UNITED STATES GEOLOGICAL SURVEY CHARLES D. WALCOTT, DIRECTOR Moogep lt ay oe OF THE ' : : BY So FRANK LEVERETT WASHINGTON GOVERNMENT PRINTING OFFICE 1902 Pe Sa Se pies Mee 551.3 HAG VA | PET ER Oi nes iT TA, University oF Cuicaco, March 13, 1901. Sir: I have the honor to transmit herewith the manuscript of a mono- graph by Mr. Frank Leverett on the Pleistocene geology of the region between the Ohio Valley and the Great Lakes. This is the second con- tribution of Mr. Leverett to the series of monographs in course of prepara- tion on the glacial formations of the Northern States, and is a fit companion to his Monograph XX XVIII, on The Illinois Glacial Lobe. The plan of the monograph and the method of its development are essentially the same as those of its forerunner. As in the preparation of that volume, our working relations have been of the most intimate kind, and I joi with the-author in the hope that it may prove an acceptable contribution to the Pleistocene problems of the United States. Respectfully, yours, T. C. CHaMBERLIN. Hon. Coarues D. Waucort, Director of United States Geological Survey. MON XLI 2 17 PUBLICATIONS OF UNITED STATES GEOLOGICAL SURVEY. [Monograph XLI.] The serial publications of the United States Geological Survey consist of (1) Annual Reports, (2) Monographs, (8) Bulletins, (4) Mineral Resources, (5) Water- Supply and Irrigation Papers, (6) Topygraphic Atlas of United States—folios and separate sheets thereof, (7) Geologic Atlas of United States—folios thereof. A circu- lar giving complete lists may be had on application. The complete list of monographs follows: MONOGRAPES. I. Lake Bonneville, by Grove Karl Gilbert. 1890. 4°. xx,438 pp.,51 pls.,1 map. Price, $1.50. Il. Tertiary history of the Grand Canon district. with atlas, by Clarence E. Dutton, Capt., U.S. A. 1882. 4°. xiv, 264 pp., 42 pls., and atlas of 24 sheets folio. Price, $10.00. III. Geology of the Comstock lode and the Washoe district, with atlas, by George 1 Becker. 1882. 4°. xy, 422 pp.,7 pls., and atlas of 21 sheets folio. Price, $11.00. IV. Comstock mining and miners, by Eliot Lord. 1883. 4°. xiv, 451 pp.,3 pls. Price, $1.50. V. The copper-bearing rocks of Lake Snperior, by Roland Duer Irving. 1883. 4°, xvi, 464 pp., 14 11., 29 pls. and maps. Price, $1.85. VI. Contributions to the knowledge of thie older Mesozoic flora of Virginia, by William Morris Fontaine. 1883. 4°. xi, 144 pp., 54 ]1., 54 pls.| Price, $1.05. VII. Silver-lead deposits of Eureka, Nevada, by Joseph Story Curtis. 1884. 4¢. xiii, 200 pp.- 16 pls. Price, $1.20. VIII. Paleontology of the Enreka district, by Charles Doolittle Walcott. 1884. 4°. xiii, 298 pp-, 2411., 24 pls. Price, $1.10. IX. Brachiopoda and Lamellibranchiata of the Raritan clays and greensand marls of New Jersey, by Robert P. Whitfield. 1885. 4°. xx, 358 pp.,35 pls., 1 imap. Price, $1.15. X. Dinocerata. A monograph of an extinet order of gigantic mammals, by Othniel Charles Marsh. 1886. 4°. xviii, 243 pp.,5611.,56 pls. Price, $2.70. XI. Geological Theta of Lake TuaTivon am. a Quaternary lake of northwestern 'Nevada, by Israel Cook Russell. 1885. 4°. xiv, 288 pp.,46 pls.and maps. Price, $1.75. } XII. Geology and mining fad niin of Leadville, Colorado, with atlas, by Samuel Franklin Emmons. 1886. 4°. xxix, 770 pp., 45 pls., and atlas of 35 sheets folio. Price, $8.40. j XIII. Geology of the quicksilver deposits of the Pacific slope, with atlas, by Georve F. Becker. 1888. 4°. xix, 486 pp.,7 pls., and atlas of 14 sheets folio. Price, $2.00. XIV. Fossil fishes and fossil plants of the Triassic rocks of New Jersey and the Connecticut Valley, by John 8S. Newberry. 1888. 4°. xiv, 152 pp.,26 pls. Price. $1.00, XV. The Potomac or younger Mesozoic flora, by William Morris Fontaine. 1889. 4°. xiv, 377 pp., 180 pls., Text and plates bound separately. Price, $2.50. } XVI. The Paleozoic tishes-of North America, by John Strong Newberry. 1889. 4°. 340 pp., ' 53 pls. Price, $1.00. XVII. The flora of the Dakota group; a posthumous work, by Leo Lesquereux, edited by Eb. H. Knowlton. 1891. 4°. 400 pp.,66 pls. Price, $1.10. XVIII. Gasteropoda and Cephalopoda of the Raritan clays and greensand marls of New Jersey, by Robert P. Whitfield. 1891. 4+. 402 pp.,50 pls. Price, $1.00. } XIX. The Penokee iron-bearing series of northern Wisconsin and Michigan, by Roland D. Irving and C. R. Van Hise. 1892. 4°. xix, 534 pp., 37 pls. Price, $1.70. XX. Geology of the Eureka district, Nevada, with an atlas, by Arnold Hague. 1892. 4°, xvii, 419 pp., 8 pls. Price, $5.25. XXI. The Tertiary rhynchophorous Coleoptera of the United States, by Samuel Hubbard Seudder. 1893. 4°. xi, 206 pp.,12 pls. Price, 90 cents. I hp? ‘Sth II MONOGRAPHS. XXII. A manual of topographic methods, by Henry Gannett, chief topographer. 1893. 4». xiy, 300 pp., 18 pls. Price, $1.00. XXIII. Geoloey of the Green Mountains in Massachusetts, by Raphael Pumpelly, T. Nelson Dale, and J. E. Wolft. 1894. 4°. xiv, 206 pp., 23 pls. Price, $1.30. XXIV. Mollusca and Crustacea of the Miocene formations of New Jersey, by Robert Parr Whitfield. 1894. 4°. 193 pp., 24 pls. Price, 90 cents. XXV. The Glacial Lake Avassiz, by Warren Upham. 1895. 4°. xxiv, 658 pp.,38 pls. Price, $1.70. XXVI. Flora of the Amboy clays, by John Strong Newberry; a p sthumous work, edited by Arthur Hollick. 1895. 4°. 260 pp.,58 pls. Price, $1.00. XXVII. Geolovy of the Denver Basin in Colorado, by Samuel Franklin Emmons, Whitman Cross, and George Homans Eldridge. 1896. 4°. 556 pp.,31 pls. Price, $1.50. XXVIII. The Marquette iron-bearing district of Michigan, with atlas, by C. R. Van Hise and W. S. Bayley, including a chapter on the Republic trough, by H. L. Smyth. 1895. 4°. 608 pp., 35 pls., and atlas of 39 sheets folio. Price, $5.75. XXIX. Geology of Old Hampshire County, Massachusetts, comprising Franklin, Hampshire, and Hampden counties, by Benjamin Kendall Emerson. 1898. 4°. xxi, 790 pp.,35 pls. Price, $1.90. XXX. Fossil medus:e, by Charles Doolittle Walcott. 1898. 4°. ix,201pp.,47pls. Price, $1.50. XXXI. Geology of the Aspen mining district, Colorado, with atlas, by Josiah Edward Spurr. 1898. 4°. xxxv, 260 pp., 43 pls., and atlas of 30 sheets folio. Price, $3.60. XXXII. Geolugy of the Yellowstone National Park, Part II, Descriptive geology, petrography, and paleontology, by Arnold Hague, J. P. Iddings, W. Harvey Weed, Charles D. Walcott, G. H. Girty, T. W. Stanton, and F. H. Knowlton. 1899. 4°. xvii, 893 pp.,12L pls. Price, $2.45. XXXIII. Geolovy of the Narragansett Basin, by N.S. Shaler, J. B. Woodworth, and August F. Foerste. 1899. 4%. xx, 402 pp.,3l pls. Price, $1.00. XXXIV. The glacial gravels of Maine and their associated deposits, by George H. Stone. 1899. 4°, xiii, 499 pp.,52 pls. Price, $1.30. p XXXV. The later extinet floras of North America, by John Strong Newberry; edited by Arthur Hollick. 1898. 4°. xviii, 295 pp.,68 pls. Price, $1.25. XXXVI. The Crystal Falls iron-bearing district of Michigan, by J. Morgan Clements and Henry Lloyd Smyth; with a chapter on the Sturgeon River tongue, by William Shirley Bayley, and ap introduction by Charles Richard Van Hise. 1899. 4°. xxxvi,512 pp.,53 pls. Price, $2.00. XXXVI. Fossil flora of the Lower Coal Measures of Missouri, by David White. 1899, 4°. xi, 467 pp., 73 pls. Price, $1.25. XXXVIII. The Illinois glacial lobe, by Frank Leverett. 1899. 4°. xxi, 817 pp., 24 pls. Price, $1.60. XXXIX. The Eocene and Lower Oligocene coral faunas of the United States, with descriptious of a few doubtfully Cretaceous species, by T.Wayland Vaughan. 1900. 4°. 263 pp., 24 pls. Price, $1.10. XL. Adephagous and clavicorn Coleoptera from the ‘Tertiary deposits at Florissant, Colo- rado, with descriptions of a few other forms and a systematic list of the non-rhynchophorous Tertiary Coleoptera of North America, by Samuel Hubbard Seudder. 1900. 4°. 148 pp., 11 pls. Price, 80 cents XLI. Glacial formations and drainage features of the Erie and Ohio basins, by Frank Leverett. 1902. 4°. 802 pp., 26 pls. Price, $1.75. In preparation: _ —Flora of the Laramie and allied formations, by Frank Hall Knowlton. Series. Author. Subject. [Take this leaf out and paste the separated titles upon three of your cata- logue cards. The first and second titles need no addition; over the third write that subject under which you would place the hook im your library. ] LIBRARY CATALOGUE SLIPS. United States. Department of the interior. (U.S. geological survey.) Department of the interior | — | Monographs | of the | United States geological survey | Volume XLI| [Seal of the depart- ment] | : Washington | government printing office | 1902 Second title: United States geological survey | Charles D. Walcott, director | — | Glacial formations and drainage features | of the | Erie and Ohio basins | by | Frank Leverett | [Vignette] | Washington | government printing oftice | 1902 4°, 802 pp., 26 pls. Leverett (Frank). United States geological survey | Charles D. Walcott, di- rector | — | Glacial formations and drainage features | of the | Erie and Ohio basins | by | Frank Leverett | [Vignette] | Washington | government printing office | 1902 4°. 802 pp., 26 pls. [Unirep Srares. Departinent of the interior. (U. S. geological survey.) Monograph XLI.} United States geological survey | Charles D. Walcott, di- rector | — | Glacial formations and drainage features | of the | Erie and Ohio basins | by | Frank Leverett | [Vignette] | Washington | government printing office | 1902 4°, 802 pp., 26 pls. [Unrrep Sraves. Department of the interior. (U. 8. geological survey.) Monograph XLI.] Til Tooeanke . Low plain south of itare Ontario * Niagara escarpment Plain south of Niagara escarpment Corniferous escarpment Lower Helderberg limestone Oriskany~sandstone ase 2. 3). 2k Sos ee Comiferous limestone 22 =... 8). _ 5.2 CONTENTS. feiidson@hiverscTOup =.= - ce oe eee eee { Medina STOUP Eee oa! als a eae Didiafe terete Clinton PTOUP eee Sea ae oss 2 4NeS a BMI AGAMA OT OUP Setar spo = |e 2/<)oio= elt eae a a Salina and Waterlime, or the Onondaga series Genesee, Portage, and Chemung, or Ohio shale series Waverly /orsBediordishale)—-\_ == -- 5-422 eeeseeeeenee a= Berea grit and shale (Catskill?) Cuyahoga shale (part of Pocono sandstone of Pennsylvania) Logan conglomerate (part of Pocono sandstone of Pennsylvania) Pottsville, or Conglomerate Coal Measures Allegheny, or Lower Productive Coal Measures Conemaugh, or Lower Barren Coal Measures Monongahela, or Upper Productive Coal Measures Dunkard! beds (Permian?) -.-.-.-_-.--- 222 2225.-12.: Plain south of Corniferous escarpment......-------- Grand River Basin Bee SCLOLOp Wier Basiny seeps Sci 2.2 Sem ee iy a felt Muna 1 ev sunce River Basin Pits 56 * 1712957 6 en : Page. CHAPTER IJI.—DRAINAGE SYSTEMS ------------- -------- +--+ 22-22 e ee nee n ne ene eee ene +: 82 Section I.—Ohio River system ......-.---------------------------=-------=----5------ Ee 82 (Oni JRIW@? {4 Joes Besse ehh dons seaeeaeocsoe eS sosantsaseessccteseecs-25 (pozecsesase- = 382 ate. or tall iaj2 32s So a eo eee a ore ele ee 82 Effect of rock resistance on size of valley .--..-.--2------ = seers nee 84 TRovelke eelemavelsprunn Wore \ellle\y, ee oes ec ose sess sesso scsssoeseos0~=- 84 Upper Ohio or old Monongahela system -..-----.-------------.----------------:. 83 Mang) @lGl Chivas o= 56 3-256 dot seo sanec eco scsossssesssecssssscesesseeccsurc= 88 {Nave Teor ebeol OWI 5 ea eee eee ae 2 ce ss aoe se se= co ssessocsccre= 94 Extent of the old Monongahela system ---..----- Sabie, t sa oot eee ee 98 Mhevold divide on the Allleghenty === = 22 py: eee eae HR 0 98 Middilel@hio or old Kanawha System - 2220 S225 22 eee eee eee eee 100 Mihreynorblawarrl outlets se ee ere ee ele ee 101 Wetlections/ ol drainage eels e Soe e = eee eye eee eee ee see 104 ower@hio system... 2.262502 0 20... 2 St SSeS eee eee ea 109 TPO) ol Olle bares BAS Se apes esac sed sesgacsscdssassseacseeogssco==" 109 Relation to topographic features ..-.....------.--------- ee sess Se 109 Mentiamyatlucviia WG CMOS ts) eae ee eee ee eee 1 Gradation plains below the level of the Tertiary deposits .............-.--..- 113 Wramage) changes mean’ Cincinnati. = 2= 22) ae aee ee 116 Relation of the glacial deposits to the erosion features of the Ohio Valley ..-..-.-- 118 Onvthe Wower Ohio 2.3. 22.2 2 2 Hae anes eee eee ee 118 (OnmukresViicidile Ohio pees aa eee eee eRe aS Obs yGodcns So Se: 119 Ongthe Upper Ohio —=- 2. oe. 2-225 =. eee eee ler ree 121 AllleghenyaRivers. Lo 2. 22a Rees Se ote ne eee ences ee ee 125 fvatenototall si): Sai oe2 pepe ee WS eaage "digs Sides ee ae oe ee 125 Rock MOOK. 62/225 .22 sas. 8 he kess bec acct eb oa doe ee eee 127 Wescription/of the valley, 23-520. 23. ==; Se eae ee ee ee 128 OldhUipper-Alllesheny, draimacelsystemi= = 5 - =e se ee een 129 Old) Winddle-Allesheny drainage systems) 92222 522s reese eee ae eee eee 132 Old drainage between the Upper and Middle Allegheny drainage systems------_.- 138 TowerAllegheny andl its tributaries 2-52-24 2ss2] oaa6 = ae ee ee 143 BOaVERARIVER Sj): =cine = = + 38 ds Qe en Cee Se oe eee eee eee 148 Tattle BeaverngRiver 2/2652! 2 eke a 0 eS ee 152 MuskingumiRivers 2220202002 0 eos ese Se 153 The oldiwestward outlet. = 2.492. 82 Sos4cs ge cee See ee 155 The present line of discharge ....... (Levit ded. Slee Lee 156 Deposits on the lower course of the Muskingum ....-...------------------------- 157 Striated blocks in Muskingum Valley near McConnelsville..-....--.-----.------- 158 Extent of the old Muskingum drainage basin.................-...--------------- 158 Drainage tributary to the westward outlet --.-..----.-----.2-s52-seeo se eeeee eee 160 Changes)in'Owll Creek drainage/basim= 3-255 -225 ee =oe ee 160 ChangesimiClear Fork of Mohicani@reek. 2) 2022. 52s ee oe gal O2ie Changes in other headwaters of Mohican Creek ___.-._.. 2-22-22 -ee eee eee eee 162 Kallpucksi@reele oo 00.0) GUS ge Ss 2a se SI 165 The oldyWUipper Tuscarawas drainage! 20)! ase eee sees ee 165 Mocking Rivetegs. ie. eke as lo, ee eee 169 Mhe presentidrainage 2-23... Sse 2.2 eee ee ee 169 Changestini the headwaten pontion== 9-922. se nese eee er 169 Raccoon Creeke oo... 2. 8. e225 eg ge ee ee eee 172. Symmesi@reckwe re 256. 2b ee as 2 ie el re RAR ie 173 Mintle Scioto River ...20.- 22.2652 aE OS ee 173 SciotowRivier 220202... de aele cSk ea 174 Pheiheadwater portion 2.255525 92. Sa ie re 175 Mheilowericounse:. _ 2.2 355.50 Us rr 177 CONTENTS. ij : ais add titan st Ae se =* AeA Meee ay Pe ee on i ee ee pen 1 de ee ee ee i = Ae ak MSR Ae Bie tee ie nthe a4 oi Srp len vm ta sian ad emer 4 Sa RR Aves earner eee ee Ae eT +e RW ee hem A She oe een iba ae Sid le ale SAA ar elles ian ey, wie oye ei a hw em Pere ena ve the Winkwenh fe: scpitsaeabak nein ‘ a COM “ness ining cnc ese i Glaciati pone ise Vic, je nin coe Nl Gc nen ee i ie aes Metal hes oa dU ee Minor tributaries of Lake Omtexiex je western, New Yorks... erecta Tiersen Coitarrse and Connesist orenke: Ay Grand yO SOSA RM eee ion arretaalpnan in “ Wemnition ee ae : aes “Huron River beens ry Pea 3500 een deie ele td all eater & “Opa MAT tll a ne. VAR Mies CONTENTS. Carter III.—DraInaGE systpmMs—Continued. Section I.—Ohio River system—Continued. Scioto River—Continued. Western tributaries south of the glacial boundary ....... Beaver OLeeketmr raat yet ean Shae ooo ek Se HRATOLO esta eeoes ey ese ee eer eS ewes te -/s\oe sees Changesbinkdmain age seer eye sc ae ae eee CreappViaMmiW@hivyeh sees see nace SNe sk hes Re ypnesenit] Sy Sle nies eet eases. c= Changes in drainage. -.