 14 12 lacustrine body existed along the lower portions ture. The second lake was situated in the valley *Sulphur separately determined. of Flat Creek and was due to the obstruction at least of the Wabash and White river valleys. caused by the ice near Cynthiana. This creek This water body is thought to have been due to a jecting above the river flats. In the course of the The general dip of this coal in the southern originally emptied into the Wabash River at a general depression (amounting perhaps to 80 or meanderings and swings of the rivers these have portion of the quadrangle is northwestward at an point 3 or 4 miles north of Stewartsville, but on 100 feet) of this region as compared with the land been attacked first from one side and then from average of about 5 feet to the mile. From an ele­ its obstruction by the ice and the formation of the farther south, over which the waters had eventually another until nearly all of them now present steep vation of 135 feet above sea level, near Evansville, lake the waters ponded up the valley of an old to pass. Into this lake the two large rivers brought faces or even bluffs to the flats. Among these it descends northward to 50 feet at Fort Branch and tributary and passed over a divide at its head into large quantities of fine silt, which was deposited in "islands" Claypole, Gordon, and Mumford hills 30 feet at Princeton, westward to about sea level Big Creek. This divide was probably about 2? their valleys in the form of what is here known as are the most prominent, though a few smaller ones in the extreme southwest corner of the quadrangle, miles northeast of Blairville. Before the retreat of marl-loess. While this material was accumulating were noted. The depth of the rock valleys sepa­ and northwestward to probably a little below sea the ice the moraine at Cynthiana had been formed and during the period immediately following the rating these hills from the general uplands is not level at New Harmony. and the old valley so blocked that even after the withdrawal of the water, before vegetation had known, but in some places the rock floors are only Millersburg coal. This coal, which in the Dit­ retreat of the ice the drainage persisted in its new- covered the surface, broad flats were doubtless a few feet below the flood plains (see fig. 13), or at ney quadrangle, on the east, lies 70 to 90 feet found channel. many times exposed to the sweep of winds, and by about the limit of erosion of the present streams. above the Petersburg and is several feet thick, is Barr Creek, like Flat Creek, which originally the action of these winds it is presumed the great This would indicate that the broadening of the not mined in the Patoka quadrangle, but three- found outlet into the Wabash along the line of sheet of common loess was accumulated. These divides and the isolation of the "islands" was fourths of a mile northwest of Stringtown a coal Black River, was deflected southward into Big winds were apparently prevailingly from the west, brought about after the stream had reached practi­ supposed to be the Millersburg is reached by a well Creek. for the deposit is both thicker and more extensive cally its present level. The steepness of the bluffs at 150 feet below the bottom of the valley, or about A still further retreat of the ice brought into on the east side of the Wabash Valley than on the indicates that the completion of the broadening 235 feet above sea level. In Evansville two wells existence a lake in the vicinity of Poseyville, in west side. took place in very recent time. situated near Pigeon Creek penetrated the Millers­ During the final retreat of the ice the Wabash burg bed, here about 18 inches thick, at depths of which deposits were built up to such a level that It was probably in late lowan times that the last G the original northern drainage lines were obliter­ important additions to the older stream silts were River was the outlet for Lake Maumee, a large gla­ 152 and 180 feet below the surface, or at 98 and ated and a new drainage into Big Creek was inau­ made. cial lake extending over the areas now covered in 100 feet, respectively, above the Petersburg. At gurated. Peorian interglacial stage. The Peorian stage is whole or in part by Lakes Michigan, Huron, and Fort Branch this coal is 3 feet 6 inches thick and Erie, together with considerable areas about their is reached 254 feet from the surface; at Princeton borders. This lake formed between the retreating the deep borings penetrated it at depths varying ice and the northward-sloping land in the region from 201 to 260 feet, the interval above the Peters­ mentioned and emptied into the Wabash a little burg bed varying from 120 to 145 feet. west of Fort Wayne, Ind. Parker coal. This is an unimportant coal, vary­ ing in thickness from 6 inches in its purer form to KECENT EVENTS. 18 inches when shaly, which occurs about 90 or Subsequent to the deposition of the Wisconsin 100 feet above the Somerville limestone. It has and transitional sediments, just noted, the region been stripped in a few places for use in threshing appears to have stood approximately at the same machine boilers, but is generally too thin and level as at present. The streams, with diminished impure to be of value. The thickness reported volume and less sediment, cut into the deposits of in wells is somewhat greater than that observed in the Wisconsin and transitional stages and excavated outcrops, which are nowhere such as would warrant the lower flood plains, which were in places several development. The outcrop of this coal outside of miles in breadth and several feet below the upper the drift area and also within the drift area as far plains. This work is still going on, new channels as it can be definitely traced is shown on the constantly being formed by local concentration of geologic map. The thin coal about 70 feet above the overflowing waters in times of flood. At the the river at Patoka, the coal at or near the same same time, however, old channels are being closed level in the bluffs 2 miles northwest of town, the up and the old level is being restored in places, the thin coal near the flood-plain level on the south­ tendency on the whole being rather toward a simple west side of Gordon Hills, and the coal in the hills shifting than toward either a general broadening or northeast of Owensville are believed to be the narrowing of the lower flood plains. equivalents of the same bed. Friendsville coal. This coal, which is of some FIG. ti. Pre-Quaternary and present drainage in the Patoka and Ditney quadrangles and vicinity. (Portions outside MINERAL RESOURCES. importance west of the Wabash, occurs about mid­ quadrangles after Leverett.) COAL. way between the Parker and Aldrich beds. It is Pre-Quaternary streams are shown by dotted lines. usually associated with a limestone that is from 2 COALS IN INDIANA. Sangamon events. After the disappearance of not known to have been characterized by any not­ to 6 feet thick. The coal in Indiana rarely meas­ the Illinoian ice sheet there seems to have been a able events in the Patoka quadrangle. The land Petersburg coal. With a few minor exceptions ures over a foot in thickness and is frequently period of somewhat active erosion. In some other appears to have remained at practically the same none of the coals outcropping in that portion of absent. So far as known it has not been worked, regions the Sangamon streams were broad and elevation as during the deposition of the loess, the Patoka quadrangle included in Indiana are now even for local supplies. sluggish and eroded but little, but in the Ditney which suffered little erosion during the interval, worked, even for local supply, the beds rarely Aldrich coal. The Aldrich coal is another thin quadrangle, immediately east of the Patoka quad­ though doubtless there was a creeping and sliding being much over a foot in thickness, and often too coal and lies from 50 to 70 or more feet above the rangle, from 80 to 100 feet of the drift filling of of the material down the hillsides into the valleys. impure to be of any value. In the Indiana portion Parker. Like the latter it is generally associated the White River Valley over a breadth of 2 miles Wisconsin deposition. In the Wisconsin stage of the quadrangle there are but two mines, the with an overlying limestone, though in some places appears to have removed, while in the Patoka the ice, though failing by more than 75 miles to Oswald at Princeton, and the Diamond just inside the limestone occurs beneath it and at other times quadrangle the reduction of the drift deposits and reach the Patoka quadrangle, by its melting fur­ the quadrangle near Evansville. These mines is wanting. At its outcrop it shows a thickness of the widening, deepening, and cutting back of val­ nished large quantities of water charged with sedi­ reach what is known as the Petersburg coal (Coal 7 to 20 inches. It is of a somewhat better quality leys are conspicuous features. Large quantities of ments which flowed from the ice margin down the 5 of the Indiana geological survey), which out­ than the Parker, and has been worked at a consid­ drift were also probably removed from the Lake Wabash and White rivers and formed broad flat crops 12 to 15 miles to the eastward, in the Ditney erable number of points in the past. The old drift Patoka deposits, 25 or more miles east of the area plains of sand and fine gravel along their valleys. quadrangle. in the bluff 1 mile southwest of New Harmony under discussion, and along the valley of the Ohio The only deposits of Wisconsin age that still At the Diamond mine, Evansville, the coal is and the outcrops 6 miles southwest of the same River. Whether there was a slight uplift of the remain in this area are the stratified beds of fine 250 feet below the surface, or about 135 feet town are probably on this coal, as are also the out­ land or whether the acceleration of erosion was due sand and gravel, with their associated dunes, that above sea level. The bed in this mine is 4 feet 6 crops near Kilroy and along the base of the Mum- simply to the relatively steep constructional slopes occur northwest of the Wabash River, near Keens- inches in thickness, overlain by 2 feet of black ford Hills. Its greatest development, however, is of the drift deposits can not be definitely stated, but burg. The upper flood-plain deposits and the shale, which forms a fairly good and strong roof. along McAdoo Creek 2i miles west of Wadesville, the latter is now thought to be the most probable. great dune belts along the eastern edge of the Below is 2 feet of firm fire clay, underlain by lime- where it has been stripped at a number of points. Patoka. 8

The outcrop is shown on the geologic map. West southwest of Cowling. A deep drilling at Gray- Thickness of coals in Patoka quadrangle and vicinity Continued. of the outcrop it is encountered in many of the ville, made expressly for information regarding wells, the records showing the dip to be nearly flat. coals, failed to find any over a few inches in thick­ Thickness. Miscellaneous coals. Because of the thickness of ness, indicating that the Friendsville vein has Nearest town. Location. Source of information. Depth. Coal. loess and of glacial till and gravel it is impossible pinched out from 4 feet to nothing in the 3 miles to trace the coals continuously in the region north stretch between the town and the well mentioned. » Feet. Feet. of the drift boundary, and correlation is, there­ The bed has not been recognized in the wells at "P 1*1 Tl f* A"f" f\T\ i)pf*n "WA!I 80 li fore, uncertain. A coal which underlies a lime­ Mount Carmel, and there is every evidence that it 283 3 Millersburg. stone, probably the Somerville, outcrops with a has likewise pinched out to the east. 422 7 Petersburg. 471 7 thickness of 18 to 24 inches along the bottom of The Friendsville coal, when at its best, main­ 593 4 the tributary joining the Patoka from the south­ tains rather persistently an average thickness of 628 3i east at a point about 3 miles northeast of Prince- about 3 feet and is often accompanied by an over­ 670 4 ton. It has been worked occasionally. A coal lying limestone which in turn is in some places, Priiiceton ..... SW. i, sec. 7, T. 2 S., R. 10 W...... Hall well ...... 355 6 Petersburg. about 6 inches thick, belonging to the same gen­ especially in the northern portion of the quad­ 470 6 eral horizon, occurs beneath a thin limestone at the rangle, overlain by a massive sandstone. It is 670 6 730 7 level of the flood plain at Townsend's quarry. mined by a 36-foot shaft at the Couch and Adams 1020 3 The black shale exposed near low-water level mine, a mile east of Friendsville, and by a 32-foot SE. i sec. 7, T. 2 S., R. 10 W...... Thompson well...... 82 1 beneath the bridge one-half mile southwest of the shaft at the Grigsby mine, 2 miles southeast of 281 2 Millersburg. quarry is probably to be correlated with that over­ that town. One and one-half miles south of Bell­ 396 6 Petersburg. lying the coal at the quarry section. About 50 mont the Bellmont Mining Company has sunk a 462 5 feet above this horizon there is another coal, gen­ shaft reaching the coal at a depth of 36 feet. In 604 6 723 6 erally 6 or 8 inches thick, which has been seen in the McClearys Bluff shaft, 3 miles east of Cow­ NE. i sec. 18, T. 2 S., R. 10 W ...... 199 2 the ravine in the center of sec. 5, T. 1 S., R. 10 W., ling, the coal, here 4 feet thick, was reached at 346 7 Petersburg. and in the bluff southwest of Patoka, about 13 a depth of 35 feet, or about 10 feet below low- 451 2 feet above the river. The coal occurring in the water level of the river. In the past this coal ~Po4-A Well 56 1 bluff section at Patoka 50 feet above the coal just has been mined at Sugar Creek, at Maud, and 178 5 described, and again in the ravines li miles north­ at several points in the region just northwest 250 3i Millersburg ? 301 5 Millersburg. west of that town is correlated, as has been indi­ of Mount Carmel. The coal burns moderately Grove Mill...... Well ...... 408 7 Petersburg. cated, with the Parker bed. freely, but has a large ash constituent and does SW. i sec. 19, T. 1 N., R. 12 W...... Couch & Adams shaft ...... 36

bearing sands and gravels, often resting upon con­ coals is a bed 1 to 7 feet in thickness, the upper Princeton, indicating a very pure clay, with a buff in color, though gray, or even nearly white siderable thicknesses of these materials. Though half of which is said to be of excellent quality for remarkably low percentage of lime. The only types are noted. Brownish, reddish, and purplish apparently sometimes overlain by till, the beds terra cotta and similar products. A second bed, a other yard at Princeton is located near the junction tints are frequently present as the result of weath­ associated with the lignites are probably water tough, plastic fire clay 1 to 3 feet in thickness, and of the railroads, 1 mile northwest of the center of ering. Outcrops are especially numerous east of deposited. They are of no economic importance. appearing to possess high refractory properties, is the town. St. Joseph and Armstrong. Fine exposures occur sometimes found below the Millersburg coal.. Three A brick yard near the station at Owensville uses in the railroad cut near Inglefield, at a place 1 mile OIL, GAS, AND ASPHALT. miles east of Princeton, along Indian Creek, an the loess and produces a fair output of brick of northeast of St. Joseph, and in many of the Five or more wells reaching a depth of 500 feet under clay, 4 feet in thickness, outcrops beneath a good grade. At Fort Branch are the works of ravines between Inglefield and St. Joseph. The or more, one of them more than 1200 and one vein of coal, and li miles north of town is an William Pope, where tile has been manufactured for sandstone has been quarried on a small scale east more than 1400 feet deep, have been drilled at outcrop 4 feet in thickness. Both these clays are 15 years, but only since 1902 has the production of Inglefield and east of Wadesville. The rock is Princeton in search of oil and gas, but have met said to be of high refractory quality, and have been of brick been attempted. The pit when visited usually very soft on quarrying, but hardens some­ with little success. Small quantities of gas were used locally in making fire brick for furnaces and was entirely in the loess. The works of George what on exposure. Long continued exposure to obtained in nearly all of the wells, and in one or kilns near Princeton. Wehler, one-half mile west of