-..----------- Canepa tune aot Wihite water Rivensec- cee sass sere rn sactios Jeis secteet Lose iRhespresentrsy stems en secre ees aioes seem seen (Chanvesmmudialn ase seems sasee ete eS ee ens Tributaries of the Ohio in Indiana --..-....--.---.......-.. WrabashwRivier system's se sem seeenote asses acces Sees oe Wabash) Riverseenas ee oes = ae ie nec ac ae aes arse ee PBS BRiisy Cees rea ee eee ea es ee IN MippecanoemRivenwaee see see e reese se niece oes Wes taWhiterRaiv ei eer a eee ees aa ae aha ey UES Tasty Waid ARN Or. GSA so ao Soe aE bbe eee ses Ree RE See aneeee Section II. St. Lawrence system .._....-...._...-.----- Re ego (Genesecidrainagelbasin= sess sees seis esse ese Genesee River .....-.---- OA See is Soya sad esemees Genesee;olacial Walkesunegacmeen e522 tes eae VVoralriallel AKC ee ueee aeons sey laa. 2/20) Nalgene Changes of drainage on the tributaries_-_......--.------ Minor tributaries of Lake Ontario in western New York-.--- Bighteenmailey Creeks sess sees \See esis sci - t eee ee WattaraugsusiCreckssee sss os 2 ee nae nes oneae Small tributaries between Cattaraugus and Conneaut creeks.-_........_.......__- CGonnesanty Creckseet eee. a. 532 Fase sae eee Chacninwivenseass ae mee saasee seteeaseswaseee see seeks Cuyahoraphivereras scccice socccc. sa seee seeeeee sees Rockyehiveteaeecee =< she cess Soest ease eae ee ee eee IB ACk@Rivermeememe a2 2 sree scott Geesee setae seems DaNGuskyPRLVeras eee, sce oss nn Setisinia cle ee eae Seee ee WIP UIMECCHLVCT AS See amen acon ace sine e eee eee Eee CHAPTER [V.—THE DRIFT BORDER OR GLACIAL BOUNDARY....---.---- Section I. The border of the oldest drift (Kansan or pre-Kansan) 8 CONTENTS. CHarrerR 1[V.—THE DRIFT BORDER OR GLACIAL BOUNDARY—Continued. Page. Section II. The border of the Illinoian drift .............--.--------------------e--- eee 222 Section III. The border of the Wisconsin drift.........-.------------------------------- 226 CHaprer V.—THE OLDEST DRIFT (KANSAN OR PRE-KANSAN) ...-..---------------------+----- 228 Generallistatement ees oo ke soc sens elk oe See 2 ee Oe a ete pene eee rar eer 228 Description/of the drits. 2222222. s2 seek ie 2 wn oo 2 eee eee eee eee ene eee eee Beeeeee 228 AmoumtiOfenOslOmis ssn eosin cee ek ak cect 2S Se Se SS eee reget et ae a 235 Characteniofatheroutwashe2 2:22.62 se eecccs os eee eee eeeeee eee eee eee 237 Tionestay Valleys ss-- 226220 ca iuee cen sobs case eso n eee Ee ee eee eee eee eee 238 ower Allesheny Walleye. 2\ 22-24 5iSo2. 22d a0-c ice oe See eee eee Ree eR RCE e eee 239 Wpper Ohio Valleys. 8822 boii sens eee een oe oe oh eee ee eee ee eee eee nee 249 Beavers Walleye sabe ee eos 22 ce tele oe e\sete Says a Yas Sole CREE eee Seer eee eee 251 GraprEn Vil Tam SInTINOTAN (DRIFT SHEET): . ....0. ---2 o> o- ose eis ene nee eee eee eee ae eee 253 Section eaBeatunesinernitie dnt border 2... 2- see see eer eeee rene eee ne eeeeeeeeeeeer 253 Generalistatemlent yas se here /a/Sk.ae.cteler= HepSteie ie Sects Soe Grate Pe ee Oe ee oe ee eee 253 Topographic expression of the drift border...-........---.---.---------------------- 254. Structuneworthoerdnithibordermeac a+ 6 S35 oes. 2 eos ee ee ene eee ee 261 Section II. General aspects of the Ilinoian. drift sheet................------------------- 270 Sections ieiC@haractenotutheroutwash= 2-80-32. -eee oo eee ee ae eee eee Eee eee eee 285 Generalistatementus sae 2s ne elo. 5 Sn ee eee 285 SandivaCreeka Valley eas se ie So oe soa cae on ee Se eee epee Cnet er cee seers 285 Rscanawaspandebniubaniese qs 2S 5 22S ee ye ere ee 286 iicking= Miskin oummValley. e322 7282 aiilee<\n)s\-[ ss ee eee nee eee eee nie ae 286 tockimomVialll eye ein a8 eis Te aes Sh eee ete ee ear 288 SalltuCreelkvialleye 25 5 ee 2c. Se eae bc eeu eels ci) SSeS REE eee eer aerate 289 SclotomVallle vier tyes esc Heke alot ci eee oe lee eer eee aera ae eee ae 289 mi vuddlerandmcower Ohio walleys.-2.--8- 222.2555 93 daceegeeeee cee eee eee eee 290 CraptTer VIJ.—Tar SANGAMON SOIL AND WEATHERED ZONE ..--------------------------------- 292 CHAPDER ALD —— lini) DOESS AND ASSOCIATED SILTS 2-2-2 5 2s. Sees eee eter eeeeeeele eae aeeaee er 295 (Generalestatementuses nee teh et acess Pale lane Ss 2 Jo Je ME ee ee rey Se eee 295 IDEA OUMONS -2 LS soo be esa ee eae eee oe eee ere ecm aceemorce soacuscoes 295 TBhickmessoimbmersilteete sso fees. oS GG 22 os. oe ae ae See ee eC See ee eee 296 (Gara Chen sitGstee ae eae ewe Car @ else ee sce en ote ees SR Cee EEE Ree Bee ee eee eee 297 COlOMe esas Wale so cn ssc ono ee anche eos See ee ae ee tee 297 MPEXGURE EE cae vers bins eee a sewnSgel botlee eee ee SRO eee ee eee 297 C@hemicaliconstitition) =... :..- 22-2 ee eee 298 Mineraloprcalsconstitttion=.4555 sec eee eee eee eee eee eae eee 298 Probable Iowan age----...----- besosess ScSkeeee cise Use Seca cee eee eee ee eee eee 298 Mod ekoigdepositlonee seetie7 ciceg. 2 so- 62-52 So oe ee eh ine bee hee eee REE E eee EERE 299 CuHAprer [X.—THE PEORIAN OR POST-LOESSIAL SOIL AND WEATHERED ZONE (TORONTO FORMATION?)- 302 CHAPTER NG — DEmEynART val WAISCONSIN: DRIFT... +. + 212 = S20 ocean cde acc nee ee ee EERO nae eee 304 Generalestatementtemsemas- ecce occ s see ke. 22 ce set nde caine eee REE Eee See 304 Section I. Early Wisconsin drift of the Miami lobe......-..-.-...---------.------------- 304 Mheroutenormlantwellomorainey- 5.82 22 oS. 5 eee eae > oe ee 304 IDiinlloninomn’. \s-baocss sae ee oer em Sse 2s Oe Ok obo5 odode 304 IRGC. 26 seco Sepete nee eee eee een EU LS SS ose desces 307 Rancemmralibde: Leesa sess eos poet ee ole Oe ay en 307 Mopoerapliyesse sees ose | SSE eS Da. a Se ee 308 Siruchuneyancanhickmess; ot Glre\chast hte 2 er Ce eae 312 TRON ICIS SEO os ee ee ae eee OME MIE et os ose oSke 325 SUITES a SSC ORM eG Oe aise ieee enemies ae eC een eR MERAE NES CES A i oa SOR 326 ImMensDOnGemmalstnictysssse ase 2. selec e im sch Sache este ae 2 i ne eR 328 Mono pian lanyghtet Pie sree yeh eh Jere pea SR A Oe Ue ee eee 328 SHAM UOIRE Ore Waeolabinos oe ee sane aaa anes aE AM MMO, EE YT a 330 Wharactemomtheroutwashtss ssc cease ease SU See Gy ae) 834 CONTENTS. 8) CHAPTER X.—THE EARLY WIsCcONSIN DRIftT—Continued. Page. Section II. Early Wisconsin drift of the Scioto lobe -...............-.------------------- 340 ImtiroductonysstaleMen te anos mee enna c en sce acs = Se seh o aa ce eae tomes 340 RHerouteror Cuban orain eases eee sa esas oes so sei) e eS etna Does soo UUS eee 341 DIS tae Ut OT es ee r= ts ee eS ete nee ere Soe ise elise aes JOR SEIN ore 341 IRSA « Sacked OSes SEES REG SESS os 65 OS Si5 SSE Ee crete ete ee ie a ee ary EL. SE 342 Rane eunyal titid Gt). evn seepeeeee bees jee tea oS otbe ele yee 343 HOO etrarp Diy gees ots See el ae Se oe ai eine ae Hey ee 343 Simuctuneanduchickness! of theldritiwesser eee aoe eee ote ee eee we 344 TBS OGL ey; erases ote ape =a eee bs lets sey ee Veda 347 Inmers bord eryphenomen ae ere ee eee ee een tee) cts ne ole el 347 SEES oo. co Re AcOH o> RENEE SE Ese Nels cosa te ee A aT ee 348 Outewborderphenomenal sco cis eee pee erent a eae a2 2)5. oe sic luee | Ta 349 Section III. Probable early Wisconsin drift of the Grand River lobe...._......._.._.____. 351 CHaApTeR XI.—THE INTERVAL BETWEEN THE EARLY AND LATE WISCONSIN DRIFT..________________ Bhy CHAPTER XII.—THE MAIN MORAINIC SYSTEM OF THE LATE WISCONSIN STAGE..--.-..____._______- 354 Sectionw lew imytbnes Mi amano Det = ays) Lye = ee ee rae Sr eae aero eae i ee Vn | 354 PIU Sr O TAIN CS fea ase rars area a aches Si ES Se Tero oa oan Shave ee Pee eer ane 354 Generalistatement esos js Xe RE mes sete a ceed Jace abet ai by eae 354 Distributions aeerscts cr rsralo.4 54 -cla oe epee ee eects ee tae OE ee 354 HRC Le Les een seer tet AS oth oe sc cers Ei Ss ecto) Lt wa Mere 306 Rang eumtal titwdeier ce ee 22-2 Seer ee eee ye teee tee eer cs cence en mee week 356 UO SOSA I 7 ecto sa me Soe CO MaRe EASES COsESds ce Saabs SORTA BRE SEE Ean e Mae euas oe eue 357 Mhicknessrotthe vanity ater Sora SO re eat eer rsiesiata stay ee a 361 Structurerotithevdiriitee = 25 05 2ir eae ae UME pu ALLE oy al me 362 TERN UO UETRS) ee SN ee pea EER 53 ca ei 371 Charactenombheroutwashtenc (2.4 322 eee enemas mea mete SUL 373 SITES i Sa USMS eB SER OR Ie Kale ae ERE A Ce telstra Sere ata ee a op 380 Inner border phenomena .-.--.------- Bea cUnncr otc se Sande Gem ee Ena yer ean erpanede 381 SectionpewimythesSciotoudoberer foe) tsar 5 seein ee tutes ce pene OE ESI esi l yd 382 hemyYemibenstoiith e7sy sterner —— 5 ~ 2-1) eae ep ane rary leat esieataye ees iat peat 382 Distnibublonyasers stacey). 22 a1 2 =o SOE ey eae Se Scot ete NR Ae 382 TRamee nme el tL UUG eee eee era 2 2 = reste ee erate ee eens eke 385 WReliiet eee ipre rte are ei. Ws oie Se eae a ate So ta ae 386 Moporrapphygmepes © eyo. 4 i= cals elect Ree eee ea toe Seed oo Me ce ts ee 387 SHED MINS OVC! auch rales ose wWoyenObawR oo ted snd oe e eeu ssesaseos se donee 399 Interlobatestractreast of theyshouldermesss- = reee- enn ae ee 401 Mas glagniclerr Or WAS SOOO NOS -oodosssesstenedesncassonsesadeese sc eeeoceue 403 Mnekeastennylinaly {orate wa ais Gb eee eae eee yee eo 405 Mibennesternulim bonithermneinel o lye yee area aera a ene eee at amr Ria 414 BO Cersis seeps ee sy. ya a aye tte ae ye Ot EU ae rae sl Ohc O 420 DRESS. ss eee: 6 oS ME ees OS BME daa mmc ea Cee ea tn Cee LO eee AE 422 Imneniborder phenomena =.05 425 eee eee ee ee eles Sere ae eres ee Ame LT oie 426 Generallieatures 22). Sass See Seer Pekameele eee Seal ee Se ae eee 426 Weaken Oral es Yc. Piste ae eee tae eee ey cE Es CAA Rae AS oo 3 Dg 426 Pickering Lomi esier <= a= sachet a emia eos ioe Sets Se as eines a ia)e ae 428 @irclewillereskers2 o2 tris saree ante es ete Liste ON a er ak SS A 429 Stiructuneyandsthicknessioteuhe; davitpesere psa ae aes 2 eno a IN 431 BO wlderibeltss 55242 Aare eee ae ee eat ae epee SU 2 ia CR a ET ae a 435 inner border phenomenajmithe shouldensess4 68.2545... -seeeeoe sence en eee es 436 Sections lle eimatheyGrandahivend obese meet artes ea es 2) eps ee en ee 437 Morainestofathe tsystemnsen sme ieee are a ee ee at ek a ae 437 Distributions ses ersee ee eee a rina isa ao aie ae ae Scie os bases ss Saar ceee eee te eee 437 Rane epinialibitad eyewear se se eine sae eee oe ele ce ce ae son ie oe 439 Topocraphiygeeerics soe ela ease see - sees tis de cece cinice Goce seeds sacs Se Ue ease oe 441 10 CONTENTS. ' Cuaprer XIJ.—THE MAIN MORAINIC SYSTEM OF THE LATE WISCONSIN STAGE—Continued. Section III. In the Grand River lobe—Continued. Moraines of the system—Continued. Strictunetandathicknesstot ithedmifty2: 225 5 \seseee aes eee ae eee Inner bord ergphenomenar fs: sien) oa2 ane Bos eae BORO EPC EEE Eee CE eEEES Generalfeatunes,.< -12se..02 aera eo ow CAI se Sane Se SENS ee ee ee Wrealkemiorainest. 9-22.61. 24 52. Jee bcd a2 k's Sh age ee DO eis leis atne cia ee ee oe ee St Sno gkde Drumalins\ (2) ise So seme iciat aie sb 2 Sn Skee ee ae eee eee Pillsplaimsieyes sees bs Boece Gai. eels ol SS Race ee eee eee eee PORTA CEE ee sie ys eters Sako wie cereus SS ia olde SENSIS SES eee eR ee Correlation and chronological position.-.-...-.--.-.-----..-----------------------=- CHaprer XIIJ.—Mrnor MORAINES OF THE LATE WISCONSIN STAGE ...-.....-----.-.---------- Section I. Moraines of the Maumee-Miami lobe....-........-----.-----.---------------- Wnionvinvorain ex.s sess aoe = ass coo eae eld as ci otAese eae: eee ee eee ID}istirall ou oVa, A ee ett ee ee eee ee me on Seon Gone See besaanoae IReaye7S tlie) ACE, Sar ee eee eee eee Ee Se emer sre och casesceseedenaasone MoWopmayp liye share rere ators d areola aie os ora EE oe ae eee ee eee Miveknesstindisimuciuneron the diihtee sees as ee see eee Outenborderphenomend) ——. ==. so- = 2 <2 lee eee eee ae eee eee 677 iiamipuretmoraine 22. see eee meee Caos 5 5) 88 ee eee ie ate ee ee 677 DIstMipUMOnIEee ness ease oe Se eos oo cele ae ee ee eee 677 Rangenmbaltitude 2... 9522-2. 2-—- snide Gdee donee BOSC te aE eRe + 678 Surface contours -.--..------- Ws edness 22 2S So eeeaeeer ee eee ee ee 678 Structunelotsthe diritti: 232-2 6252. c oo. os 2 i oe near eee ene eee eae eee 679 @Outerborder drainaves= 2... 05.2 sei 242s ee eee eee ete eee Eee eee 679 Marillaimiordine weer sesee ces csces nese oe cle a eee eee eee eee eee ate 681 Distr outlOneeees i= Scene eso k.ciseSaeiee a= = oe eee ee ee Ce eee 681 Rang enmnualltithd Cheese te. Sa ene ee ee eee eee ee ee eee eee 681 Mopograip liye Nasties tea = ls Seite s I5 We te ee oe eet 682 Structurevoti they diritti 25 223 !c << hee cinat be aban ese eee ee eee eee 682 Relationsto WakeuWihittlesey@< -....-.2 42 5-2-2825 S2 eases eee ener eee eee eee eee eee 683 Outer borderidainage: << 2-2-5. 52 53.-5).cce bed aie see eee Pee Pe eee Renee 683 IA denim onaine mses 2 Sc ee Se kie soci Re Bee eS OEE EOE eae eee 684 Distrib ublonys seer oases se eis ete ys hee alke s Sie Susle See Se Se eo on 684 Ramee vintakbitud evs sees te sk uae cess ce eens eee eee eee eee eee 684 Mopocraphypesee ses ee ee ms. oe See eases ace weenie ne sche e eee eee Ree eee eee 684 Structuneroitherdriitesseee sot os ta5- 55s. dobar cek eee eo seeeee BEC eee eee eee eae 685 Outerybouderdrainawe= seas. oc esse us skee ht Soe ose o a eee eee 685 Relationpioslake Warnenea- 2 sees 22 38 Sn eae cee Sen eee eee eee 685 Pemlbrokeinidg estes se saser ces sacie te csiaee Bence nena bees aeiee 9 aoe ae een 685 Distribublombes ste eee cee sos seas eso welctcjelaid biG epstel a eo, ski oe) eae eee ee 685 IRaAETD TN MINOR. aod oksoe oes Heep ee Oat en eceesonereee saab enesaccsouscsses 686 MONON) jsoscesccosscebssnacossscuosseenoeasssesese coseeigeencusosysasooss 686 Structunevotutheidrittessesas- sen oe Seno Se eS Se Lo ee eee 687 Ojeiiar lonley chime gs- 5553s bcasce sheers seoseodedsoeseson see see soessi2ss5ca2 687 CONTENTS. CHapTerR XIII.—MINoR MORAINES OF THE LATE WISCONSIN STAGE—Continued. Section V. Moraines of western New York south of Lake Ontario—Continued. Dafa apm Oraln ewer: so 2.\<.5 2 h..te cscs ee eee ene erere ie MEA RCs 9 gee oe ala Tete LOS {nei XBR AIG oo nee ee tet se i Lym Sesh chelate UNE SMe a ace pane enmialtiiitd eye) 3 k= 5 cl eye oe eee een ye. be ca eee Mo popmany liye ayia (a4 | oe eee eee mene tate he oe teigg seca ed ce MURUCLUNCTO lb Mena rath es 53,5 cit a RN PIC ny eS AE oe ayia ts Ramee soya Gui errs sea ciao 2S ene eee See MS ne ope RelA este oe oye & PL OPO RAT eee Ao ois ie)s cian, amine ee eee tea Ae Seite WN ok ge od SUE OLE MONE), ae’ CODD Ae eae sen ee acs Sno cS ssc Se CE Se Us See ee ae omens PRAM ee mati bG eee ee aers ste ee oi: 2 Sah a I ae erence NE Ee ERO PORTA liye ae ke tele eles aso 5 = ce -Sicis S ee a RN ae oe ae eee 22k SinUChune Olah ents perce oslo as 2S sae ae eee eee ne Aen ae eee tn Raneeyimial Giolid 6 seen ae a ciein sie 65 bn) 2 Sore Ree ee Eee Stoo -8 Gai eae cea a pornap Dy geen eee er: 5c <5 aS ne cee ae Ey reste ste SE se PSLAOKEL DURE NCO} ELH] XEN (GN AU CIs tee es are eR ta ne od A Ne Rat en Toneribord erphen omen dae). 52.5 S84 a2 Ae ee eta eam eee eiccs en LYNE An Glacialistirizeee eee ewes sz eae os Li). at Je eee eee See aie eee TB SUL te So aM TROTS MBLE OTN SAS Sere em ie: ere Sere atte ey ee en ee gOS SS rn 2 eo years Oe ae aa a ons Mena CHE Gr \Wellopytael Brats (Olena ee ee oe =o ce ce on Sac an Soe eeeemeceoeeeo seo Srsmullen@neela@ Mam elise eae sey ace enya ks he ge eye me eA ose A SES Uae Ens CUAL TES yes ees ele en rans ES OE Ws ele ee ce ea The Maumee beaches from the Fort Wayne to the Imlay outlet -........-...--...--...--- Metailedidescnipwonees see sass e Les le. Oe I eee ee re ie moe kT ‘Vania tionmaralioitud Cecseee asso nsec! a 2 ul See nee tease, freemen oo Spe Mhesouthishorejoilbaker Maram ee ryote S22) 2s ae alee re eee e tea Re) aay y gS a Wetailledk descrip tlone sy eres sas nies sas oy CLA ee ere re Sree sseemene Ee a Wariatlombime aipih ere rae crete esau sn =o Suhel Ne ee ae eons Sot ee PRS 2 lh Calisestonjiwowbeaches!S 4a 8c ese ce calc eee tee ee Eee see twe ee Ab eee CEAPT ER XC V.— Dry GLA CTD Akin (Wit TTLESEY 22 os Seen ee teen e ees se ciate Sane cee oes elses Alia GT GTO yee eter eee re rie ale <<) pe EM npc OID eA SL aye eee WhesWiblyxOubleties see ee cea ms. af cece Oe eee meee ed eae gaye MR The Belmore beach from the Ubly outlet to the Maumee River ...-..--....-..---.--.---- TONSA AM OVUM) oe ere ee ie aie MOORE So Le a ee Eee en ne Descriptionxoiathewpeache -/..5..5e otis Soares eos aaajnen sees a Sem ee NET aut OM ne aT tLe eos hy, Se SS acy See eT aes MhetshonevomMetiamcey Bayne 5.0.92 = ope ae as, See nd ie a SAN a ae ihersouryshonreroimealkenw/ bith] ese y sf sea see eee aerate eat esis cee tence TD Yas reT OUOUETCO NTS = ose. Ee Ie alte A Sk 5 2 a or ee a Wamationstna.streagthy.2c <5 =e Se eeeeteeren ates nae ase ores c Sonne ec ceogue Ma ATOT Sum AULULU LLC C!s) oats ote eee er Rays Ft ah aS BAe OA es Cause formhedoweniney ofthe ake wearer ee” oe. 22 eh Ss Soh re ea (CHAPTER PNG ile = DH: GINA CLA: Z ANKchs WHAIRRIE Nae eee ce erate SO 4 le hy Ae ee Introductory Awe. 422 see wane seems ears Myer Le ee Ae See oes WeScnipioniolethewbea Ch es mae aap smarts eatery L252 SL Le ae ae he sg ea Pct CONTENTS. CHAPTER XVI. —THE GLACIAL ier Warren—Continued. The withdrawal from Lake Warren to Lake Ontario. .---.--. 1 Ue eeee . Lake Dana (Lake Lundy?) BE PREP bic inck ote aaa eee ci He pikakeroquoistes: meet recta ce ss cescte scene eneemeeics Slee eee Cuarter X VII.—Sorts-.- Sources of soil material Classes of soil -.......-------- ta Residuary soils SEA eosee Se St ESE REARS EASE as och Bo keosS Py Stomysclayasoil seer ies et ene eae ce te eet ie Gravelly or stony soils -- Sandy soils -.-.-..--------- aietbeeetel Silty soils... -- weds! eye) Peaty or organic SOU See Swicjains co eee ts ice eeewenteieeemome cpa ‘ RA Sat hONS: Page Prare I. Topographic map of area discussed. -.......2.------------- 2-02 e ees eee eee een nee -- 22 JUL, Gleeiall maja on amen Ghisonsseel. oo: 26-522 54s24ecqs ces Pensraqagesascbeoscobessasos- 50 III. Pleistocene map of the district between Niagara River and Rochester, N. Y....-.-- 68 IDV, Abas Cee, IN Wey WOO RIE MNS BINGE oo oas5c5 een eenonsnodoeecedeeeEeso seas In pocket. VY. Topographic map showing drainage/features near Cincinnati, Ohio.............._.-- 84 Vi. The Owensboro, Ky., topographic sheet ..........._.........-.-...-----.-.--- In pocket. VII. Topographic map showing drainage features near Ironton, Ohio .-.-...._........-.- 106 VIII. Map showing change of drainage near Franklin, Pa........-..-.......-..---.--.--- 136 IX. A, Middle Falls of Genesee River at Portage, N. Y.;.B, Genesee River Canyon below Middl esa sae tee Bis eeays ses sralele clooney s Sea ae amine sash aon feels Neco tee 202 Xx. Middle and Lower falls of Genesee River at Rochester, N. Y....................--- 204 XI. Map of the Maumee-Miami glacial lobe -.....-._.....-...--..-.-.--.-------.------ 304 XII. A, Section of till at Lane’s mill, near Darrtown, Ohio; B, Exposure of till some miles eastroimleanesmmilltsectionias. 24 ease eee ee cee seein naan es secs sel ame 330 XE Ma plo ine Sciotorslaciallel Ole ae ee see ee eee ese 8 atic yess eee 340 XIV. A, Section of peat and till near Germantown, Ohio; B, Section showing wood included TOMO elon eyouthy ot Oxtordsy) Ohio) sass a mee ene euler ee 364 Wo Miya Oia Carine iio elke Mole se 35 oo 5 sdeneeesas bad ssessesneer ose oe ee 436 XVI. A, Gravel pit at Fort Wayne, Ind.; B, Near view of part of same gravel pit......._-. 578 XVII. A, Glaciated surface on Middle Bass Island, in Lake Erie; B, Large glacial groove on Marblehead Peninsula, near Lakeside, Ohio ..-...-...............-.---.--------- 608 XVIII. Pleistocene map of part of the Girard and Erie, Pa., quadrangles .................-. 652 XIX. Pleistocene map of parts of the Dunkirk, Cherry Creek, and Silver Creek, N. Y., quiadmame] es reer ee rae rictc ot See Seat sR ee a ne eee ae st Vente EW MM LEM tN OY toe 654 XOX Mapronminst: make lMiaum cess /:/2 Mey Gee ee ey ae eee) a be oe 710 XXI. Map of Lake Maumee at its greatest expansion._..-.--.....-.---- POM eas 82 Sis Nee 714 XXII. Map of beaches near Sandusky, Ohio.....-..-.--.---- he ea NESE IN Sy apm eee eS tc 730 XOX Map olialke Wan ittleseryuls/< tosis Ue Ses Bie) Te) ebay ay a ae ee) sg 740 XXIV. Map of the Belmore Beach of Defiance Bay and Lake Whittlesey near Defiance, Ohio. 748 XXYV. Pleistocene features near eastern terminus of the Belmore beach southeast of Buffalo, INCE ES A eye ye Rea ree he ICL Gai I uae RE pe a he eM i Dae URC 754 NONGVilee iapon bakes Warmrene. “52 Sa ie sieeve DI RS Reay e ae S205 oA MEN ea RS 758 Fic. 1. Probable preglacial drainage of the Upper Ohio region....._.__......_.....-......--- 89 2. The Upper Ohio drainage near the supposed old divide ...._.............-....2------ 90 3. The Old Kanawha drainage in southern Ohio _.._..._.........2..2 2222222222222 eee 101 4, Relation between the present stream bed and the rock floor along the preglacial Upper ANIC NETO, TEAS ee en es Ae Ib Gye ciate A ey el MEN NER CC 130 5. Present drainage of part of the Middle Allegheny..................-...-.------------ 134 6. Probable preglacial drainage of part of the Middle Allegheny..............-.--------- 135 7. Profile along the Low Grade Division of the Allegheny Valley Railroad ..........-.--- 147 Sy Eby drographiy olithes Genesee: Valleya-ss-5--42-4-\-6- <2 -- ==. 22cs-s-- enced ae eee 201 LISS waOMY (O10 \/ OUI D CuapTer I. Inrropuction.-—The area treated in this monograph extends from the Genesee Valley in New York westward across northwestern Pennsylvania and Ohio to central and southern Indiana, and southward from Lakes Ontario and Krie to the vicinity of the Alleeheny and Ohio rivers. It includes the old drift of north- western Pennsylvania, the Illinoian drift of Ohio, Kentucky, and southeastern Indiana, and the Wisconsin drift of the Maumee-Miami, Scioto, and Grand River lobes, as well as the drift of western New York. It includes the portions of the glacial Lakes Maumee, Whittlesey, and Warren, which border the Lake Erie Basin on the south and west, and also their westward outlets. This chapter presents an outline of previous publications on the glacial geology of the region, and also outlines the geologic formations and the several sheets of drift there present. Cuarrer II. PHysicaL FHATURES.—The variations in altitude are great, rang- ing from about 250 feet up to nearly 2,500 feet above sea level in the drift-covered region south of Lake Ontario, and from below sea level if that basin be included. There are series of plains south of Lake Ontario separated by escarpments, and south of these is a greatly eroded table-land. Farther west are the Grand River and Scioto basins, bordered by eroded table-land, and still farther west is the low plain of the central Mississippi Basin, whose eastern border is found in western Ohio. Cuaprer III. Drarnacr systems.—This discussion includes not only a descrip- tion of the present systems of drainage, but also directs attention to important changes of drainage that have occurred and attempts to determine to some extent the causes of these changes. CuaptEer IV. THE DRIFT BORDER, OR GLACIAL BOUNDARY.—It is found that the glacial boundary is not a unit, but is formed in part by the border of the Wisconsin drift, in part by the Ilinoian drift, and in part by a sheet of drift that appears to be still older than the Illinoian. Cuaprer V. Tor OLDEST DRIFT (KANSAN oR PRE-Kansan?).—This drift, which is exposed outside the Wisconsin drift in northwestern Pennsylvania, is shown to 19 20 ABSTRACT OF VOLUME. have suffered a much greater amount of erosion and weathering than the Illinoian drift. Its characteristics are set forth, and the glacial drainage connected with it is discussed. Craprer VI. THe Inuroran prirr.—This embraces the portion of the Illinoian drift exposed outside the Wisconsin drift from the reentrant angle in the glacial boundary in southern Indiana eastward to central Ohio, where its border passes beneath the Wisconsin drift border. Its structure and topographic expression and the character of the glacial drainage are discussed. Cuarter VII. Tort SANGAMON SOIL AND WEATHERED ZONE.—The weathered zone and accompanying soils and peat beds which occur between the Illinoian drift and the overlying loess are described in their exposures outside the Wisconsin drift, and to some extent within the limits of that drift. Cuaprrer VIII. THE LOEss AND ASSOCIATED stLTs.—The Iowan drift does not appear to be exposed in this region outside the Wisconsin drift, but a deposit of silt of loess-like characteristics occupies the horizon of this drift sheet. It may be to some extent a dependency of the Iowan drift, for the loess in the vicinity of the Mississippi River is found to have that relation, as indicated in Monograph XX XVIII. The mode of deposition is, however, considered problematical. Cuarrer LX. THE PEORIAN OR POST-LOESSIAL SOIL AND WEATHERED ZONE.— The evidence of this interval between the loess deposition and the Wisconsin gla- ciation is found in the relative amounts of weathering displayed by the loess and the Wisconsin drift. It may also be inferred trom the change in the attitude of the land by which better drainage conditions became prevalent in the Wisconsin than obtained in the Jowan stage of glaciation. The marked difference in the outline of the Iowan and Wisconsin borders also indicates an interval of some consequence. CHapreR X. THE EARLY Wisconstn prirr.—The early Wisconsin drift is less extensively exposed in this region than in that covered by the Illinois glacial lobe, discussed in Monograph XX XVIII, there being in southwestern Ohio but one moraine and a narrow till plain which seem referable to this drift, while in central and eastern Ohio and northwestern Pennsylvania it has a still more limited exposure. In southeastern Indiana two moraines of the White River lobe and one of the Miami lobe seem referable to this drift. The present report embraces only the part of this drift extending from the Miami lobe eastward. It treats of both the drift and the outwash connected with it. Cuarrer XI. THE INTERVAL BETWEEN THE EARLY AND LATE WISCONSIN prirt.—The evidence of this interval is more clearly shown in the region covered by the Illinois glacial lobe than in this region, for there the border of the outer moraine of the late Wisconsin group is strikingly discordant with that of the neigh- boring moraine or moraines of the early Wisconsin group, while in this region there is not a marked discordance. There is, however, in this region, as well as in the Illinois region, a marked contrast in the topography of the moraines, those of the early Wisconsin having smooth ridges without lakes or deep basins on them, while ABSTRACT OF VOLUME. 21 the late Wisconsin moraines present a hummocky surface, deeply indented by basins, and in places carry lakes. The interval, if measured by contrasts in weathering, seems much shorter than the Peorian and Sangamon interglacial stages. CuaprerR XII. THE MAIN MORAINIC SYSTEM OF THE LATE WISCONSIN STAGE.— This morainic system was brought to notice by Chamberlin in the Third Annual Report of this Survey as the ‘‘Terminal moraine of the second Glacial epoch.” It is by far the strongest morainic system of the entire series. The morainic loops in the several lobes—Miami, Scioto, and Grand River—are taken up in the order named. The question of the equivalent system to the east of the reentrant angle of southwestern New York is left open. Till plains, eskers, and other features to the north of this morainic system are discussed, and also the outwash to the south so far as it is connected with the morainic system. CHarteR XIII. Minor MORAINES OF THE LATE WISCONSIN STAGE.—The several moraines lying between the main morainic system and the shores of Lake Erie and Lake Ontario are taken up in natural groups, and with them the eskers and other features of the drift. Those of the Maumee-Miami Basin form one group, and those of the Scioto Basin another, while later moraines lying within the Maumee Basin are next considered, and then those which closely border Lake Erie. The chapter closes with the moraines and associated drumlins and eskers south of Lake Ontario. Attention is incidentally called to glacial lakes in connection with the discussion of the border drainage. CuapTeR XIV. Tue cGiactaL Lake MAumrer.—This was the highest of the great glacial lakes which formed in front of the retreating ice sheet as it withdrew into the Huron and Erie basins. The chapter describes two beaches, and also other features of this glacial lake, together with the successive outlets past Fort Wayne, Indiana, and Imlay, Michigan. CHaprer XV. Tur GuaciaL Lake Wuirritesny.—This lake was a close successor to Lake Maumee, and stood only about 30 feet lower. The Belmore beach, which marks its shore, is described throughout its course from southeastern Michigan southward and eastward to its apparent terminus at Marilla, in western New York. The Ubly outlet, through which the lake discharged westward to the Saginaw Basin, and the Grand River outlet, which led from the Saginaw Basin to Lake Chicago, are briefly considered. As in the preceding chapter, the relation of the ice sheet to the extent of the lake forms an important subject. A marked warping of the eastern portion of the beach is also discussed and is shown to contrast strongly with the nearly perfect horizontality in Ohio and southeastern Michigan. CHaprterR XVI. Tue eiActaL Lake Warren.—Lake Warren as here defined was a successor of Lake Whittlesey in the Huron and Erie basins. Its borders are marked by a complex system of beaches standing 40 to 75 feet below the level of the Belmore beach, two of which are known as the Arkona and Forest beaches. Lake Warren also extended into the Saginaw Basin and discharged across Michigan through 22 ABSTRACT OF VOLUME. the Grand River outlet to Lake Chicago in the Lake Michigan Basin. The discussion is restricted to the part of the beaches which border the west and south sides of the Erie Basin. Attention is called to the marked warping displayed by the beaches in the eastern part of the Erie Basin, and the contrast with the nearly horizontal attitude to the west. In this chapter the lowering of the lake from Lake Warren to Lake Iroquois is briefly considered, and the probable relations of the lake to the ice sheet are set forth. Cuaprer XVII. Sorms.—The soils are classified according to their origin, the following classes being recognized: Residuary soils, bowlder-clay soils, gravelly soils, sandy soils, loamy soils grading into fine silts, peaty or organic soils. MICHIGAN | MASON OCEANA MUSKEGON MONTCALM 17 SAGINAW aa RON TOwSIOeLUN =| co ie 5 2 C] 22 GENESEE 23 SHIAWASSEE 23 CLINTON WAYNE 36 WASHTENAW 37 JACKSON. 