Haubstadt, have the weather, however, frequently causes it to scale two of them very slight indications of oil are said At the southeastern edge of the quadrangle the produced common brick for several years, the or even completely disintegrate, making it undesir­ to have been obtained. Neither gas nor oil, how­ Evansville mines show fire clays beneath both coal output being reported to average 500,000 a year. able for important structures. ever, was found in sufficient quantities to be of any beds. That below the worked or Petersburg seam The clay bank is about 7 feet in depth, and as the The sandstone over the Parker coal is a cliff- commercial value. is said to be of quality similar to the clay associated lower portion is a little tough, it is necessary to making sandstone, and outcrops in the Gordon and During the drilling of a well by the Interstate with the same bed at Princeton. It contains some mix material from the upper and lower portions of Claypole hills, and at Grand Rapids, Hanging Gas and Oil Company at Princeton, in 1902, a pyrites, which can be easily removed, but is not of the bed to produce a brick that will not crack. At Rock, and Skelton Cliff. It is an even-grained 5-foot bed of asphalt was reported at a depth of so good quality as that below the Millersburg coal. Cynthiana brick making has been carried on for buff to gray sandstone of rather pleasing appear­ about 500 foot, or a little over 100 feet below the In Wabash County, 111., fire clays have been many years, but the only plant now running is ance, but, like the Inglefield, scales or crumbles on Petersburg coal. Small samples of the material reported in a number of deep wells. l At Mount that of Redmond & Company, which produces exposure. Large quantities were quarried at the brought out by the bailer showed the asphalt to be Carmel several beds have been penetrated, one about 700,000 bricks and 3000 to 4000 rods of northern end of the Gordon Hills for the piers of a jet black, nearly pure variety closely resembling showing a thickness of 9 feet being found at 49 tile in a year. The maximum depth of this pit is the Southern Railway bridge at Mount Carmel, but Trinidad asphalt in its reactions to physical and feet below the surface, one of 3 feet 10 inches at 8 feet. To obtain the best consistency the materials the stone was found to scale badly and it became chemical tests. A small bed of similar material is 62 feet, one of 4 feet 2 inches at 154 feet and from all parts of the bed from top to bottom are necessary to cover it with a protecting coating of reported to have been encountered in the old Hall above 7 inches of coal, and one of 3 feet directly mixed. Fairchild's tile and brick works, 1? miles cement. The same sandstone was also used in the well, on the southwest outskirts of Princeton, below the same coal. The coal outcropping along southeast of Poseyville, have been operated for construction of a dam at Grand Rapids. about a mile south of the new well, while in the Bonpas Creek, between Grayville and Cowling, is over 30 years. The loess is here less than 5 feet The sandstone over the Friendsville coal is a Oswald mine, three-fourths of a mile to the west, underlain by a light-gray fire clay, and in Craw­ thick and rather sandy. Three miles northeast of thick bed outcropping in the Mumford Hills, at a black substance, known as liquid asphalt, seeps fish Creek, sec. 5, T. 1 S., R. 12 W., a bed 4 feet Inglefield is a loess pit which formerly produced the lower end of the "cut off" near New Harmony, into the bottom of the mine at 430 feet to such an thick and of good quality is reported. good clay but which has not been worked for many at points northeast of this town, and along extent that some of the rooms have been abandoned Clays other than fire clays. Clays useful in the years. At New Harmony there has been a small McAdoo Creek. In the northern half of the and closed. It is said to enter through a nearly manufacture of common building brick and drain brick industry for many years, the clay coming quadrangle the sandstone is found just over the vertical "break" filled with clay. tile are of wide distribution and are worked at a from alluvium on the Upper portion of the flood Friendsville coal. It is gray to buff in color, and The fact that wells reaching depths of over 1000 number of points. The most valuable deposits plain north of the town, at the works of George in the southern half of the area frequently shows feet have been drilled at only one point shows that consist of loess and of argillaceous shale. B. Beale. The pit is 8 feet deep; the top is a cementation by crystalline calcite. It has been the territory has been by no means carefully tested. The shales, known locally as "soapstone," are tender clay, which is mixed with one-fifth part of quarried at several points, and has been used by None of the wells have reached the Trenton lime­ abundant throughout the quadrangle. The colors the underlying terrace sand to make it suitable for the Illinois Central Railroad in some of its bridges stone. While there is nothing to indicate the vary from blue to buff. They are often almost use. and in the levee along the bayou. presence of oil or gas in the region, there is noth­ free from grit and where weathered are soft and The only one of the numerous plants at Evans­ Thick sandstones outcrop in the hills southeast ing to indicate its absence, and it is not impossible soapy, although in fresh exposures they may be ville which comes within the limits of the Patoka of Hazleton, but in general are too soft to be of that drilling may develop pools of commercial firm and hard. The largest pit is operated by the quadrangle is that of Henry Alexander, on First use, though certain layers are sometimes worked value. Evansville Pressed Brick Company, and is situated avenue, north of Pigeon Creek. The pit is 4 feet for local supplies. At Townsend's quarry, 3 miles In general it may be said that the positions that just north of Pigeon Creek on the State road, in depth and the loess is toughest near the bottom. northeast of Princeton, a gray stone of fair quality are geologically most favorable for drilling are the where the following beds are exposed: Loess, 15 About 600,000 bricks are made annually. is taken out in some amounts. Both probably low anticlinal swells and the flat areas of the rocks feet; soft, drab argillaceous shale, 10 feet; blue Till is not known to have been used in the belong to the Inglefield formation. Sandstone was just east of the points where their westward dip arenaceous shale, 10 feet; and sandstone (only top quadrangle for the manufacture of brick, and formerly taken from the river bed at Rochester and changes from low to steep. The most pronounced exposed). With the exception of three bands of although the more clayey forms are often suitable between Rochester and Mount Carmel. A higher anticlinal swell is between Friendsville and Mount kidney iron ore, each 2 inches in thickness, the for making a fair grade of brick, the superior sandstone, of the Wabash formation, is quarried Carmel in the northern portion of the quadrangle, entire argillaceous bed is excellent material. For quality of loess makes it unnecessary to use poorer 2 miles north of Gards Point, in the northern por­ while the most notable flat area extends from north making brick it is mixed with the overlying loess material. tion of the quadrangle. of the Claypole Hills south westward to the south­ and enough argillaceous shale to form one-fifth of Analyses of brick clays. west corner of the quadrangle. Flat dips are also the whole, making a mixture with the composition encountered to the west of the low anticlinal swell given in Column I of the accompanying table of I II III Constituent. Evansville Prineeton Princeton mentioned. Both of these areas of flat rocks are analyses. It forms a valuable vitrified brick, which (shale and loess). (shale) . (loess) . marked by many minor undulations of the rocks, is strong, tough, and non-absorbent. some of which are brought out on the geologic map An exposure along the roadbed of the Southern Clay base and sand : by figures, which show the depths to the Friends­ Railway southeast of Princeton gives the follow­ Silica (Si0 2) ...... 65.87 62.04 71.20 ville coal in the northwestern portion of the quad­ ing section: Soil and loess, 12i feet; sandstone 6 Insoluble silica ...... 46.10 43.58 Titanium oxide (TiO s) ...... 1.10 1.30 .80 rangle. These minor irregularities are, perhaps, feet; gray argillaceous shale, 8 feet. The analysis Alumina (A12 O 3)...... 14.66 18.49 18.56 more likely to be important as regards the occur­ of the shale given in the second column of the 2.63 3.70 rence of oil or gas than some of the broader accompaning. table shows it to be of good quality 4.59 6.50 6.80 features, but they do not usually extend farther for paving brick. Aside from the two instances Fluxes : than a few hundred yards, and in most cases their mentioned, shale is not known to have been used Ferric oxide (Fe2 O3)...... 6.23 7.54 1.34 location can not be predicted. In the eastern half in the quadrangle. Ferrous oxide (Fe2 O) ...... 1.37 .06 .15 Lime (CaO) ...... 39 , ,.16 .14 of the quadrangle the dips are more pronounced, A number of pits' in the loess now furnish Magnesia (MgO) ...... 1.54 .91 .52 and are less favorable to the occurrence of the oil brick clay of good quality. Two of these are Potash (K2 O)...... 2.66 .93 .32 or gas in definite pools. located at Princeton, two at Mount Carmel, and 1 21 one each at Owensville, Haubstadt, Cynthiana, Soda (NaaO) ...... 1.30 2.04 1.26 CLAYS. and Poseyville. At Evansville, just outside the Total...... 99.72 49.94 99.97 47.28 100.59 The clays of the Patoka quadrangle fall into limits of the quadrangle, a score or more pits are 86.22 87.33 96.86 two general classes: (1) Fire clays or the refrac­ worked. All the companies make soft mud brick, 13.50 12.64 3.73 tory clays occurring beneath the coals and else­ and occasionally small outputs of tile are reported. Analyses I and III are by Robert Lyons; Analyses II is by W. A. Noyes. where in the Carboniferous formations of the area, The plants generally run only five or six months and (2) brick clays, including the less refractory of the year, and the entire production is usually BUILDING STONE. Limestone. There are three rather persistent clays, argillaceous shales, till, loess, and alluvial retailed within a few miles of the kilns. The red limestones within the limits of the quadrangle: (1) clays. The clays of the coal-bearing rocks of type of loess throughout the quadrangle is thought Sandstone. There are three general horizons of in the Somerville formation, (2) over the Parker Indiana have been investigated by W. S. Blatchley, to be of fair quality for making ordinary brick. sandstone in the Patoka quadrangle. The first, coal, and (3) over the Aldrich coal. Neither of these State geologist, and the results are published in At Princeton, in the southwestern part of town, which includes the sandstones of the Inglefield for­ is everywhere uniform in lithologic character, each the Twentieth Annual Report of the Department there is a large yard where the following section mation, is the most important, though the second varying from light-gray shaly forms through darker of Geology and Natural Resources. The portion has been opened: Loess, 10 to 15 feet; red pebbly and third, the sandstones over the Parker and gray fossiliferous varieties into compact and almost of the following discussions relating to this class of till, 10 feet; buff stratified sand, 10 feet. The Friendsville coals in the Wabash formation, are black types. The portions of the outcrops of the clays is based largely on that report, but the dis­ loess in this pit is a good brick clay, and the under­ strongly developed in many places. three beds that lie outside the boundary of the gla­ cussion of the other types of clays is based on the lying bed furnishes sand for the molds. The The sandstones of the Inglefield horizon occur cial drift are shown on the geologic map. Inside present field work. annual output of bricks is said to average 700,000, mainly in the lower half of the formation, the this boundary they are difficult to trace. Fire clays. These clays occur in beds of rather of which about one-third is shipped out of town. beds, which include a few thin partings of shale, The limestone in the Somerville formation is the widespread occurrence beneath most of the coal No analysis of the clay from this locality has been sometimes reaching, as in the bluffs in the valley only one that has been quarried to any extent. seams. East of the Wabash the thickest beds made, but Column III of the table gives the com­ east of St. Joseph, an aggregate thickness of more Near the eastern edge of the quadrangle the lime- known are at Princeton, where they have been position of the loess at an opening in southeastern than 60 feet. The faces of the cliffs are frequently estone appears to lie in two benches, each generally penetrated by several borings and by one shaft vertical and are marked by the presence of cavities less than 10 feet thick, and separated by a few feet 1 Worthen, Report on the Economical Geology of Illinois, sunk through the coals. Below the higher thin vol. 3, pp. 383-398. due to weathering. The sandstones are mainly of shale or sandstone. A few miles farther west the Patoka. 10 limestone appears to occur as a single bed, with a he first column of the accompanying table, which garden vegetables are raised. The average yield of ing 45 bushels per acre. The lower portions, next thickness of 10 or 12 feet, and still farther west jjives the types recognized by the United States wheat is said to be about 20 bushels and of corn the river, are subject to annual overflow and are and also farther north it is 5 or 6 feet thick. The Greological Survey. By the refined methods of from 35 to 40 bushels per acre. The accompanying never troubled with drought. They include some limestone has been used mainly as road metal, hysical and chemical analyses some of these soils mechanical analyses by the Bureau of Soils indicate of the best corn lands in Indiana and Illinois. though the more massive portions are sometimes may be still further subdivided. These subdi­ the physical character of the soil. An analysis of the river silts near Mount Vernon quarried for use in rough masonry. A large num­ visions, which are the results of detailed studies by Marl-loess soils. The marl-loess soils lie in two shows 2.42 per cent of organic matter, 66.70 per ber of quarries were formerly worked about Mr. H. W. Marean of the Bureau of Soils of the belts, one on each side of the Wabash Valley. cent of silt from .05 to .005 millimeters, and 28.42 Evansville, and small quarries have been worked United States Department of Agriculture, are given They do not occur over the entire area mapped as per cent from .005 to .0001 millimeters in diameter. farther north, especially near Kasson, Staser, in the second column. The third column states marl-loess, but only along the edges of the belts This soil is frequently underlain by a gravel layer Kratzville, and Inglefield. ariefly their occurrence in relation to the geologic next the river, the remaining portions being covered which is of great assistance in draining. The limestone over the Parker coal is from 2 to formations and surface deposits shown on the with common loess. In color the marl-loess is a Lake and subordinate stream silts. This class 4 feet thick and was formerly worked for road metal accompanying geologic map. The mechanical pale yellow or straw color. It is also in somewhat embraces the silt deposits of all streams except the 2 miles southeast of St. Wendells. It has also been analyses and many of the details in the following marked contrast with the loess of the common type Wabash and White rivers and the broad drift flats quarried 2 miles south of Armstrong. The description as to the productiveness are the results in composition, frequently carrying 5 per cent or marking the old lake beds. Most of the material Aldrich bed runs from 2 to 6 feet in thickness, and of the careful examination by the Bureau of Soils. more of CaCO 3 , while the latter generally contains is derived from the erosion and redeposition of the has been quarried in the past at several points Residual soils. Although the rock underlies the less than 1 per cent. It weathers to a deep reddish loess and is therefore exceedingly fine and clayey. south of Big Creek. Neither of the limestones loess