38 CALHOUN 39 KALAMAZOO 40 VAN BUREN 41 BERRIEN 42 CASS 43 ST.JOSEPH f 2 Ed FA a 2 1 LAPORTE 3 ELKHART WELLS: HUNTINGTON WABASH MIAMI CASS CARROLL HOWARD GRANT BLACKFORD JAY RANDOLPH a5 UR 45 BARTHOLOMEW 47 BROWN 48 JACKSON 49 JENNINGS 50 RIPLEY 5] DEARBORN 52 SWITZERLAND 53 JEFFERSON 54 SCOTT 55 WASHINGTON 56 CLARK 57, FLOYD 58 HARRISON OHIO 1 WILLIAMS 6 ASHTABULA 7 TRUMBULL. 6 GEAUGA 9 CUYAHOGA 10 LORAIN 1) ERIE 12 SANDUSKY 13 Woop: 22 SUMMIT 23 PORTAGE 24 MAHONING 25 COLUMBIANA 26 STARK 27 WAYNE 34 MERCER 35 AUGLAIZE 36 HARDIN 37 MARION 38 MORROW 39 KNOX 40 HOLMES 41 COSHOCTON 45 JEFFERSON 46 BELMONT 47 GUERNSEY. $8 MUSKINGUM 49 LICKING 50 DELAWARE 5) UNION 52 LOGAN 53 SHELBY 34 DARKE 55 MIAMI 55 CHAMPAIGN 57 CLARK EB MADISON 59 FRANKLIN 60 PICKAWAY 61 FAIRFIELO 64 NOBLE 65 MONROE 6 WASHINGTON 67 ATHENS 68 HOCKING 59 VINTON 74 PREBLE 75 BUTLER 75 WARREN 77 CLINTON 78 HIGHLAND. 73 PIKE BO JACKSON Bt MEIGS 2 GALLIA 83 LAWRENCE 84 SCIOTO BS ADAMS 86 BROWN 87 CLERMONT 88 HAMILTON BRACKEN. RENDLETON GRANT GALLATIN GR =o ecsousun— a OWEN 16 HARRISON ig seaamiee™ ig et BoYo 21 LAWRENCE ScoTTr 28 FRANKLIN SHELBY 30 JEFFERSON BULLITT CLARK MONTGOMERY NEW YORK JEFFERSON Lewis & PGK Sworn aun Si 17 ONONDAGA 18 MADISON 19 CHENANGO. 27 ALLEGANY 28 CATTARAUGUS 29 CHAUTAUQUA PENNSYLVANIA a 8 6 7 SUSQUEHANNA 8 WYOMING 8 SULLIVAN (0 LYCOMING 1 CLINTON 2 CAMERON ELK FOREST VENANGO. CRAWFORD 1ON 25 NORTHUMBERLAND |” MONTOUR: COLUMBIA 33 ALLEGHENY 34 WESTMORELAND 35 SOMERSET 36 FAYETTE 37 WASHINGTON 36 GREENE MONONGALIA MARION PRESTON TAYLOR 10 HARRISON 11 DODDAIDGE TYLER: 13 RITCHIE 14 PLEASANTS. WOOD t 2 3 4 S WETZEL, 7 c 9 32 NICHOLAS 93 WEBSTER 34 POCAHONTAS 35 GREENBRIER 36 FAYETTE 37 BOONE 3@ UNCOLN 39 WAYNE U.S. GEOLOGICAL SURVEY 3 ve 35), oVersailte: at s \ 84° MONOGRAPH XLI PL. | Ce AUN Se Eater i ZB ZU Ea TOPOGRAPHIC MAP OF OHIO AND PARTS OF MICHIGAN, INDIANA, KENTUCKY, WEST VIRGINIA, PENNSYLVANIA.AND NEW YORK Compiled by Frank Leverett 1901 Seale 10 20 4O 40 50 190 Miles = —— = —= - 100 10 20 30 40 50 100 Kilometers et = Contour interval 500 feet Datumis mean sea level aay ran ae 81° JULIUS BIEN SCO.LITH NY. ee ee ee ee ae ee ge ee Se a : - 4 ct hoy A ree a ae) _s ‘ iW MONOGRAPH XL PL. 1 = z - 2 i i+ = & Hy 2 Beet eaar ise HI ® 3 eft a SESE SLES BEVEEN OSS SS Sas FES Sect eee - = 3 ? 3 : : _ Ss ; = = SEs ms $82 E 3 £ a F a a = = na < = = > = OG FOF ve ie $3 = g egatetesgeesseeeesranesnsssss a = oreige z ay SEs, ene SEES *epee as scarSes. He ee a a ei %3 | Cerin e tom) LMG : he : AW Gin pe OOM) , ? r = 3 a - en G | | eS 7 es GO verre H f VA Ky? 9 ° d ! x omersail Si a ey | 35 | 24 4 eae \ PM, nd TOPOGRAPHIC MAP OHIO AND PARTS OF MICHIGAN, I INDIANA, KENTUCKY,WEST VIRGINIA, PENNSYLVANIA.AND NEW YORK Compiled by Frank Leverett bar! . ' a tye" Iso] foo Miles = woo Kilometers Tas cA, 1 7 A Contour interval 500 feet = aS - —— = Datum is thean sea tevel eFleningstm: fc 7 \ at 7 ‘Nee UTES : i Ys bY ne JUUUS BIEN BOO ITH OY GLACIAL FORMATIONS AND DRAINAGE FEATURES OF THE ERIE AND OHIO BASINS. By Frank LEVERETT. G Jel ek Je aah des I INTRODUCTION. OUTLINE OF THE AREA AND SUBJECTS DISCUSSED. The region embraced in this discussion has for its northern boundary the south line of Michigan and the southern borders of Lakes Erie and Ontario: for its eastern boundary the Genesee River; for its southeastern and southern boundary the Allegheny and Ohio rivers, except in northern Kentucky, where the southern limits of the drift extend beyond the Ohio River; and for its western boundary the driftless part of southern Indiana. There is included at the east a system of interlobate moraines lying between the lobe of the Finger Lakes region in New York and the Grand River lobe of northeastern Ohio and the neighboring parts of Pennsylvania and New York, but no discussion of the moraines of the Finger Lakes region is attempted. he deposits and features of the region covered by three glacial lobes of Wisconsin age are described—the Grand River, the Scioto, and the Miami—with the interlobate tracts between, and the valley gravels leading away from these lobes. The older drift lying outside and also beneath the Wisconsin deposits, and the silt deposits which cover this older drift, are also described. In addition to this an attempt is made to interpret some of the drainage features of the region. There is also a discussion of a part of the lake history succeeding the withdrawal of the ice sheet. 23 24 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. This report, like that on the Illinois glacial lobe (Monograph XX XVIII), presents the results of an investigation carried on for several years under the direction of Prof. T. C. Chamberlin, who preceded the writer in a reconnaissance of the region, and has published a preliminary report.' To these earlier results, as well as to Chamberlin’s direction and suggestions, the writer is greatly indebted. Indebtedness is also acknowledged to many others who were earlier on the ground, and to many who throughout the investigation have aided by contribution of material and by suggestions concerning the interpretations of the phenomena. OUTLINE OF PREVIOUS PUBLICATIONS. It is impracticable to give a full review of the many papers which deal with the surface geology of the region. About 500 of these papers have been examined and an endeavor has been made to duly accredit those which have materially advanced the interpretations. In addition to this a list of all the papers which have come to the writer’s notice is presented. Upon turning to this list the reader will find that Niagara River and its falls and gorge have furnished themes for not fewer than thirty geolo- gists and travelers from the time these striking natural features were first brought to the attention of civilized man in 1535. The gigantic mammals which once roamed this region, but which are now extinct, furnished a theme for animated discussion at the early meet- ings of scientific associations in America. The discovery of their bones at Big Bone Lick in Kentucky in 1744 was followed by numerous other discoveries in all parts of the region here described, as well as in other parts of North America. This subject has received less notice in recent years than in the first half of the last century, and the present report has nothing new to offer. The glacial drift of the region appears to have attracted notice from the earliest days of settlement. This is especially true of Ohio, as shown by the papers of Drake in 1817, of Atwater from 1818 to 1826, of Granger in 1823, of Hildreth from 1827 to 1837, of Darius and Increase Lapham in 1832, of Riddell in 1837, and by the Geological Reports for 1838 1Preliminary paper on the terminal moraine of the second Glacial epoch, by T. C. Chamberlin: Third Ann. Rept. U. S. Geol. Survey, 1883, pp. 330-352. « OUTLINE OF PREVIOUS PUBLICATIONS. 25 prepared by Mather, Whittlesey, Locke, Foster, and Briggs. Hall and Horsford had given it attention in southwestern New York in 1838 and 1839. As early as 1838 it had become established that the drift extends to the Ohio River in southwestern Ohio, and to the ‘hill country” of southeastern Ohio. It was also known equally early that it extends to the hilly districts of southern Indiana and southern Illinois. At that date its limits in northwestern Pennsylvania were perhaps less definitely known. Strize were reported at Sandusky, Ohio, by Granger in 1823; near Lock- port and Brockport, N. Y., by Thomas in 1830; near Buffalo, N. Y., by Hayes in 1837; at Rochester, N. Y., by Dewey in the same year; and near Dayton, Ohio, by Locke in the succeeding year. In explanation of the drift and of the strize, it seems to have been gen- erally recognized as early as 1839 that currents from the north were the agency of transportation, and that these currents carried large masses of ice which were laden with rock material. It was early recognized that i “ co strize could not be the result of ordinary currents of water. In reference to the striation at Sandusky, Granger remarked in 1823: ’ The surface is polished as if by friction. It has the appearance of having been formed by the powerful and continued attrition of some hard body. The flutings in depth, width, and direction are as regular as if they had been cut out by some groov- ing plane. This running water could not effect, nor could its operation have produced, that glossy smoothness which in many parts it still retains.’ Locke remarked in 1838, concerning striz near Dayton, Ohio: It is impossible to account for the phenomena by supposing them to be the effect of alluvial action. The motion occasioned by a river may wear a surface in general smooth, but not to any extent to a perfect plane. It may roll stones or slide them along, but seldom, if ever, so as to engrave lines so perfectly straight and parallel. I deem it proper here to observe that I did not come to the conclusion that the above- described grooves were ancient or *‘diluvial grooves” without caution and particular examination.” Dewey remarked, in 1839, concerning strize in western New York, that they apparently support the glacial theory of Agassiz. He thought, how- ever, that great masses of floating ice might produce the phenomena, and that floods were required to account for the transportation of bowlders across high ridges.’ 1 Am.Vour. Sci., lst series, Vol. VI, 1823, pp. 179-180. *Second Ann. Rept. Geol. Survey Ohio, 1838, pp. 231-282. * Am. Jour. Sci., Ist series, Vol. XX XVII, 1839, pp. 240-242; idem, Ist series, Vol. XLIV, 1843, pp- 146-150. 26 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. By many of the early students the surface bowlders were thought to be a distinct deposit from the sheet of drift which they cover, but some of the earliest writers found them to be a part of that sheet. Thus, Darius and I. A. Lapham noted, in 1832, the occurrence of bowlders in the blue and yellow clays of the “‘diluvium” near Circleville, Ohio. They remarked also that the rounding of the bowlders is independent of modern stream action.’ The effect of the drift on the northern tributaries of the Ohio was early recognized by Drake, who, in 1817, called attention to the fact that the drift terraces are found on northern but not on southern tributaries, and that the northern tributaries have been so filled by the drift that their descent to the Ohio is much more rapid than that of southern tributaries. Drake also discussed, quite clearly for so early a date, the extent of the erratics in the Mississippi Basin, his discussion being based upon his own observations, coupled with those of his friends, Nuttall, Goforth, and Warren. The agent of transportation is thought by him to have been icebergs.” Among other early papers worthy of special mention is one by J. 'T. Plummer, of Richmond, Ind., which contains a lucid description of Sstrize and drift in the vicinity of that city.’ Several papers by Whittlesey are full of important data, among which may be mentioned Notes on the Dritt of Ohio and the West,* Fresh Water Glacial Drift of the Northwestern States,’ and Ice Movements in the St. Lawrence Valley. Alfred T. King presented a brief but discriminating discussion of the Ancient Alluvium of the Ohio and Tributaries in an early volume of the Philadelphia Academy of Sciences.’ O. N. Stoddard early called attention to a bowlder pave- ment in Ohio and urged it as evidence of glacial action.® EK. B. Andrews discussed the relation of the river terraces of southern Ohio to drift theories, and held that they were glacial dependencies, rather _1Am. Jour. Sci., 1st series, Vol. XXII, 1832, pp. 300-303. * Paper read before the American Philnsophical Society in 1818; published in Trans. Am. Philos. Soe., new series, Vol. II, 1825, pp. 124-139. ’Am. Jour. Sci., Ist series, Vol. XLIV, 1843, pp. 281-315. ‘Idem, 2d series, Vol. V, 1843, pp. 205-217. 5 Smithsonian Contrib., Vol. XV., 1867, 32 pages. ®Proc. Am. Assoc. Adv. Sci., Vol. XV, 1867, pp. 43-54. ™Proec. Phila. Acad. Sci., Vol. VII, 1856, pp. 4-8. 8Am. Jour. Sci., 2d series, Vol. XX VIII., 1859, pp. 227-228. OUTLINE OF PREVIOUS PUBLICATIONS. Di than marine or lacustrine.’ He called attention also to the fact that the termination of the drift is on a southward-sloping country and that its dis- tribution is consistent only with the glacial hypothesis. The drift and drainage features were given only incidental notice in ~ the first geological surveys of Ohio and Pennsylvania, and but limited attention by the New York survey. The second geological survey of Ohio, organized in 1869 under Newberry, has given, in the reports for each county, a brief discussion of these features. In addition to this, New- berry presented, in Volume II of the Geology of Ohio, a special discussion of surface geology, covering about 80 pages, in which the principal facts scattered through Volumes I and II are brought together and interpreted. The data collected by that survey are discussed in some detail in the body of this report in connection with those collected subsequently by the writer and others. The second geological survey of Pennsylvania, under the direction of Lesley, collected in the decade beginning in 1875 many facts bearing on the drift and drainage features of northwestern Pennsylvania. These appear in connection with the study of the underlying rock formations in Reports I’, I’, and I’, prepared by Carll; in K, KK, and KKK, by Stevenson; in Q, QQ, Q’, and Q*, by White; and in VV, by Chance. In addition to these, a special study of the glacial. boundary in Pennsylvania and southwestern New York was made in 1882 by Lewis, with the assist- ance of G. F. Wright, which forms Report Z of the Pennsylvania survey. The data thus collected are more carefully noted in the body of this report. The mapping of the glacial boundary was continued by Wright across Ohio and northern Kentucky under the auspices of the Western Reserve Historical Society of Cleveland, Ohio, and across Indiana and Illinois under the present Survey. The results of the former study appeared in a bulletin of the society, while the main results of the entire study are presented in Bulletin 58 of this Survey. Wright has also incorporated this material in his Ice Age in North America, while special topics connected with these and other studies have been discussed by him in various scientific journals. The mapping by Wright is found to apply in northwestern Pennsylvania and eastern and central Ohio chiefly to the border of the Wisconsin drift, but in southwestern Ohio and districts farther west it indicates the approximate 1Proc. Am. Assoc. Ady. Sci., Vol. XIII, 1860, pp. 319-321. 