and drift at very moderate depths over the brown and frequently shows abundant lime, even The material is generally strongly weathered and leached of its lime. The stream silts are generally are worked at present. Larger part of the uplands, it has been removed at the immediate surface, while in the common A limestone, possibly that of the Somerville for­ only on the steep bluffs and the sides of the sharper type the lime is rarely present at the surface. Its overflowed annually and are frequently wet throughout the year in places. Where artificial mation, occurs near the level of the valley floors ravines. The soils of this type are usually stony, soil is superior to that of the common loess, with of the tributaries of the Patoka River northeast sandstone fragments predominating, though occa- which it is sometimes mixed as a fertilizer, with drainage has not been established the old lake flats of Princeton, and is reported beneath the sandstone lional shale soils were noted. The slopes on which some success. The following analysis, taken from are also very wet. Corn is the best crop, yielding at Townsend's quarry. A limestone is frequently they occur are generally too steep for cultivation the Thirteenth Annual Report of the Indiana 50 bushels per acre in places. Good crops of grass found with the Friendsville coal, but it outcrops and are covered with moderate growths of timber. Geological Survey (p. 46), gives a fair idea of its can also be grown. only for short distances near Friendsville. There Drift soils. As in the case of the residuary character: In the class of subordinate stream silts may also be included the clayey soils of some of the low are also numerous thin limestones of local occur­ soils, it is only where the slope of the land is so Chemical analysis of loess, Posey County, Ind. rence, but they are generally too thin to be of value, steep that the coating of loess has been removed terraces bordering many of the streams of the quad­ though beds have been opened near Rochester, that the drift soils are found at the surface. The Constituent. Amount. rangle, especially in the southern half. north of Mount Carm el, and at a number of other soils are generally sandy or even gravelly, but Swamp deposits. In this class are included the 1.35 black silts, mucks, and peaty deposits that occur in points. clayey types are not uncommon. Because of their limitation to steep bluffs and the sides of ravines Soluble organic matter...... 30 the various depressions of the flood plains and on TncrVlnT^lA snlii^A't'.AQ 73.30 GRAVEL AND SAND. they are never cultivated, but are generally the broad drift flats. The depressions of the flood 10.00 plains are of two types, the broad, shallow depres­ Gravel is found at slight depths at many points timbered. Lime ...... 6.80 sions, representing incomplete upbuilding of the on the Wabash and White river flood plains, and Common loess soils. The common loess forms TM"Q O»V*OQI S\ * . 3.78 occasionally forms the surface layer. In a few the immediate surface over the entire quadrangle, Alumina and peroxide of iron ...... 2.80 plains, and the relatively narrow bayous and other instances it has been hauled for short distances and except on the river and stream flats and over the .12 abandoned stream channels. The broader depres­ T ./-\OCC QVirl fllkflllAtt 1.55 used as road metal, but in general no use is made narrow belts of sand and marl-loess hills along the sions are usually filled by the slow accumulation of of it. borders of the Wabash Valley. It is generally of Total ...... 100.00 ordinary river silts, which are washed in at times Sands are found at many points on the Wabasl a light-buff to reddish-brown color, though becom- of flood, and which are mixed with accumulations and White river bottoms, and in the sand hills Sand-hill soils. The sand hills of the quadran­ of leaf mold, etc., giving a black color to the whole. Mechanical analyses of loess soils from a point 1 mile north Occasional cypress ponds and swamps, in which (old dunes) along the east side of the Wabash of Mount Vernon, Posey County, Ind. gle are of two types, the first including the rela­ Valley, and to a less extent near Patton, Keens- tively fine white sands extending from Keensburg the accumulations are almost entirely of vegetable burg, McClearys Bluff, and Cowling on the west inches0-8 surffromace. inches8-36 surface.from westward to Bonpas Creek, and the second embrac­ matter, are found on the Wabash flats, especially Diameter in side. As a rule no use is made of this sand, millimeters. Conventional name. ing the wider interrupted belt of coarse sands northeast of Mount Carmel, on the Indiana side of though there are two large pits west of Princeton extending along the eastern border of the Wabash the Wabash. The bayous are generally filled with flats from near Hazelton to the southwestern limits silts mixed with large quantities of leaves, logs, etc. where considerable quantities have been taken out .0001- .005 Clay ...... 13.68 9.10 of the quadrangle. In general these sand hills are Many depressions in the surface of the drift flats for use in mortar and for other purposes in that .005 - .05 Silt ...... 81.82 84.16 city. Small quantities are also occasionally usec .05 - .1 Very fine sand ...... 3.86 5.92 so porous and are so well drained that they are marking the beds of the old glacial lakes have been in sanding the molds, or mixed with the clay at .1 - .25 Pine sand ...... 36 .50 poorly adapted to general farm crops, but large occupied by shallow water bodies even up to within the various brick yards. .25 - .5 Medium sand ...... 08 .12 quantities of watermelons are grown, 500 to 1000 the memory of many of the present inhabitants. .5 -1. .14 .10 car loads being shipped annually from Posey The soil of these portions consists of a black muck SOILS. Tots il mineral matter...... 99.94 99.90 County. Stock peas are raised in small amounts, containing more or less silt washed in from the sur­ The region in which the Patoka quadrangle is Org 2.47 .34 and wheat does well if it follows melons in rotation. rounding areas. The soil is very fertile and after situated is primarily an agricultural one, and con­ Mr. H. W. Marean, of the Bureau of Soils, believes drainage yields as high as 50 bushels of corn, 25 tains some of the best agricultural land of the two ing pale at times. The upper 9 inches is usually that alfalfa might profitably be introduced. bushels of wheat, li to 2 tons of clover, or li tons States. The staple products are corn, wheat, hay fairly open, but below the limit it is more plastic, River sands and gravels. In this class are of timothy to the acre. The higher portions of the and watermelons. Sorghum, broom corn, anc tenacious, and clayey. Under cultivation it included the areas of coarser materials of both the flats are characterized by the redeposited loess soils tobacco are raised in limited amounts. Artificia becomes ashy gray in color. The materials of the lower and upper levels of the Wabash and White of the previous class. fertilizers are seldom used. Fruit is grown to onlj loess were originally derived from diverse materials River flats. These areas, being limited to original RECLAMATION OF BOTTOM LANDS. a limited extent, though many varieties do well that were scattered over wide areas and it thus con­ depositional elevations, are of slight extent as com­ Apples, peaches, pears, plums, and grapes ar tains all the essential ingredients of an unusually pared with the areas of fine silts filling the inter­ Ditches. One of the notable features of the sur­ raised. fertile soil. It gives good yields of corn, wheat, mediate depressions. In general the soils consist face of the quadrangle is the existence of numerous The soils of the Patoka quadrangle may b clover, timothy, and would probably make good of buff sandy or gravelly loams which nearly wide flats bordering the present rivers and larger divided into nine very distinct classes, shown ii tobacco land. Fruit, especially apples, and some always contain considerable quantities of fine silts creeks and also occupying areas that are supposed to and in places are mixed with considerable quanti­ have once 'contained the larger lakes, such as those /Soils of Patoka quadrangle. ties of vegetable matter, giving almost black colors. north of the Patoka River, southwest of Princeton, In general the sandy soils are most common near east of Cynthiana, and about Poseyville. The SOIL NAMES USED BY H. W. MAREAN, BUREAU . "' .GEOLOGIC EQUIVALENTS. DESCRIPTIVE TERMS USED IN THIS FOLIO. OF SOILS (Ms. of report for 1902). the immediate banks of the rivers, where additions flats of bothl types originally included extensive are constantly being made by overflow or through undrained areas, shallow lakes of considerable size Steep slopes of Carboniferous the action of wind. remaining in the depressions throughout the year, Residual soils. deposits. The higher portions of the sand and gravel flats even within the memory of many of the present inhabitants. Within the last forty years, however, Drift soils. Steep slopes of morainal deposits. will yield an average of 25 bushels of wheat per acre, and will afford good crops of clover or timothy. and especially during the last decade, numerous Common loess soils. Common loess. About 40 bushels of corn per acre may be obtained. ditches have been dug and the lake areas have been Miami silt loam. The sandier upper portions in places yield good drained, and some of the finest crops of the region Marl- loess soils. Marl-loess. crops of melons. are raised where the waters formerly stood. Even River silts. By the term river silts is meant now, however, though large areas, especially .on the Sand-hill soils. Miami sand. Earlier and later dune sands and Wis­ those finer deposits which have been mentioned as Wabash flats, have been drained by the McCarty, consin terrace deposits (in part). occupying the original depressions of the Wabash Blair, Stunkle, and other large ditches built by and White river flats. The material is largely county aid, many square miles of bottom land Wisconsin terrace deposits (in part) Miami sandy loam. and upper and lower flood-plain what may be termed a coarse silt. While much within the quadrangle are yet to be reclaimed for River sands and gravels. Yazoo sandy loam (in part). deposits (in part). Natural levees. finer than the sand of the preceding class of soils, agricultural purposes. These undrained areas sup­ it is coarser than the clayey silts of the smaller port a heavy growth of timber, which is now being Yazoo sandy loam (in part). streams. These silts appear to be composed of rapidly cut off both by lumbermen and farmers. River silts. Yazoo loam. Upper and lower flood-plain deposits Yazoo clay. (in part). particles which, as compared with those of the clay Dikes. The lowlands along the Wabash and soils, are only moderately weathered. They con­ White rivers are protected in some places from the Memphis silt loam (stream) Older stream silts. stitute, next to the loess, the most important soils scour of the overflowing waters in times of flood by Lake and subordinate stream silts. of the quadrangle, comprising the larger portion of systems of dikes or levees. The most important of Waverly silt loam (lake or swamp). Glacial lake deposits (in part). the Wabash and White river flood plains. Owing these are located near Grayville, one on each side to the very recent drainage of much of the area of of the river. The one on the south extends along Abandoned channel deposits. Swamp deposits. Griffin clay. Swamp deposits. the flats, large tracts are still timbered. The the neck inclosed by the sharp loop of the river on cleared areas produce large crops of corn, averag­ which Grayville is located and has doubtless been 11 of importance in delaying the formation of a cut­ As many as forty or fifty species of trees may be The accompanying table gives a list of the princi­ calcareous tufa several feet in thickness, "crowded off at this point. The second dike extends along found in a single 50-acre lot, and very seldom does pal trees of the quadrangle. Nearly all are of more with impressions of leaves and mosses. The water the west bank of the river from a point about a a particular species predominate over all the others. or less value for lumber. Originally the cotton- at present flows downward in a definite channel mile south of Cowling to the southern portion of This feature has done much toward the preservation wood, hickory, elm, gum, Spanish oak, and syca­ several inches in width and bordered by an elevated the area in the southward loop east of Gray ville. of the forests, the lumbermen in many instances more were the principal trees, but there were a calcareous rim or miniature levee about 2 inches simply culling out the particular species having the number of pecan, walnut, water oak, white oak, broad. FOREST RESOURCES. greatest value at the time. Rankness of growth is bur oak, white ash, poplar, cypress, and a lesser Next to Dripping Spring the most notable fea­ Originally the forest lands of the Patoka quad­ especially marked in the abandoned channels and number of the other species. With the exception ture of this type is the line of springs occurring rangle consisted of two well-defined types: (1) The in partially filled bayous. Grape vines up to 32 of the water oak, sweet gum, black or yellow gum, along the bluff at an elevation of about 30 feet heavily timbered bottoms of the rivers and larger inches, trumpet vines up to 38 inches in circum­ and the various hickories, a large proportion of the above its base for about li miles west of Hazelton. streams, and (2) the more thinly forested areas ference, and immense cross vines are found pendant timber of value has been cut. The trees just The conditions are not clearly shown, but the water interspersed with open prairies of the uplands. from or clinging to sycamore and other trees from mentioned, however, are still being cut for timber appears to issue directly from a tufa bed, which in Since the settlement of the country, early in the 5 to 10 feet in diameter, while the smaller vines along the Wabash, important mills being located at turn is overlain by a sandstone, both apparently century, great inroads have been made into the frequently form impenetrable networks. Although Mount Carmel and Grayville. belonging to the Carboniferous rocks. The tufa, forested areas of the bottoms, especially since one of the rarest of the southern species, the bald although very open and porous, and marked by WATER SUPPLY. small convolutions and other similar structures, Larger trees and shrubs of the Patoka quadrangle. The surface of the Patoka quadrangle may be sub­ does not appear to afford any traces of vegetable divided into lands of two classes, the first including Maximumh't Maximumcir­ impressions. The mineral matter itself is of a branches.first cumference. the broad, flat bottom lands bordering the Wabash, Maxi­ Author­ harder consistency than that at the Dripping Common name. Specific name. Habitat. mum height. ity.* White, and Patoka rivers, characterized by a never- Spring. Tufa blocks of a similar character were failing water supply at slight depths, and the found in a ravine cut in the drift 3 miles south­ second embracing the remaining portions of the west of Hazelton, but their origin could not be Feet. Feet. Feet. quadrangle, including the uplands and the rela­ determined. Taxodium distichum ...... 146 74 19 J. S. Uplands ...... 75 5 R. R. tively narrow bottoms of the smaller streams, char­ Besides the springs mentioned there are numer­ 117 R. R. acterized as a whole by a deficiency of water during ous smaller ones in nearly all of the sharper rock Upland hills...... 155 74 22 J. S. the summer months. The sources of supply are ravines, both at the borders of the flats and in 175 90 16 J. S. streams, artificial ponds, springs, and ordinary and the Claypole, Gordon, Mumford, and other rock 113 R. R. artesian wells. "islands" that project through the Wabash flats. Uplands ...... 129 R. R. /Streams. The only streams maintaining any The limestone outcrops, especially those of the Shellbark ...... 119 8 J. S. Uplands ...... 112 55 10 J. S. notable flow through the drier seasons are the Somerville formation, are frequently marked by Pignut ...... 