28 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. border of the older drift. In portions of central Ohio and northwestern Pennsylvania the older drift extends several miles beyond the limits of the Wisconsin, and thus invalidates the use of the term glacial boundary for portions of the line traced by Lewis and Wright, since it was not on the boundary. The name terminal moraine, however, is more pertinent to “hs portion, since it is the Wisconsin terminal moraine. Within the portion of Indiana under discussion much attention has been given by the Indiana geological survey to the drift of the northeastern counties, which are reported upon by Dryer, and to a few counties in the eastern and southeastern portions, reported upon by Phinney, McCaslin, Elrod, Warder, and Borden. The reports of Dryer and Phinney have given due attention to moraines and other drift forms, and are notably in harmony with present methods of classification. Each of the other reports also contains valuable data. The preliminary report by Chamberlin, referred to above, deals chiefly with a strong morainic system which he traced from Wisconsin southeast- ward into Indiana and thence eastward into New York, and found to be dis- posed in loops around the western and southern ends of the great basins of the region. Jn this and subsequent papers Chamberlin has sought to dis- criminate between drift sheets of different ages and to determine the several stages of the Glacial epoch. Aside from the reports and papers already mentioned there are several papers by Chamberlin, Claypole, Dryer, Fairchild, Foshay, Hice, Spencer, Taylor, Tight, Upham, White, Wright, and others, which throw light on the glacial history of this region, as shown in the course of the discussion. For titles and places of publication of these and other papers bearing upon the region the subjoined list may be consulted: BIBLIOGRAPHY. (Brought down to the close of the year 1899.) Anprews, E. B. Relation of the river terraces of southern Ohio to the drift and drift theories: Proc. Am. Assoc. Ady. Sci., Vol. XIII, 1860, pp. 319-321. General features and drift of the second district: Rept. Geol. Survey Ohio, 1869, pp. 57-64. Bowlders and surface drift of the second district: Rept. Geol. Survey Ohio, 1870, pp. 57-58. On a peat bed under drift in Ohio: Am. Naturalist, Vol. V, 1871, p. 522. BIBLIOGRAPHY. 29 AnprEws, E. B. Surface geology of southeastern Ohio: Geology of Ohio, Vol. I, 1874, pp. 441-452. ASHBURNER, CHaRLES A. The geology of McKean County, Pennsylvania: Second Geol. Survey Pennsylvania, Report R, 1880. ATWATER, CaLEB. On the prairies and barrens of the West: Am. Jour. Sci., Ist series, Vol. I, 1818, pp. 116-125. Ancient human bones, bones of the mastodon and mammoth, and various shells found in Ohio and the West: Am. Jour. Sci., Ist series, Vol. II, 1820, pp. 249-246, Climate, diseases, geology, and organized remains of part of the State of — Ohio: Am. Jour. Sei., Ist series, Vol. XI, 1826, pp. 224-231. BakEWELL, R. Origin of the whirlpool and rapids below the Falls of Niagara: Am. Jour. Sci., 2d series, Vol. IV, 1847, pp. 25-36. Observations on the Falls of Niagara, with reference to the changes which have taken place and now are in’ progress: Am. Jour. Sci., 2d series, Vol. XXII, 1857, pp. 95-96. Batiou, W. H. Niagara River: Sci. Am. Supp., Vol. XIII, 1882, pp. 5045-5046. Bennert, L. F. The eastern escarpment of the knobstone formation: Proc. Indiana Acad. Sci., 1898, pp. 283-288. BisHor, Irvine P. Geology of Erie County, New York: Fifteenth Ann. Rept. New York Geol. Survey, Vol. I, 1897, pp. 17-18, 305-392. Borpen, W. W. General features and drift of Scott County and Jefferson County, Indiana: Sixth Ann. Rept. Geol. Survey Indiana, 1874, pp. 112-118, 135-145. Quaternary beds and surface features of Jennings and Ripley counties, Indiana: Seventh Ann. Rept. Geol. Survey Indiana, 1875, pp. 146-147, 171- 178, 181-182, 195-196. Bownocksr, J. A. A deep preglacial channel in western Ohio and eastern Indiana: Am. Geologist, Vol. XXIII, 1899, pp. 178-182. Briees, C. Fossil bones; mammoth, or fossil elephant: Rept. Geol. Survey Ohio, 1838, pp. 96-97. Superficial material of Wood and Crawford counties, Ohio: Rept. Geol. Survey Ohio, 1838, pp. 114-118, 122-129. Brown, R. T. General sketch of Indiana geology: Third Rept. Indiana Board Agr., 1853, pp. 299-322. Geological and topographical survey of Marion County, Indiana: Twelfth Ann. Rept. Geol. Survey Indiana, 1882, pp. 79-99. Geological and topographical survey of Hamilton and Madison counties, Indiana: Fourteenth Ann. Rept. Geol. Survey Indiana, 1884, pp. 20-40. Survey of Hancock County, Indiana: Fifteenth Ann. Rept. Geol. Survey Indiana, 1886, pp. 187-197. Bryson, Joun. The terminal moraine near Louisville, Kentucky: Am. Geologist, Vol. IV, 1889, pp. 125-126. Preglacial channels at the falls of the Ohio: Am. Geologist, Vol. V, 1890, pp. 186-188. Burke, M. D. Drift near Cincinnati as a source of water supply: Jour. Cincinnati Soe. Nat. Hist., Vol. II, 1888, pp. 69-75. 30 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Cart, J. F. Report of progress in the Venango district: Second Geol. Survey Pennsylvania, Rept. I, 1875, p. 47. A discussion of the preglacial and postglacial drainage in northwestern Pennsylvania and southwestern New York: Second Geol. Survey Pennsylvania, Rept. ILI, 1880, pp. 1-10, 330-397. Geology of Warren County, Pennsylvania: Second Geol. Survey Pennsyl- vania, Rept. I*, 1883. CHAMBERLIN, T. C. La moraine terminal du Amérique du nord: Proc. Internat. Congr. Geol., Paris, August, 1878. Extent and significance of the Kettle moraine: Trans. Wisconsin Acad. Sci., Vol. IV, 1878, pp. 201-234, map. Bearings of some recent determinations on the correlation of the eastern and western terminal moraines: Am. Jour, Sci., 3d series, Vol. XXIV, 1882, pp. 93-97. Preliminary report on the terminal moraine of the second Glacial epoch: Third Ann. Rept. U. 5. Geol. Survey, 1883, pp. 291-402. Hillocks of angular gravel and disturbed stratification: Am. Jour. Sci., 3d series, Vol. XX VII, 1884, pp. 378-390. An inventory of our glacial drift: Proc. Am. Assoc. Adv. Sci., Vol. XX XV, 1886, pp. 195-211. The rock-scorings of the great ice invasions: Seventh Ann. Rept. U.S. Geol. Survey, 1888, pp. 174-248. Bowlder belts and bowlder trains: Bull. Geol. Soc. America, Vol. I, 1890. pp. 27-31. The glacial boundary in western Pennsylvania, Ohio, Kentucky, and Illinois: Bull. U. S. Geol. Survey No. 58, 1890, pp. 13-38. Attitude of the eastern and central portions of the United States during the Glacial period: Am. Geologist, Vol. VIII, 1891, pp. 267-275. Nature of the englacial drift in the Mississippi Basin: Jour. Geol., Vol. 1, 1893, pp. 47-60. Horizon of drumlin, osar, and kame accumulations: Jour. Geol., Vol. I, 1893, pp. 255-267. The diversity of the Glacial period: Am. Jour. Sci., 3d series, Vol. XLV, 1893, pp. 171-200. Further studies in the upper Ohio region: Am. Jour. Sci., 3d series, Vol. XLVII, 1894, pp. 247-283, 483. Proposed genetic classification of glacial deposits: Jour. Geol., Vol. II, 1894, pp. 517-538. The glacial phenomena of North America: Geikie’s Ice Age, 3d edition, pp: 724-775. London and New York, 1894. i Classification of American glacial deposits: Jour. Geol., Vol. III, 1895, pp. 270-277. Age of the second terrace on the Ohio, near Steubenville: Jour. Geol., Vol. IV, 1896, p. 219. —— Classification of the glacial deposits: Jour. Geol., Vol. IV, 1896, pp. 874-878. BIBLIOGRAPHY. 31 CHAMBERLIN, IT. C. Several papers by Chamberlin on the glacial phenomena of Greenland, published in the Journal of Geology, throw light on the method of deposition of the glacial deposits of the region embraced in this report. Cuance, H. M. Survey along the Beaver and Shenango rivers: Second Geol. Survey Pennsylvania, Report of Progress, Vol. XVII, 1879. The geology of Clarion County, Pennsylvania: Second Geol. Survey Penn- sylvania, Report VV, i880, pp. 1x—x, 17-22. Curisty, Davrp. Letters on geology and an essay on the erratic rocks of North America. Oxford, 1848. CrarkE, JoHN M. Sink holes at Attica, New York: Sixth Ann. Rept. New York Geol. Survey, 1886, pp. 34-35. Bones of Mastodon, or Elephas, found associated with charcoal and pottery at Attica, New York: Forty-first Rept. New York State Museum Nat. Hist., 1888, pp. 388-390. CriaypoLe, E. W. Preglacial topography of the Great Lakes: Canadian Naturalist, Vol. VIII, 1878, pp. 187-206. Origin of the basins of Lake Erie and Lake Ontario: Proc. Am. Assoc. Ady. Sci., Vol. XXX, 1881, pp. 147-159. Also Canadian Naturalist, new series, Vol. LX, 1881, pp. 213-227. Buffalo and Chicago, or ** What might have been:” Am. Naturalist, Vol. XX, 1886, pp. 856-862. The old gorge at Niagara: Science, Vol. VIII, 1886, p. 236. The lake age in Ohio: Trans. Edinburgh Geol. Soc., Vol. V, 1887, pp. 421-458. Falls of rock at Niagara: Nature, Vol. XX XIX, 1889, p. 367. Megalonyx in Holmes County, Ohio: Am. Geologist, Vol. VII, 1891, pp. 149-153. Deep preglacial river bed near Akren, Ohio: Proc. Am. Assoc. Ady. Sci., Vol. XL, 1891, p. 259. Deep boring near Akron, Ohio: Am. Geologist, Vol. VIII, 1891, p. 239. Human relics in the drift of Ohio: Am. Geologist, Vol. XVIII, 1896, pp. 302-314. Cotter?, Joun. Geology of Brown County, Indiana: Sixth Ann. Rept.’ Geol. Survey Indiana, 1874, pp. 77-110. Geology of Harrison and Crawford counties, Indiana: Tenth Ann. Rept. Geol. Survey Indiana, 1878, pp. 292-302, 426-429. Geology of Shelby County, Indiana: Eleventh Ann. Rept. Geol. Survey Indiana, 1881, pp. 55-88. Cox, E. T. Geology of Jackson County, Indiana: Sixth Ann. Rept. Geol. Survey Indiana, 1874, pp. 41-42, 55-60. General discussion of glacial drift in Indiana: Tenth Ann. Rept. Geol. Survey Indiana, 1878, pp. 98-120. Geology of Wayne County, Indiana: Tenth Ann. Rept. Geol. Survey Indiana, pp. 171-232. CuLgpertson, GLENN. Reference marks for estimating the rate of recession of falls near Madison, Indiana: Proc. Indiana Acad. Sci., 1897, p. 242-248. 32 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Darpy, Witttam. The emigrants’ guide to the Western and Southwestern States and Territories (geographical and statistical). New York, 1818. Davis, H. J. Modification of the Jonathan Creek drainage basin: Bull. Denison Univ., Vol. XI, pp. 155-173, March, 1899. Dr Geer, GerARD. Pleistocene changes of level in eastern North America: Am. Geologist, Vol. XI, 1893, pp. 22-44; also Proc. Boston Soc. Nat. Hist., Vol. XXYV, pp. 454-477. Isobases of the postglacial elevation: Am. Geologist, Vol IX, 1892, pp. DA7-249, Drsor, E. On marine shells in Lake Ontario basin up to 310 feet: Bull. Soe. géol. France, 2d series, Vol. VIII, 1851, pp. 420-423. Note on terraces of Lake Erie: Proc. Boston Soc. Nat. Hist., Vol. II, 1851, pp. 291-292. On the ridge road from Rochester to Lewiston: Proc. Boston Soc. Nat. Hist., Vol. Il], 1851, pp. 358-359. Ueber Niagara Falls: Zeitschr. Deutsch. geol. Gesell., Vol. V, 1853, pp. 643— 644. Dewey, Cuester. Bones of the Mammoth in Rochester, New York: Am. Jour. ‘Sci., Ist series, Vol. XX XIII, 1838, p. 201. On the polished limestone of Rochester: Am. Jour. Sci., Ist series, Vol. XXXVII, 1839, pp. 240-949; also Trans. Assoc. Am. Geol. and Nat., 1843, pp. 264-266. Striz and furrows of the polished rocks of western New York: Am. Jour. Sci., Ist series, Vol XLIV, 1843, pp. 146-150. Drakes, Danie. Geological account of the valley of the Ohio: Trans. Am. Philos. Soe., new series, Vol. II, 1825, pp. 124-139. Dryer, C. R. Geology of Allen County; Indiana: Sixteenth Ann. Rept. Geol. Sur- vey Indiana, 1888, pp. 105-130. Geology of Dekalb County, Indiana: Sixteenth Ann. Rept. Geol. Survey Indiana, pp. 98-104. The glacial geology of the Irondequoit region. Am. Geologist, Vol. V, 1890, pp. 202-207. Geology of Steuben County, Indiana: Seventeenth Ann. Rept. Geol. Sur- vey Indiana, 1891, pp. 114-134. Geology of Whitley County, Indiana: sp eioncelanin Ann. Rept. Geol. Sur- vey Indiana, pp. 160-170. Geology of Noble SUN Indiana: Kighteenth Mane Rept. Geol. Pency Indiana, 1893, pp. 17-32 Indiana, 1893, pp. 72-82. The drift of the Wabash-Erie region: HKighteenth Ann. Rept. Geol. Survey ‘Indiana, 1893, pp. 82-90. The general geography of Indiana: Studies in Indiana geography, pp. 17-29. Terre Haute, 1897. This paper and the next two papers by Dryer first appeared in vols. 2-4 of the Inland Educator, 1896-97. Geology of eee County, Indiana: Eighteenth Ann. Rept. Geol. See ey , BIBLIOGRAPHY. 33 Dryer, C. R. The Erie-Wabash region: Studies in Indiana geography, pp. 43-52 The morainic lakes of Indiana: Studies in Indiana geography, pp. 53-60. The meanders of the Museatatuck at Vernon, Indiana: Proc. Indiana Acad. Sci., 1898, pp. 270-274. Dun, Water A. Sketch of the floods on the Ohio River: Jour. Cincinnati Soe. Nat. Hist., Vol. VII, 1884, pp. 104-124. Eaton, Amos. A geological and agricultural survey of the district adjoining the Krie Canal. Albany, 1824, 126 pages. Epson, Opep. The Glacial period in the Chautauqua Lake region. 1892, 13 pages. Private publication (7). Epmunps, E. $. Geology of Lagrange County, Indiana: Kansas City Review Vol., II, 1879, pp. 500-508; Vol. III, 1880, pp. 28-383 Farrcuitp, H. L. Geological history of Renee New York: Proc. Rochester Acad. Scei., Vol. IL, 1894, pp. 215-228. ; The kame moraine at Rochester, New York: Am. Geologist, Vol. XVI, 1895, pp. 39-51. Glacial lakes of western New York: Bull. Geol. Soc. America, Vol. VI, 1895, pp- 858-37 4. Lake Newberry, the probable successor of Lake Warren: Bull. Geol. Soc. America, Vol. VI, pp. 462-466. Glacial Genesee lakes: Bull. Geol. Soe. Auten, Vol. VII, 1896, pp. 423-452. Kame areas in western New York: Jour. Geol., Vol. IV, 1896, pp. 129-159. Lake Warren shore lines in western New York: Jour. Geol., Vol. V, 1897, pp. 269-282. Glacial geology of western New York: Geol. Mag., new series, Decade 4, Vol. IV, 1897, pp. 529-537. Glacial geology in America: Proc. Am. Assoc. Ady. Sci., Vol. XLVI, 1898, pp. 261-290. . Basins in glacial lake deltas: Jour. Geol., Vol. VI, 1898, pp- 589-592. Glacial waters in the ‘*‘ Finger Lakes” region: Bull. Geol. Soc. America, Vol. X, 1899, pp. 27-68. Glacial lakes Newberry, Warren, and Dana, in central New York: Am. - Jour. Sci., 4th series, Vol. VI, 1899, pp. 249-263. Fareo, J. G. Bowlder near Bete New York: Am. Jour. Sci., 3d series, Vol. X, 1875, pp. 479-480. FEATHERSTONHAUGH, G. W. On the ancient drainage of North America, and the origin of the cataract of Niagara: Am. Jour. Geol. and Nat. Sei., Vol. I, 1831, pp. 13-21. On the excavation of the rocky channels of rivers by the recession of their cataracts: Rept. Fourteenth Meeting British Assoc.