120 8i J. S. Wabash, White, and Patoka rivers. Of these the springs of small size. 134 10 R. R. Wabash is by far the largest in fact, it is stated At a few places the springs are used for domestic Salix nigra ...... J. S. that its volume at its junction with the Ohio River purposes or for watering cattle, but this source of 70 1* R. R. is greater than that of the latter above the junction. supply is in the main rarely available, mainly Uplands ...... 97 44 R. R. During the summer the water is frequently nearly because it is generally found only in ravines and Swamp cot ton wood. . Populus heterophylla ...... J. S. 170 75 22 J. S. colorless and carries but little organic matter. It other similar situations, where the surface is too River birch ...... Uplands ...... 105 10 J. S. is used as a source of municipal supply at Gray­ rugged for cultivation. 122 10 11 J. S. ville, at the western border of the Patoka quadran­ Wells of the river flats. Under the term river Chestnut ...... Uplands ...... 100 + R. R. gle. The water is not so wholesome as could be flats are included the bottom lands of the Wabash, White oak...... 150 60 18 J. S. wished, but it is probably superior to that of the White, and Patoka rivers. The materials of these 103 10 J. S. Ohio River. flats vary from fine clay-like silts, or even muck, Bur oak ...... 165 79 22 J. S. 100+ R. R. Next to the Wabash in volume is the White upward to coarse gravel. In the Wabash flats Chinquapin oak. .... J. S. River. The water, though not generally so clear sand and gravel predominate. They usually 100 -f- R, R. as that of the Wabash, is frequently nearly free obtain an abundant water supply at a depth of 15 119 13 R. R. from sediment during the drier seasons, and is feet, and it is almost never necessary to go more Red oak...... 150 R. R. probably equally wholesome. The Patoka River than 25 feet for a supply. Practically all the f~^n Pi*f*n Q r* r\f* OITI f*n 181 94 20 J. S. is the smallest of the three perennial streams; in wells are driven. The wells usually go through a 160 75 20 J. S. Quercus digitata ...... 100+ R. R. fact, in seasons of unusual dryness it is hardly few feet of clayey silt and then strike coarse sand 135 9,3 1* J. S. more than a series of mud holes, frequently filled or quicksand. The clay is usually gray or black J. S. with rotting logs, through which a weak flow is at the surface because of the contained vegetable 65 *u R. R. maintained. The water is always highly charged matter, but is gray, bluish, or greenish at a depth Shingle oak ...... 100 R. R. with sediment. It is, nevertheless the source of of a few feet. The gravels contain all types of Ulmus pubescens ...... J. S. ' public supply for Princeton, the largest city within fresh, unweathered pebbles, many of them being of 119 R. R. Ulmus alata ...... J. S. the quadrangle, and although disagreeable in Canadian materials. Quartz pebbles are, however, 136 J. S. aspect, does not appear to have any very marked generally the most common. Large bowlders are Sugarberry ...... Celtis mississippiensis ...... 100+ R. R. effect on the health of the users. reported in some wells. 62 20 10 J. S. In wet years the Fox and Black rivers, and Bon- The materials of the White River flats are of 100+ R. R. pas, Pigeon, Big, and Flat creeks maintain weak the same general character as those of the Wabash Tulip tree...... Liriodendron tulipifera...... 190 91 25 J. S. flows nearly if not quite through the summer, but flats, but are, perhaps, a little finer on the average. Uplands and bottom lands ...... 48 2* R. R. Sassafras ...... 95 75 8 J.,S. in dry years dwindle to series of disconnected and Water is readily obtained. The Patoka flats are 164 80 17 J. S. stagnant pools. All of the smaller streams go dry composed of more clayey materials. Gravels are Sycamore...... Wet bottoms along streams ...... 176 68 33 J. S. each summer except a few that start from springs not commonly reported in the wells, the water being Vv "1 1 f\ f*Tl f*T*T*V Upland hills...... 135 10i J. S. and flow short distances before being absorbed or derived generally from quicksands. Near the river 156 61 18 J. S. evaporated. the wells are usually not more than 15 or 20 feet 48 Water locust ...... 90 R. R. Springs. Springs are numerous in the sand hills deep, but farther back, and especially near the Grymnocladus dioicus ...... 129 J. S. 95 111 R. R. bordering the Wabash Valley on the east, especially borders of the valley, an abundant supply is more Uplands ...... 118 60 12 J. S. along the base next the flats, and give rise to a difficult to dbtain, some of the wells deriving Black maple ...... Uplands ...... J. S. number of brooks, some of which flow for a mile water from depths of 75 to 100 feet. 118 R. R. or two before they are absorbed by the sands and The water from the Wabash and White river 108 60 13 J. S. gravels of the Wabash flats. It is probable that flats is generally soft and pure, but sometimes 01 Boxelder...... 60 60 R. R. the loess, marl-loess, or till that in many places carries lime derived from calcareous clays which are Ohio buckeye ...... 83 3 R. R. 135 50 Q8 J. S. underlies the sand furnishes a relatively impervious occasionally present. Mount Carmel obtains its 100 t- R. R. stratum, which causes the water to appear at the supply from wells sunk in the flats. The water of Black gum ...... Nyssa biflora ...... Drier bottoms and uplands ...... J. S. surface, although the finer sand layers are known the Patoka flats is generally good, though it is 115 80 5* J. S. to be the determining factor in some instances. frequently hard, and often tastes strongly of iron 124 R. R. The water is usually fairly soft and pure. sulphate. The latter substance is especially likely White ash ...... Fraxinus americana ...... Uplands ...... 144 90 17 J. S. The drift hills bordering the flats between the to be present where buried wood or lignitic beds 138 16 J. S. Fraxinus lanceolata...... 100 f R. R. White and Patoka rivers on the east side of the are encountered. Black ash ...... 100+ R. R. Wabash Valley also give rise to numerous springs, Wells of the tributary valleys. The coarse sands 101 48 6 J. S. but the streams from them are soon absorbed. The and gravels of the Wabash and White river flats water is more likely to be hard than the water from were derived from places at considerable distances to *J. S., Dr. J. Schneck, Seventh Ann. Rept. Indiana Greol. Surv., p. 512; R. R., Robert Ridgway, Proc. U. S. Nat. Mus. the springs in the sand hills, but is a pure and safe the north at a time when the northern portion of the vol. 5, pp. 55-57, 1882, and vol. 17, p. 419, 1894. drinking water. State was covered with ice and the glacial torrents the opening of the drainage ditches of the last cypress is probably the most noticeable of them all. The rock hills are also sometimes' the source of were discharging large quantities of sands and decade. On the uplands, however, there has in It is limited in occurrence, so far as was seen, to the springs. Perhaps the most notable of these is gravels into the headwaters of the streams men­ places been a rapid encroachment of young forests cypress swamp just northeast of the junction of the Dripping Spring, located on the face of the bluff tioned. Their tributaries, however, had no such on uncultivated portions of the original prairie White and Wabash rivers. Large trees formerly bordering the Wabash flats about 4 miles north­ source to draw upon, the materials they transported lands. grew here, some of them measuring 22 feet or more west of Owensville (NE. i sec. 33, T. 2 S., R. being derived at first from the rather fine and The most marked features of the forests are the in diameter above the basal swelling and 90 feet 12 W.). This spring, which is one of the largest clayey glacial drift and later from the loess coating. absence of coniferous trees, the many species grow­ high clear of branches, but most of the perfect trees within the quadrangle, emerges at an elevation of The result is that the deposits of the tributaries ing together, the great number of southern species, have now been culled out. They are associated about 25 feet above the base of the bluff, over the consist largely of clay or of interrupted beds of very and the rank growths of portions of the bottoms. with sweet gums and ashes of even greater size. face of which it has built an irregular coating of fine sand, and these, as compared with the White Patoka. 12 and Wabash deposits, contain relatively little water. usually good, but sometimes tastes strongly of sul­ wash plains between Princeton and Fort Branch lenticular and disconnected character of the beds There is rarely a point^ however, where wells do phate or phosphate of iron. Samples of the latter water is commonly obtained at a moderate depth of the Carboniferous series, few if any of the beds not obtain a fair supply near the center of the val­ mineral (vivianite) were found in the gravel from except near the moraine, in the vicinity of which continuing without interruption for any consider­ leys, although nearer the sides and in the smaller one well. some of the wells enter the rock. Wood and coaly able distances. tributaries, where clays predominate, the success of Wells in the loess. By loess is meant the more matter (lignite) are reported in many of the wells. Among the few flowing wells the following may wells is less probable. The water level is not so or less clayey silts which everywhere cover the Most of the water from the drift is hard, and water be mentioned: (1) The Bixler well, about 5 miles near the surface as on the river flats. The quality uplands, whether the latter are of rock or of tasting of iron sulphate or iron phosphate is not southwest of Haubstadt, which delivers good water of the water is generally good, though in some wells gravelly drift. As the loess is rarely over 20 feet uncommon. at a height of 3 feet above surface; (2) the Silas the supply is hard or even marked by the presence and usually 10 feet or less in thickness, only the Shallow rock wells. Most of the upland wells, Redmond well, east of Cynthiana, 80 feet deep, of iron sulphate. Logs of wood and coal beds shallower wells derive their supplies from it. even when dug, enter the rock for short distances, mostly through "blue mud," which obtains from a (lignite) are frequently reported in the deeper wells. Although it undoubtedly holds large quantities water generally being obtained in some one of the quicksand water that rises 3i feet above the sur­ Some of the wells enter the rock. of moisture, its clayey texture and the absence of numerous sandstone beds. In many instances, face; (3) a well If miles northeast of Poseyville, Wells of the sand hills. Nearly all of the water sandy layers prevent the easy passage of water however, the water does not occur throughout the 126 feet deep, sunk through sand or gravel all the falling on the sand hills bordering the Wabash through it, and only in relatively rare instances sandy stratum, but only in rather definite channels, way, which finds water in gravel at 85 and 126 Valley sinks into the ground at once to the basal does it furnish a considerable supply, the majority neighboring wells often varying greatly in amount feet that flows out at the surface; (4) a well at the portion of the sand, where it meets the underlying of the wells failing in years of drought. The marl- of supply. The rock water is extremely variable foot of the bluff south of the Wabash River, 2i impervious loess, which it follows until it reappears loess, or the coarser and more calcareous type occur­ in quality, much of it being excellent; while some miles north of Savah, drilled for coal, in which as springs along the base of the hills. Wells some­ ring along the east border of the Wabash Valley, of it is hard or is charged with iron sulphate, which water charged with iron sulphate rises 2i feet above times find water in this basal layer, but as the water is more porous, but does not usually hold water, impregnates especially water derived from places the surface. tends to follow channels on the underlying surface except near its base. From this portion, however, where coal beds have been encountered. Wells in Cisterns. Because of the insufficiency of the the higher portions are practically dry and success­ water is frequently obtained. The water from the the rock on narrow ridges or on the edge of steep supply derived from the shallow wells of the loess, ful wells are not numerous in the sand hills. Many loess is generally hard, and sometimes contains bluffs are usually dry throughout several months drift, or rock, a supplementary supply consisting of the sand-hill wells obtain their supply from the sufficient magnesia to have a deleterious effect on in the year, and many of the shallow wells in other of rainwater is frequently collected in cisterns. underlying rocks. health. situations are dry at times. Many of the inhabitants have been forced in late Wells of the old lake flats. What is here termed Wells in the drift. Under this term is included Deep rock wells. The Carboniferous rocks of the years to rely on cisterns as the only source of old lake flats are those broad, flat areas such as those more or less sandy or gravelly materials sup­ region consist mainly of shale and sandstones in domestic water supply, as" numerous wells, because occur southwest of Princeton, east of Cynthiana, posed to have been deposited either directly by the frequent alternation, the sandstones often being of improper location, have become badly contami­ south of Poseyville, and at other places, where ice or indirectly by streams leading away from its water bearing. Wells drilled to a depth of 200 nated from outhouses, barns, drains, etc. The deposits are supposed to have accumulated in margin. The principal deposits of this type are feet usually obtain a satisfactory supply of water supply furnished by the cisterns is rarely sufficient, broad shallow lakes ponded in front of the ice those forming the moraines shown on the geologic either from the sandstones or from beds associated however, for other than domestic uses, and water margin when it occupied this region. As these map. The sloping plains leading eastward from with the coals or limestones. The water associated for stock is often hauled from neighboring streams. materials were derived from a glacier that was near the moraine between Princeton and Fort Branch with the coal is likely to be charged with iron sul­ Artificial ponds. Except the cypress ponds at hand they are frequently rather coarse, but at to the vicinity of Port Gibson, near the eastern phate resulting from the decomposition of pyrite, occupying depressions at one or two points on the other points may consist mainly of clay. In the boundary of the quadrangle, are believed to have while the water from the limestone and even some Wabash flats and the occasional bayous, neither of lake flats southwest of Princeton wells obtain been deposited by streams flowing from the ice of that from the sandstone is hard. In many areas which are of importance as sources of water, no water from sand or gravels at 15 or 20 feet, on top margin and are classed with the drift deposits. The little but shale is encountered and no water is found natural ponds occur in the area. The loess soil of which rests an impervious clay bed. When this composition of the deposits is far from uniform, even at considerable depths. This is especially with which the larger part of the uplands is covered is penetrated the water sometimes rises rapidly in and from this it follows that, the water supply is true in the portion of the quadrangle lying within is rather impervious, a fact that is taken advantage the wells to within 10 feet of the surface. The very variable. While one well may yield an the State of Illinois. of at many points by the construction of small wells of the lake flats west of Cynthiana and about abundant supply another near-by well may be an Notwithstanding the regular westerly dip of the artificial ponds, which furnish watering places for Poseyville are not uniformly successful, the mate­ utter failure. In general the higher and more rocks, which affords the structural conditions for stock. The water in these ponds is, however, very rials penetrated consisting largely of clay. Many rugged the drift hills the less will be the supply of an artesian supply, very few of the wells flow. In muddy and is generally of inferior quality. of the wells enter and derive their supplies from water. Thus in the high drift hills between Patoka fact, no definite water horizons have been recog­ the underlying rock. The water of the flats is and Hazelton water is rarely present, while in the nized. This is probably due to the well known May, 1903.