- Ady. Sci., Pt. II, 1845, pp. 45-46. Fincu, Joun. Age of basins of Lake Erie and St.. Lawrence River: Am. Jour. Sci., ist series, Vol. XX VII, 1835, p. 151. Foor, Lyman. Notices of geology and mineralogy of Niagara Falls region: Am. Jour. Sci., Ist series, Vol. IV, 1822, pp. 35-37. a MON XLI———3 34 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Fosnay, P. Max. Preglacial drainage and recent. geological history of western Pennsylvania: Am. Jour. Sei., 3d series, Vol. XL, 1890, pp. 397-403. Newly discovered glacial phenomena in Beaver Valley: Am. Naturalist, Vol. XXIV, 1890, pp. 816-818. Glacial grooves at the southern margin of the drift: Bull. Geol. Soe. America, Vol. Il, 1890, pp. 457-464. Fosrrr, J. W. Revou on Muskingum and parts of Licking and Franklin counties, Ohio: Rept. Geol. Survey Ohio, 1838, pp. 73-83. Mastodon giganteum from Crawford County, Ohio: Am. Jour. Sci., 1st. - series, Vol. XXXVI, 1839, pp. 189-191. ; On the occurrence of “Mastodon remains in Ohio: Proc. Boston Soc. Nat. Hist., Vol. TU, 1851, pp. 111-116. On the geological position of the deposits in which occur the remains of the fossil elephant of North America: Proc. Am. Assoc. Ady. Sci., Vol. X, 1857, pt. 2, pp. 148-169. The Mississippi Valley, its physical geography, etc. Chicago and London, 1869, 445 pages. Fowks, Gurarp. Preglacial and recent ae channels in Ross County, Ohio: Bull. Denison Uniy., Vol. TX, 1895, pp. 15-2 Preglacial chotaeee | in ie vicinity ot ae Bull. Denison Uniy., Vol. XI, 1898, pp. 1-10. : Gipspes, L. R. Remarks on Niagara Falls: Proe. Am. Assoc. Ady. Sci., Vol. X, 1857, pt. 2, pp. 69-78. The past and present conditions of Niagara Falls: Proc. Elliott (S. C.) Soe. Nat. Hist., Vol. 1, 1859, pp. 91-100. Gipson, JoHN. Geology of the Lakes and the valley of the Mississippi: Am. Jour. Sci., Ist series, Vol. X XIX, 1836, pp. 201-213. Ginprrt, G. K. Surface geology of the Maumee Valley: Am. Jour. Sci., 3d series, Vol. I, 1871, pp. 339-345. Gadlonr of Williams, Fulton, and Lucas counties, Ohio: Rept. Geol. Sener Ohio, 1870, pp. 485-499. Surface geology of the Maumee Valley: Geology of Ohio, Vol. I, 1873, pp: 537-556. Geology of Williams, Fulton, and Lucas counties and West Sister Island: Geology of Ohio, Vol. I, 1873, pp. 557-590. Topographic features of lake shores: Fifth Ann. Rept. U.S. Geol. Survey, 1885, pp. 69-123. Some new geologic wrinkles: Proc. Am. Assoc. Ady. Sci., Vol. XXXV, 1886, p. 227; also Am. Jour. Sci., 3d series, Vol. XXXII, 1885, p. 324. Place of Niagara Falls in geologic history: Proc. Am. Assoc. Ady. Sci., Vol. XX XV, 1886, pp. 222-228. Prehistoric hearth under Quaternary deposits in western New York: Sci. Am. Supp., Vol. XXIII, 1887, pp. 9221-9229. —— Old shore lines in the Ontario Basin: Proc. Canadian Inst., 3d series, Vol. VI, 1888, pp. 2-4. —— Changes of level of the Great Lakes: The Forum, Vol. V, i888, pp. 417-428. BIBLIOGRAPHY. 35 GitperT, G. K. History of Niagara River: Sixth Rept. New York State Reserva- tion at Niagara, 1890, pp. 61-84. Postglacial anticlinal ridges near Ripley and Caledonia, New York: Proc. Am. Assoc. Ady. Sci., Vol. XL, 1891, pp. 249-250. Niagara River: Nat. Geog. Monographs, No. 7, 1895, 34 pages. Old tracks of Erian drainage in western New York: Bull. Geol. Soc. Amer- ica, Vol. VIII,#1897, pp. 285-286. Modification of the Great Lakes by earth movement: Nat. Geog. Mag., Vol. VIII, 1897, pp. 283-247. ——— Recent earth movement in the Great Lakes region: Tenet Ann. Rept. U.S. Geol. Survey, Pt. II, 1898, pp. 601-647. —— Bowlder pavement at Wilson, New York: Jour. Geol., Vol. V1, 1898, pp. T1175. Glacial sculpture in western Newy York: Bull. Geol. Soc. America, Vol. X, 1899, pp. 121-130. Dislocation at Thirtymile Point, New York: Bull. Geol. Soc. America, Vol. X, 1899, pp. 131-134. Gout. D. T. Preglacial course of Rocky River in Ohio: Berea (Ohio) Advertiser, April 16, 1886. Grapau, A. W. The preglacial channel of Genesee River: Proc. Boston Soc. Nat. Hist., Vol. XX VI, 1894, pp. 359-369. GRANGER, EBENEZER. Notice of a curious fluted rock at Sandusky, Ohio: Am. Jour. Sci., Ist series, Vol. VI, 1823, pp. 179-180. GREENE, G. M. Geology of Monroe County, Indiana: Second Ann. Rept. Bureau of Statistics and Geology, State of Indiana, 1880, pp. 427-449. Grestey, W.S, Fifth Ann. Rept. New York Geol. Survey, Fourth Geol. District, 1841, 30 pages. Natural history of New York, Pt. IV, Geology, comprising the survey of the Fourth Geol. District, 1843, 675 pages. On exposures of broken and contorted strata and intermingled drift on the shore of Lake Erie: Am. Jour. Sci., 1st series, Vol. XLV, 1848, pp. 327-329. 36 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Hart James. Glaciated surfaces of cherty limestone from near Niagara: Am. Jour. - Sci., Ist series, Vol. XLV, 1845, p. 332. Niagara Falls, their slaves changes and the geology and topography of the surrounding country: Boston Jour. Nat. Hist., Vol. IV, 1844, pp. 206-234. Notice of the geological position of the cranium of the Castoroides ohio- ensis: Boston Jour. Nat. Hist., Vol. V, 1847, pp. 385-391. Note on recession of Niagara Falls: Proc. Am. Assoc.’Ady. Sci., Vol. X, 1857, pt. 2, pp. 76-78. Hayes, Grorcr F. Remarks on the geology and topography of western New York: Am. Jour. Sci., 1st series, Vol. XX XV, 1839, pp. 86-105. Evidences of diluvial currents: Am. Jour. Sci., 1st series, Vol. XXXV, 1839, p. 191. Hayns, Joun L. Probable influence of icebergs upon drift: Am. Jour. Sci., 1st series, Vol. XLY, 1843, pp. 316-319; also Boston Jour. Nat. Hist., Vol. IV, 1844, pp. 426-452. Haymonp, Rurus. Notices of remains of mastodon, etc.: Am. Jour. Sci., Ist series, Vol. XLVI, 1844, pp. 294-296. Geology of Franklin County, Indiana: First Ann. Rept. Geol. Survey Indi- ana, 1869, pp. 175-202. Herzer, H. Geology of Brown County, Ohio: Geology of Ohio, Vol. III, 1878, pp. 942-944, Hicn, R. R. Newly discovered glacial phenomena in the Beaver Valley: Am. Naturalist, Vol. XXIV, 1890, pp. 816-818. Glacial grooves at the southern margin of the dvift: Bull. Geol. Soc. America, Vol. IL, 1891, pp. 457-464. Note on the buried drainage system of the pps Ohio: Science, Vol. XXII, 1893, p. 170. The inner gorge terraces of the Upper Ohio and Beaver rivers: Am. Jour. Sci., 3d series, Vol. XLIX, 1895, pp. 112-120. Hitpreru, §. P. Miscellaneous observations on the coal, diluvial, and other strata of certain portions of the State of Ohio: Am. Jour. Sci., 1st series, Vol. XIII, 1828, pp. 38-40. Bowlder stones of primitive rocks in Ohio: Am. Jour. Sci., 1st sOnIS, Vol. XVI, 1829, pp. 154-159. ‘ Falls of the Cuyahoga, etc.: Am. Jour. Sci., Ist series, Vol. XX XI, 1837, pp. 1-84. Hinz, Franxurn C. Geology of Logan and Champaign counties, Ohio: Geology of Ohio, Vol. III, 1878, pp. 482-495. Hopex, Jamus T. Geology of Coshocton County, Ohio: Geology of Ohio, Vol. III, 1878, pp. 562-563. Houiry, Grorce W. Niagara, its history, geology, etc. New York, 1872, 165 pages. The proximate future of Niagara: Proc. Am. Assoc. Ady. Sci., Vol. XXII, 1874, pt. 2, pp. 147-155. Hoimes, W.H. Traces of glacial man in Ohio: Jour. Geol., Vol. I, 1893, pp. 147-163. Hussey, Joun. Geology of Clinton, Fayette, Shelby, aul Mae counties, Ohio; Gasloss of Ohio, Vol. III, 1878, pp. 429-481. BIBLIOGRAPHY. Bill Hyatt, AvpHEus. Rockruins, Niagara Falls: Am. Naturalist, Vol. I, 1869, pp. 77-85. JaMES, JospPH F. The geology and topography of Cincinnati: Jour. Cincinnati Soc. Nat. Hist., Vol. LX, 1886, pp. 20-31, 136-141. An ancient channel of the Ohio River at Cincinnati: Jour. Cincinnati Soc. Nat. Hist., Vol. XI, 1888, pp. 96-101. The Ivorydale well in Mill Creek Valley: Jour. Cincinnati Soc. Nat. Hist., Vol. XI, 1888, pp. 102-104. A brief history of the Ohio River: Pop. Sci. Monthly, Vol. XX XVIII, 1891, pp. 739-748. The Cincinnati ice dam: Am. Geologist, Vol. XI, 1893, pp. 199-202. Jitison, B. C. Report on geology of Allegheny County, Pennsylvania: Trans. Med. Soc. Pennsylvania, 4th series, Vol. II, 1866, pp. 42-46. River terraces in and near Pittsburg: Proc. Pittsburg Acad. Sci., 1893. JOHNSON, LauRENcE. The parallel drift hills of western New York: Annals New York Acad. Sci., Vol. Il, 1882, pp. 249-266. Kine, AtFrep T. On the ancient alluvium of the Ohio and its tributaries: Proc. Phila. Acad. Sei., Vol. VII, 1856, pp. 4-8. Kuiprart, Joun H. Agricultural survey of Ohio: Rept. Geol. Survey Ohio, 1870, pp. 318-400. Lanepon, F. W. The giant beaver in Ohio: Jour. Cincinnati Soc. Nat. Hist., Vol. V1, 1883, pp. 238-239. LaprHam, D. and I. A. Observations on the primitive and: other bowlders of Ohio: Am. Jour. Sci., Ist series, Vol. X XII, 1832, pp. 300-308. Larnam, I. A. Notice of the Louisville and Shippingsport Canal and of the geology of the vicinity: Am. Jour. Sci., Ist series, Vol. XIV, 1828, pp. 65-69. On the existence of certain lacustrine deposits in the vicinity of the Great Lakes: Am. Jour. Sci., 2d series, Vol. III, 1847, pp. 90-94. Lestey, J. P. Manual of coal and its topography. Philadelphia, 1856, 224 pages. On a curious instance of reverse drainage: Proc. Phila. Acad. Sci., Vol. X, 1859, pp. 8-9. Note on a map intended to illustrate five types of earth surface in the United States, between Cincinnati and the Atlantic: Trans. Am. Philos. Soe., new series, Vol. XIII, 1869, pp. 305-312. On terrace levels in Pennsylvania: Am. Jour. Sci., 3d series, Vol. XVI, 1878, pp. 68-69. Geology of Beaver County, Pennsylvania: Second Geol. Survey Pennsyl- yania, Rept. Q, 1878, pp. ix—xlvi. Geology of Lawrence County, Pennsylvania: Second Geol. Survey Pennsyl- vania, Rept. Q*, 1879, pp. ix—-xxxvi. Preglacial channels of Allegheny and Clarion rivers: Proce. Am. Philos. Soc., Vol. XVIII, 1880, pp. 365-366. Geology of Mercer County, Pennsylvania: Second Geol. Survey Pennsyl- vania, Rept. Q*, 1880, pp. xi-xiv. Report on the oil region of Pennsylvania: Second Geol. Survey Pennsyl- yania, Rept. 1°, 1880, pp. v-xvil. 38 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Lustey, J. P. Geology of Mrie and Crawford counties, Pennsylvania: Second Geol. Survey Pennsylvania, Rept. Q*, 1881, pp. v—xiil. On the former flow of the Upper Ohio: Proc. Am. Philos. Soc., Vol. XIX, 1882, p. 353. On the glacial erosion and outlet of the Great Lakes: Proc. Am. Philos. Soc., Vol. XX, 1883, pp. 95-101. Wright’s ee dam at Cincinnati: Science, Vol. II, 1883, p. 436. Report on the terminal moraine in Pennsylvania and western New York: Second Geol. Survey Pennsylvania, Rept. Z, 1884, pp. v—xlix. Geology of Warren County, Pennsylvania: Second Geol. Survey Pennsyl- vania, Rept. I*, 1884, pp. ix—xx. Leverert, Frank. Natural gas borings in Indiana: Am. Geologist, Vol. IV, 1889, pp: 6-21. Changes of climate indicated by interglacial beds and attendant oxidation and leaching: Proc. Boston Soc. Nat. Hist., Vol. XXIV, 1890, pp. 455-459. Glacial studies bearing on the antiquity of man: Proc. Boston Soc. Nat. Hist., Vol. XXIV, 1890, pp. 585-586. The Cincinnati ice dam: Proc. Am. Assoc. Ady. Sci., Vol. XL, 1891, pp. 250-251; also Am. Geologist, Vol. VIII, 1891, pp. 232-933. Relation of a Loveland, Ohio, implement- hea ing terrace to the moraines of the great ice sheet: Proc. Am. Assoc. Ady. Sci., Vol. XL, 1891, pp. 361-369. Pleistocene fluvial plains of western Penner Am. Jour. Sci., 3d series, Vol. XLII, 1891, pp. 200-212. White clays of the Ohio region: Am. Geologist, Vol. X, 1892, pp. 18-25. Correlation of moraines with the raised beaches of Lake Hrie: Am. Jour. Sci., 3d series, Vol. XLIII, 1892, pp. 281-301; abstract in Trans. Wisconsin Acad. Sci., Vol. VIII, 1892, pp. 233-240. Supposed glacial man in southwestern Ohio: Am. Geologist, Vol. XI, 1893, pp- 186-189. Relation of the attenuated drift border to the outer moraine in WONG: Am. Geologist, Vol. XI, pp. 215-216. The glacial succession in Ohio: Jour. Geol., Vol. I, 1898, pp. 129-146. Preglacial valleys of the Mississippi and tributaries: Jour. Geol., Vol. ILI, 1895, pp. 740-763. Further studies in the upper Ohio region: Am. Jour. Sci., 3d series, Vol. XLVII, 1894, pp. 247-283. Correlation of New York moraines with raised beaches of Lake Erie: Am. Jour. Sci., 3d series, Vol. L, 1895, pp. 1-20. The glacial deposi of ‘indian. Inland Educator, Vol. I1, 1896, pp. 23-39; also Studies in Indiana Geography, pp. 28-41. Terre Haute, 1897. Water resources of Indiana and Ohio: Eighteenth Ann. Rept. U. S. Geol. Survey, Pt. IV, 1897, pp. 419-559. Changes in the drainage of southern Ohio: Bull. Denison Univ., Vol. [X 1897, pt. 2, pp. 18-21. Correlation of moraines with beaches on the border of Lake Erie: Am. Geologist, Vol. XXI, 1898, pp. 195-199. 2) BIBLIOGRAPHY. . 39 Leverett, Frank. The Yarmouth, Sangamon, and Peorian soils and weathered zones: Jour. Geol., Vol. VI, 1898, pp. 171-181, 238-249. The wells of northern Indiana: Water-Supply and Irrigation Paper U. S. Geol. Survey No. 21, 1899, 82 pages. The wells of southern Indiana: Water-Supply and Irrigation Paper U. S. Geol. Survey No. 26, 1899, 64 pages. Leverre, G. M. Observations in Dekalb, Laporte, and other counties in Indiana: Fifth Ann. Rept. Geol. Survey Indiana, 1873, pp. 480-474. Observations on lakes in northern Indiana: Seventh Ann. Rept. Geol. Sur- vey Indiana, 1875, pp. 469-503. Lewis, H. C. The great terminal moraine across Pennsylvania: Proc. Am. Assoc. Ady. Sci., Vol. XIII, 1882, pp. 389-398; also Science, Vol. I, 1882, pp. 163-167. The great ice age in Pennsylvania: Jour. Franklin Inst., 3d series, Vol. LXXXYV, 1883, pp. 287-307. Map of the terminal moraine in Pennsylvania: Proc. Am. Philos. Soc., Vol. XX, 1883, pp. 662-664. Supposed glaciation in Pennsylvania south of the terminal moraine: Am. Jour. Sci., 3d series, Vol. XXVIII, 1884, pp. 276-285. Report on the terminal moraine across Pennsylvania and western New York: Second Geol. Survey Pennsylvania, Rept. Z, 1884, 299 pages. The ice of the Glacial period: Proc. Phila. Acad. Sci., Vol. XX XV, 1884, pp. 47-49, 70-71. Marginal kames: Proc. Phila. Acad. Sci., Vol. XX XVI, 1885, pp. 157-1738. Lincotn, D. F. Glaciation in the Finger lake region of New York: Am. Jour. ’ Sei., 3d series, Vol. XLIV, 1892, pp. 290-301. Amount of glacial erosion in the Finger lake region: Am. Jour. Sci., 3d series, Vol. XLVII, 1894, pp. 105-113. Geology of Seneca County, New York: Fourteenth Ann. Rept. New York Geol. Survey, 1897, pp. 60-125. linpemutn, A. C. Geology of Darke County, Ohio: Geology of Ohio, Vol. IIL, 1878, pp. 496-518. Locks, JoHN. Report on southwestern Ohio: Rept. Geol. Survey Ohio, 1838, pp. 201-286. : Glacial planing and bowlders in Ohio: Am. Jour. Sci., Ist series, Vol. XLI, 1841, pp. 175-176. Notice of a prostrate forest under the diluvium of Ohio: Trans. Assoc. Am. Geol., 1843, pp. 240-241. LyeLi, Cuarues. On the geological position of Mastodon giganteum and asso- ciated fossil remains at Big Bone Lick, Kentucky, and other localities in the United States and Canada: Am. Jour. Sci., 1st series, Vol. XLVI, 1844, pp. 320-323. On the ridges, elevated beaches, inland cliffs, and bowlder formations of the Canadian lakes and valley of the St. Lawrence: Am. Jour. Sci., 1st series, Vol. XLVI, pp. 314-317. Travels in North America, 1841-1842. New York, 1845, 2 vols. 40 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Lyon, Srpney S. Supposed drift near Ashland, Kentucky: Second Geol. Report of Kentucky for 1856 and 1857, p. 360. McCasuix, Davip. Geology of Jay County, Ian Twelfth Ann. Rept. Geol. Survey Indiana, 1882, pp. 153-176. Geology of Johnson County, Indiana: Thirteenth Ann. Rept. Geol. Survey Indiana, 1883, pp. 116-137. Marcou, Junes. Le Niagara quinze ans apres: Bull. Soc. géol. France, 2d series, Vol. XXII, 1865, pp. 290-300, 529-530. Martner, W. W. First Annual Rept. Geol. Survey Ohio, 1838, pp. 5-23. Second Annual Rept. Geol. Survey Ohio, 1838, pp. 5-39. On the occurrence of bowlders and scratches: Am. Jour. Sci., 1st series, Vol. XLI, 1841, pp. 174-176; also Trans. Assoc. Am. Geol., 1843, pp. 27-28. Mitier, 8. A. The drift of the central part of the continent:,\Jour. Cincinnati Soc. Nat. Hist., Vol. [V, 1881, pp. 183-234. Moorz, Josppu. Weare stone quarry of Upper Silurian iFienestions near Richmond, Indiana: Proce. Indiana Acad. Sci., 1896, pp. 75-76. The Randolph mastodon: Eno, Indiana Acad. Sci., 1896, pp. 277-278. Newserry, J. S. Notes on the surface geology of the basins of the Great Lakes: Proce. Boston Soc. Nat. Hist., Vol. LX, 1865, pp. 42-46. On the surface geology of the basin of the Great Lakes and the yalley of the Mississippi: Annals Lyceum Nat. Hist. New York, Vol. LX, 1870, pp. 213- 934; also Am. Naturalist, Vol. IV, 1871, pp. 193-218. The geological position of the remains of elephant and mastodon in North America: Trans. Lyceum Nat. Hist. New York, Vol. I, 1871, pp. 77-83. Physical geography and general geology of Ohio: Geology of Ohio, Vol. I, 1873, pp. 16-167. Geology of Cuyahoga and Summit counties, Ohio: Geology of Ohio, Vol. I, 1873, pp. 171-228. Note on the vegetation of the drift: Proc. Cleveland Acad. Sci., Vol. 1, 1874, pp- (6-80. Surface geology of Ohio: Geology of Ohio, Vol. II, 1874, pp. 1-80. Geology of Erie and Lorain counties, Ohio, and the islands of Lake Hrie: Geology of Ohio, Vol. II, 1874, pp. 183-224. On the structure and origin of the Great Lakes:, Proc. Lyceum Nat. Hist. New York, 2d series, 1874, pp. 136-138. Geology of Tuscarawas, Columbiana, Portage, and Stark counties, Ohio: Geology of Ohio, Vol. III, 1878, pp. 52-176. Geology of Jefferson and Wolhowine counties, Ohio: Geology of Ohio, Vol. III, 1878, pp. 716-814. — On the origin and drainage of the basins of the Great Lakes: Proc. Am. Philos. Soc?, Vol. XX, 1883, pp. 91-95. The evidences of ancient glaciation in North America and their bearing on the theory of the ice period: Trans. New York Acad. Sci., Vol. Il, 1883, pp. 155-159. The drift deposits of Indiana: Fourteenth Ann. Rept. Geol. Survey Indiana, 1884, pp. 85-97. BIBLIOGRAPHY. 4] Newprrry, J. S. The erosive power of glacier ice and its influences on the topog- raphy of North America: Trans. New York Acad. Sei., Vol. III, 1885, pp. 51-52. The eroding power of ice: School of Mines Quart., Vol. VI, 1885, pp. 142-153. North America in the ice period: Pop. Sci. Monthly, Vol. XXX, 1886, jojos Wealil Orton, Epwarp. On the occurrence of a peat bed beneath deposits of drift in southwestern Ohio: Am. Jour. Sci., 2d series, Vol. L, 1870, pp. 54-57, 293; also Rept. Geol. Survey Ohio, 1869, pp. 165-167. Geology of Montgomery County, Ohio: Rept. Geol. Survey Ohio, 1869, pp. 143-164. ; Geology of Highland County, Ohio: Rept. Geol. Survey Ohio, 1870, pp. 255-310. Report on the third geological district of Ohio: Geology of Ohio, Vol. I, 1873, pp. 365-480. Geology of Pike, Ross, and Greene counties, Ohio: Geology of Ohio, Vol. II, 1874, pp. 611-696. Geology of Warren, Butler, Preble, and Madison counties, Ohio: Geology of Ohio, Vol. III, 1878, pp. 381-428. — Geology of Franklin County, Ohio: Geology of Ohio, Vol. II, 1878, pp. 596-646. The drift deposits of Ohio: Geology of Ohio, Vol. VI, 1888, pp. 772-782. Rock waters of Ohio and flowing wells from the drift: Nineteenth Ann. Rept. U. 5. Geol. Survey, Pt. IV, 1898, pp. 633-718; also in Report of Ohio State Board of Health for 1898. PacxarpD, A. S. The hairy mammoth: Am. Naturalist, Vol. Il, 1868, pp. 23-35. Punt, 5. D. Mastodon in swamp in Ohio: Jour. Cincinnati Soc. Nat. Hist., Vol. VIII, 1886, pp. 117-118. ‘Puinney, A. J. Geology of Delaware County, Indiana: Eleventh Ann. Rept. Geol. Survey Indiana, 1881, pp. 126-149. Geology of Randolph County, Indiana: Twelfth Ann. Rept. Geol. Survey Indiana, 1882, pp. 177-195. Geology of Grant County, Indiana: Thirteenth Ann. Rept. Geol. Survey Indiana, 1883, pp. 138-153. 3 Geology of Henry County and portions of Randolph, Wayne, and Delaware counties, Indiana: Fifteenth Ann. Rept. Geol. Survey Indiana, 1886, pp. 97-116. The natural gas field of Indiana: Eleventh Ann. Rept. U. S. Geol. Survey, Pt. I, 1891, pp. 579-742. Prmrcr, 8. J. The preglacial Cuyahoga Valley in Ohio: Am. Geologist, Vol. XX, 1897, pp. 176-181. PrummMer. Joun T. Suburban geology, or rocks, soil, and water about Richmond, Wayne County, Indiana: Am. Jour. Sci., Ist series, Vol. XLIV, 1843, pp. 281-313. ~ Poutman, Jutius. The life history of Niagara River: Trans. Am. Inst. Min. Eng., Vol. XVII, 1889, pp. 322-338; also Proc. Am. Assoc. Ady. Sci.. Vol. XXXII, 1883, p. 202, and Vol. XX XV, 1887, pp. 221-299. 42 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Ranpat, F. A. Observations of the geology around Warren, Pennsylvania: Second Geol. Survey Pennsylvania, Rept. I, 1874, pp. 50-54; alee Rept. I*, 1883, pp. 1-15, 19-22, 309-311. Reap, M. C. Sketches of the geology of Geauga and iSiel aes counties, Ohio: Rept. Gea Survey Ohio, 1870, pp. 463-484. Geology of stitainale, Trumbull, Lake, and Gaines counties, Ohio: Geology of Ohio, Vol. I, 1873, pp. 481-533. Geology of Huron, Richland, Knox, and Licking counties, Ohio: Geology of Ohio, Vol. III, 1878, pp. 289-361. — Geology of ‘Ashalesnal Wayne, and Holmes counties, Ohio: Geology of Ohio, Vol. ILI, 1878, pp. 519-561. Water supply of drift clay lands of Ohio: Reprint from Ohio Agricultural report, 5 pages. Reprrep, Wm. C. On the cause of the drift phenomena in Portage County, Ohio: Am. Jour. Sci., Ist series, Vol. XLVII, 1844, pp. 120-121. Dispersion of bowlders and drift: Proc. Am. Assoc. Ady. Sci., Vol. II 1848, pp. 310-311. Reep, STEPHEN. On trains of bowlders, and on the transport ot Jbowlders to:a level above that of their source: Am. Jour. Sci., 3d series, Vol. V, 1873, pp. 218-219. RippeLL, Joun L. As these names represent only the main divisions of the Glacial epoch, others are necessary to denote the sabdivisions. In the report on the Illinois glacial lobe, and in the present report, several names are thus introduced to designate the moraines and their associated sheets of drift. These names are usually selected from towns located on the moraines or from streams whose courses are governed by the moraines. In most cases they have come into use in the office and in correspondence with other gla- cialists, as a convenient form of reference. The selection of names thus made seems suitable for general use. The outline given below aims to cover the events between the deposi- tion of the oldest recognized drift sheet and the final recession of the ice sheet into the region north of the Great Lakes. The main divisions appear to be much longer than the secondary ones. The latter are not thought to be marked by intervals sufficiently prolonged to merit the application of the term epoch. It is probable, however, as shown further on, that some oscillations of the ice front occurred, so that the moraines on which these subdivisions are based do not mark simply halts in the recession of the ice. | OUTLINE OF DRIFT SHEETS AND INTERVALS. 1. Oldest recognized drift sheet, the sub-Aftonian of Chamberlin, and perhaps the Albertan of Dawson. 2. First interval of deglaciation, Aftonian of Chamberlin. 3. Kansan drift sheet of the lowa geologists. 1The Illinois Glacial Lobe, Mon. U. 8. Geol. Survey, Vol. XK2 VII. 2See Geikie’s Great Ice Age, third edition, 1894, pp. 754-774. See also Jour. Geol., Vol. III, an 270-277, and Vol. IV, pp. 872-876. MICHIGAN WAYNE WASHTENAW 87 JACKSON. CALHOUN KALAMAZOO VAN BUREN 4) BERRIEN CASS: ST.JOSEPH BRANCH HILUSDALE LENAWEE, MONROE DIANA. | LAPORTE 2 ST.JOSEPH 3 ELKHART 45 41 & KOSCIUSKO 3 MARSHALL {0 STARKE {1 PULASKI 12 FULTON 13 WHITLEY 14 ALLEN 15 ADAMS (6 WELLS 7 HUNTINGTON. 1B WABASH MIAMI “ASS CARROLL HOWARD GRANT BLACKFORD JAY ~ RANDOLPH FRANKLIN. DECATUR BARTHOLOMEW BROWN. JACKSON JENNINGS: RIPLEY DEARBORN SWITZERLAND JEFFERSON Scort WASHINGTON CLARK FLOYD ¥ HARRISON OHIO - | WILLIAMS 19 20 21 22 23 24 25 26 27 28 2 30 31 32 33 34 35 36 37 38 39 40 4) 42 43 Ag 45 46 aq 48 43 50 51 52 53 54 55 56 57 5B 7 TRUMBULL 10 LORAIN 1 ERIE 12 SANDUSKY 13 Woop 15 DEFIANCE 16 PAULOING 17 PUTNAM. - 1B HANCOCK 22 SUMMIT 23 PORTAGE 24 MAHONING 25 COLUMBIANA 26 STARK 35 VAN WERT 34 MERCER 3S AUGLAIZE 36 HARDIN 37 MARION 36 MoRROW 39 KNOX 40 HOLMES 41 COSHOCTON 42 TUSCARAWAS. 43 CARROLL 43 HARRISON 45 JEFFERSON 46 BELMONT 47 GUERNSEY 48 MUSKINGUM 49 LICKING 50 DELAWARE 51 UNION. 52 LOGAN 53 SHELBY 54 DARKE 55 MIAMI. 56 CHAMPAIGN 57 CLARK 58 MADISON 5S FRANKLIN 60 PICKAWAY 6] FAIRFIELD 62 PERRY. 86 WASHINGTON 7 ATHENS 68 HOCKING 69 VINTON 72 GREENE 73 MONTGOMERY 74 PREBLE 75 BUTLER 76 WARREN 77 CLINTON 78 HIGHLAND 19 PIKE BO JACKSON 81 MEIGS @z2 GALLIA 83 LAWRENCE E i) KENTUCKY 17 ROBERTSON 18 FLEMING CARTER z0 BOYD 21 LAWRENCE 25 NICHOLAS BOURBON ScoTT 28 FRANKLIN 29 SHELBY + 30 JEFFERSON 36 CLARK 37 MONTGOMERY NEW YORK | JEFFERSON 5 (lL GENESEE 12 WYOMING 13. LIVINGSTON 14 ONTARIO 20 27 ALLEGANY 28 CATTARAUGUS 29 CHAUTAUQUA PENNSYLVANIA 1 ERIE 2 WARREN 3 MC.KEAN 4 POTTER 5 TIOGA 6 BRADFORD 7 SUSQUEHANNA & WYOMING § SULLIVAN 0 LYCOMING 11 CLINTON 12 CAMERON \4 FOREST 15 VENANGO 16 CRAWFORD 7 MERCER 18 LAWRENCE BUTLER CLARION 21 JEFFERSON 2 CLEARFIELD 3 CENTER UNION: 25 NORTHUMBERLAND MONTOUR 27 COLUMBIA 34 WESTMORELAND SOMERSET FAYETTE 37 WASHINGTON GREENE {0 HARRISON (1 DODDRIDGE 12 TYLER 13 RITCHIE 14 PLEASANTS wooo: 32 NICHOLAS 33 WEBSTER POCAHONTAS. GREENBRIER 38 UNCOLN WAYNE U.S. GEOLOGICAL SURVEY Cnn y at = 49° | Versai ] 6 J ; MONOGRAPH XLI PL. Il WHER 4M . sual} iinet es SS Rat 3 Ss GLACIAL MAP OF AREA DISCUSSED AND OF SOME OUTLYING DISTRICTS BY FRANK LEVERETT 1900 Seale oO 10 20 30 “k0 50 ee _ = 19 0 10 20 30 4050 ——_—— 100 Kilometers Contour interval 500 feet Datum is mean sea level NOTE The moraines inthe Canadian part of the map, so tar as represented, are based uponF'B. Taylors investigations, and the shore lines largely upor JW. Spencers. The moraines and shore tines on the Thumb “of Michigan aebasedupon Taylors studies and those of the Michigan. Geological Survey. The border of the Wisconsin dritinPennsywania, eastol the 78 '* meridian, ustrom the Loree by. BCarvel Lewis, and that of northwestern PennsyWand, andeastern, Ohio follows the boundary established by GFrederick Wright The border of an. eartier dritt. sheet east of the 780 Meridian ws based upon te work of EAWilliams Jr and is trcomplete. Theshore lines tor- dering the Ere and Ontarto basins have been traced tr. large part by earlier students, rota bl. LYLE EOE Charles Whittlesey, GE. Gilbert, NH Winckel, AAWright, MCRead, ara hl Fairchild . The present writer: supplemented and completed the mapping of beaches. ; The main morainte system of the lateWisconsin drift wastrlarge part ecamined byl Cthambertin prior to the writersexaminations. Several of the miner moraines of northwestern Ohio were mapped by Gilbertand Winchell for the Ohio Geological Survey; and moraines tnnorteastern Indiana by CRD ryer, for the Indiana Survey. The present writer has not only mapped the remaining moraines but has avamined in sone detail the entiresertes of moraines, the several Arie sheets, andthe glacial drainage of Indiana, Ohto northwestern Pennsyl varua, and western NewXork:, 100 Miles = 78° ates 13 ze JUUUS BIEN S CO.LITH NY. | LEGEND Moraines with strong expression mainly land-laid Water-laid moraines with faint expression KansantorPre-Kansan? drift Ca Old driftof eastern Pennsylvania Tilinoian drift Farly Wisconsin drift Late Wisconsin drift Local glacial lakes ol sai Great glacial lakes, Maumee Whitllesey, etc. —_ ——~_| Shore of Lake Maumee and its outlets and Lake Chicago ae Shore of Lake Whittlesey and Lake Saginaw Unglaciated region Ra cred Not examined uy Glacial striae 20 2) WAPERR« HE 36 WASHTENAW 37 JAOKBRON 2) BERRIEN “6 47 MONROE INDIANA 5) DEARBORN Sy SWITZERLAND 53 JEFFERSON 2 fULTON a 63 MORGAN A ODL uf a oe H i : eSesisukasts sess: ane gsgesee 15 OWEN 1G HARRISON 17 ROBERTSON Zi LAWRENCE @2 ELLIOTT 23 ROWAN Evcn 35 worrooMERY NEW YORK 1 JEFFERSON 2B CATTARAUGUS 25 CHAUTAUQUA PENNSYLVANIA 10 KYCOMINO 11 CLINTON 12 CAMERON 19 EK 14 FOREST 15 VENANGO. 16 CRAWFORD ER. 34 WESTMORELAND 35 SOMERSET 36 FAYE 37. WASHINGTON as GREEN 1p Lew SSSSCRE BY SSRNE CREE: U.S.GEOLOGICAL SURVEY MONOGRAPH XLI PL. {I h <7 Ae NS i CHESTER, A INO\ 4Iy GLACIAL MAP OF AREA DIS'CUS SED | AND OF SOME OUTLYING DISTRICTS BY FRANK LEVERETY 1900 Seale 100 Miles — _ 100 Kilometers 100 10 20 40 40 ———— = Contour interval 500 feet Datumis mean Sea lev NOTE The moraines inthe Canadian part of He map, so tar as represented. are based. upon FB. Taylors investigations, and the shore lines largely upon JW. Spencers. The moraines and shore tines on the *Thumo of Michigen t aebasedupon Taylors sindies and those of theMichigar Geological Survey. The border of the Wisconsin driftinPennsywania, eastot the 78 meridian, istrom the map by ACarvel Lewis,and that of northwestern Pennsylvania i i | and eastern, Ohio follows the boundary established by GFrederick Wright The border of an eartier aritt sheet east of the 740Meridian ts based upon Gie work of EH Williams Jr.and istncomplete. Theshore tones bor dering the Erve and Ontaria basis have been tra ced. tn large part by cartier students, notably Bela Hubbard, Charles Whittlesey, CF. Gilbert, NA Winchell AAWright MC Read, anal Facrchild The present writerhas supplemented and completed the mapping | beaches. {| The main moraine system of the late Wisconsin drift was large part | evamined byl CChambertin prior to tie wretersexanunations. Several of te minor moraines of northwestern Ohio were mapped by Gilbert ard. Winchell for the Ohto Geological Survey, and moraines tnnorGwastern Indiana by CRDryer, for the Indiana Survey. The present writer has nat only mapped the rematning moraines but has evanined tn. some detail the entreserwes of MORUNES, theseverad arett sheets, ylvarua, and and the glacial drainage of Indiana, Ohio, northwestern PAnnsy Waterlaid moraines with faint expression KansantorPre-Kansan? drift Sa code ea Old dvift of eastern Pennsylvania [Oe ERG Minoan dvift Karly Wisconsin drift Led Tate Wisconsin drift Gravel plains and lines of Slacial drainage Great glacial |i Maumee Whittlesey, ete —— eer ed Shore of Lake Maumee and its outlets and Lake Chicago eee ve of Lake Whitllesey and Lake Saginaw ~ — = | Shore of Lake Warren Unglaviatedregion a Not examined Glacial strie western New Fork: JOUUS BIEN B CO LITH M¥ ne ee 4a tr ar . OUTLINE OF DRIFT SHEETS AND INTERVALS. 51 Second or Yarmouth interval of recession or deglaciation. Ilinoian drift sheet. Third or Sangamon interval of recession or deglaciation. Iowan drift sheet and main loess deposit. Fourth or Peorian interval of recession or deglaciation. Early Wisconsin drift sheets, as represented in Illinois, the display in the Ohio district being less complete. §2 G9 Sl Ga Ex = a. Shelbyville morainic system. b. Champaign morainic system. c. Bloomington morainic system. d. Marseilles morainic system. 10. Fifth interval of recession (unnamed), shown by shifting of ice lobes. 11. Late Wisconsin drift sheet, as represented in the Ohio district. a. The main morainic system and attendant great bowlder belts. b. Mississinawa (Valparaiso?) morainic system; includes Union and Mississinawa moraines of the Maumee-Miami lobe and the Powell and Broadway moraines of the Scioto lobe, and is a probable correlative of the Valparaiso morainic system of the Lake Michigan lobe. c. St. Johns or Salamonie moraine. d. Wabash moraine. e. St. Marys or Fort Wayne moraine. Ff. Lake Maumee beaches and correlative moraines. g. Lake Whittlesey beach and correlative moraines. h. Lake Warren beaches and correlative moraines. 7 Lake Dana beach (Lake Lundy’). j. Lake Iroquois beach. By reference to the glacial map, PI. II, the extent of exposure of each till sheet and the distribution of the moraines and the lake beaches may be seen. It will be observed that the oldest drift sheet of this region (the Kansan or pre-Kansan) is exposed only in a limited area in northwestern Penn- sylvania. The next younger or Illinoian drift sheet has not been recognized in northwestern Pennsylvania, but it is extensively exposed in southwestern Ohio, southeastern Indiana, and in the glaciated portion of Kentucky. The Iowan drift sheet appears not to extend beyond the limits of the Wisconsin drift in the region covered by the map, but a silt deposit which appears to 52 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. be of Iowan age covers the I]linoian drift and extends beyond it into the unglaciated district to an undetermined distance. The early Wisconsin drift is exposed outside the limits of the late Wisconsin in southeastern Indiana and southwestern Ohio, and may perhaps be represented in the southern portion of the drift east of the reentrant angle im the glacial boundary in western New York. But in central and eastern Ohio and in northwestern Pennsylvania it occurs to but a limited extent, if at all, outside the late Wisconsin. The late Wisconsin drift covers a large part of the glaciated portion of this region. The distribution of its several moraines is indicated on the glacial map. The extent of the great glacial lakes, Maumee, Whittlesey, and Warren, is shown in Pls. XX, XXIJ, XXIII, and XXVI more clearly than in the glacial map. As the several drift sheets, the moraines, and the beaches are discussed in detail farther on, they may be left here with this passing reference. OUTLINE OF ROCK FORMATIONS. Inasmuch as the topographic features of this region depend largely upon the character of its rock formations, a brief outline of the distribution and characteristics of each of the formations here represented seems necessary. Some difficulty is found in the correlation and grouping of certain formations because of the variations which they display when carried over so large a region, and also because of the uncertainty as to exact equivalency where outcrops occur only in widely separated districts. In some cases a forma- tion whose equivalency is well established has a constitution that is quite unlike its constitution in the type locality. In other cases a similar constitution is found in widely separated areas, but the equivalency has not been fully established. The classification of the Ohio rock series presented by Orton in a recent report of this Survey’ and in the last volume’ of the Ohio survey” is based upon a careful comparison of the Ohio series with those of New York and Pennsylvania, where most of the type localities occur. It is, however, designed only for Ohio, and needs to be supplemented in the wider region embraced in the present report. The arrangement of the formations is quite simple, the only axes of 1The rock waters of Ohio, by Edward Orton: Nineteenth Ann. Rept. U. 8. Geol. Survey, Pt. IV, Hydrography, 1898, pp. 638-650. 2 The geological scale of Ohio, by Edward Orton: Geology of Ohio, Vol. VII, 1894, pp. 3-44. OUTLINE OF ROCK FORMATIONS. 53 disturbance that have sufficient prominence to affect seriously the distribu- tion of the rock formations being the Cincinnati arch with its western and eastern branches. Along its broad, flat-topped crest the oldest formations of Ohio and Indiana are exposed. The strata dip westward from the arch and its western arm toward the coal basin of Indiana and Illinois, while between the arms they dip northward toward the coal basin of Michigan. From the borders of Lakes Ontario and Erie the strata dip southward and southeastward to the coal basin of the Allegheny Plateau, while from the * Cincinnati arch they dip eastward toward the same basin. In passing toward the coal basins either from the Cincinnati arch and its branches or from the north border of the region, a succession of rock formations is encountered which have an imbricate arrangement, and the outcrops present an ascending series in the geological scale. The series embraces that part of the. geological time scale which falls between the Trenton epoch of the Lower Silurian or Ordovician and the Permian epoch of the Carboniferous. It includes the groups of rocks set forth in the following series, which are given in their order of development from older to newer. Table of rock formations. Trenton limestone. Lower (Ordovician) --) Utica shale. Hudson River group. Medina group. | Clinton group. Upper.-------------- Niagara group. Salina and Waterlime. Lower Helderberg limestone. Oriskany sandstone. Corniferous limestone. Marcellus shale and Hamilton formation. Genesee, Portage, and Chemung, or Ohio shale. Wayerly or Bedford shale (Catskill? ). | Berea grit and shale (Catskill?). Cuyahoga shale (equivalent of part of Pocono sandstone). Logan conglomerate (equivalent of part of Pocono sandstone). Pottsville, or Conglomerate Coal Measures. Allegheny, or Lower Productive Coal Measures. Conemaugh, or Lower Barren Coal Measures. Monongahela, or Upper Productive Coal Measures. Dunkard beds (Permian?). Trenton limestone and Utica shale—The two lower members of the above series, although clearly represented in a large part of this region beneath later rock D4 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS formations, are not known certainly to have outcrops, and will therefore be passed by without further description. Hudson River group-—T he Hudson River group, as described in the Indiana and Ohio reports, consists of alternating beds of limestone and shale. Its outcrop covers about 4,000 square miles in Ohio, 1,800 square miles in southeastern Indiana, and also a large area in the adjacent part of Kentucky. Its outcrops in the three States embrace the central part of the Cimcinnati arch. The crown of the arch, capped as it is by the soft and friable rocks of this group, has suffered greater reduction than the slopes. Much of it is slightly lower than the portion of the slopes capped by the resistant Lock- port (Niagara) limestone. Medina group—The Medina group outcrops extensively along the south border of Lake Ontario in western New York. It has only a limited out- crop in Indiana and Ohio, on the borders of the Hudson River outcrop. In Indiana and western Ohio the Medina is almost entirely a shale forma- tion, but in eastern Ohio and farther east sandstones are interbedded with the shale. The heaviest beds in New York are shales, but there are also resistant sandstones of considerable thickness. This formation has usually a reddish color, both as shale and as. sandstone. The part taken by the Medina sandstone in forming the waterfalls in western New York is discussed farther on. Clinton group——The Clinton limestone outcrops in western New York immediately south of the outcrop of the Medina. In Ohio and Indiana it is restricted, like the Medina, to a narrow strip on the margin of the outcrop of the Hudson River group.. The most characteristic stratum is a firm . limestone, but the drill has shown that in parts of Ohio it is a sandstone, while in eastern Ohio it becomes shaly. In New York it is a limestone with ferruginous bands. In New York and to some extent in Indiana and Ohio it has produced waterfalls in connection with the underlying shaly beds of the Medina group. Niagara group— The outcrop of the Niagara group in western New York is a narrow strip leading eastward from the Niagara River to the vicinity of Utica. It forms a conspicuous part of the Niagara Falls and the gorge below the falls, as well as other falls and gorges in western New York. The name Niagara was given because of the outcrops on the Niagara River. The group is divided into two formations. The main member is the Lockport aT OUTLINE OF ROCK FORMATIONS. 19) limestone.t Beneath this is the Rochester shale, which includes the Dayton building stone. The Niagara group covers in its outcrops or as a surface rock not less than 5,000 square miles in western Ohio. The main area of outcrop is immediately north and east of the area of the Hudson River group. But there are extensive outcrops farther north in a belt leading from Hardin County northward to the western end of Lake Erie. In Indiana the group appears as the surface rock in an area of fully 5,000 square miles along the north and west borders of the area of the Hudson River group. There is a small area of outcrop in the northwestern part of the State, but that lies outside the region under discussion. A considerable area in northern Kentucky, contiguous to the areas of Indiana and Ohio, also lies outside this region. Salina and Waterlime, or the Onondaga series —I hese two somewhat unlike forma- tions have been referred by Hall, Dana, and others to a single geological epoch, the Onondaga. The outcrop of the Salina formation in New York covers a narrow belt leading eastward from Grand Island in Niagara River to the Hudson River Valley. Its thickness in the eastern part of the State is only 100 to 200 feet, but in Onondaga County, in central New York, it reaches a thickness of 800 feet and continues thick from that locality west- ward. Like the Hudson River group, it consists largely of soft rocks, shales, and shaly limestone, with marls and beds or veins of gypsum. As a result of its soft texture the area of outcrop of this formation has become the site of a shallow basin. The Waterlime formation in western New York rests upon the Salina without a perceptible break or line of demarca- tion. It consists of an impure silico-argillaceous limestone, which is more enduring than the remainder of the salt group and can be distinctly traced through the district. Orton considers it doubtful whether the Salina beds occur in the Ohio rock series. The Waterlime outcrops extensively in northwestern Ohio and also in the north-central part of the State, its outcrops being about as extensive as those of the Niagara group. It is in the main a compact magnesian limestone of drab or brown color. 1The Lockport limestone and the Rochester shale were formerly called the Niagara limestone and the Niagara shale, but by the usage of the United States Geological Survey the term Niagara is now applied only to the group or higher classific unit. 56 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The equivalent of this group in Indiana occurs as the surface rock in a narrow strip on the north and northwest border of the Niagara area north of Indianapolis; also in a small tract in the vicinity of Logansport, and, as interpreted by Phinney, in a considerable area in the northwestern part of the State. The exposures in Indiana are few on account of the great thick- ness of the drift. This is also the case in much of the Ohio area. Lowe- Helderberg limeston—The Lower Helderberg has been separated from the Waterlime in New York and in Indiana, but was classed with it by Orton in his latest report on Ohio. It is an extensive formation in eastern New York, having a thickness of 300 or 400 feet, but it becomes incon- spicuous before reaching the western part of the State. In Indiana, also, it lies mainly outside the region here discussed. It is therefore of little importance to the present discussion. Oriskany sandstone— This formation, like the Lower Helderberg, is con- spicuous in eastern New York, but thins out and disappears before reaching the western part of the State. Although its geographical distribution is about the same as the Lower Helderberg, its fauna and flora are very different, being pronouncedly Devonian. The Sylvania sandstone of northwestern Ohio, which was at first referred to the Oriskany, was finally considered by Orton, on paleonto- logical grounds, to be a part of the underlying formation, and therefore of Upper Silurian instead of Devonian age. Corniferous limestone—'I"he rocks of the Corniferous epoch in New York include the Schoharie and Caudagalli grits as well as the Corniferous lime- stone; but only the limestone appears in western New York. It outcrops in a narrow strip leading eastward from Buffalo to the Hudson River. This limestone, being a more resistant rock in western New York than the forma- tions immediately above and below, now presents a well-defined escarp- ment, over which several small streams have waterfalls. Hall divided it between the Onondaga and Corniferous, the former including the gray lower member and the latter the darker-colored upper member of the formation;’ but the earlier classification by Eaton has now become estab- lished. he thickness of this formation in New York is commonly only 100 to 150 feet, but in the eastern part of the State it in places reaches about 250 feet. 1New York Geol. Survey, Fourth Geol. District, 1843, pp. 151-176. ; 5 §, § f y OUTLINE OF ROCK FORMATIONS. iG In Ohio a Devonian limestone occurs, which is thought by Orton probably to cover more than the single epoch known as the Corniferous in New York. It forms the surface rock in a narrow strip, 5 to 15 miles in width, extending from Sandusky southward past Columbus into north- western Pickaway County, lying immediately east of the outcrop of the Waterlime. It appears in a strip of similar width in northwestern Ohio, on the northwest border of the Waterlime. It also appears on some of the islands in the western end of Lake Erie, and on the elevated tract in Logan and parts of neighboring counties in west-central Ohio. Its thickness seldom exceeds 75 feet. In Indiana the Corniferous or Upper Helderberg outcrops at intervals in a narrow belt extending northward from the Ohio River at the Louisville Rapids to Logansport. It is shown by well drillings to immediately underlie the drift in several counties north of the Wabash River in a belt extending from the Obio-Indiana line westward about to Rensselaer. It is found to present considerable variation in color, composition, and texture in different localities. It is thought by Phinney to range from 30 to 65 feet in thickness, but as the data are largely from drillings this estimate of range may be only an approximation. Marcellus shale and Hamilton formation—[‘he Marcellus shale of New York occupies a narrow depression along the southern border of the Cornif- erous limestone, from the vicinity of Cayuga Lake westward to the city of Buffalo. It is exposed only in a few valleys, the drift being so heavy as to conceal it elsewhere. The greatest observed thickness in western New York does not exceed 50 feet. A portion of it is very bituminous and of “black color. This formation is considered by Hall to be a part of the Hamilton group, there being no well-marked line of separation from that group.’ The Hamilton group of New York consists of a series of shales with occasional thin beds of limestone, and attains a thickness in central New York of nearly 1,000 feet. Hach member of the series thins gradually to the west, until at the border of Lake Erie the thickness of the entire group is scarcely 500 feet. The shales are of blue-gray or green color, and thus contrast strikingly with the dark Marcellus shale. The outcrop is confined to a narrow strip, scarcely 10 miles in average width, which extends from the 1 New York Geol. Survey, Fourth Geol. District, 1843, p. 177. 58 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. eastern end of Lake Erie eastward past the northern ends of the Finger Lakes to the Hudson River Valley. This group of rocks forms the foot- hills of the elevated uplands which occupy the southern portion of western New York. In Ohio there is only a thin development of this group of rocks in the central and northern parts of the State. This group may have a thin development in northern Indiana.t’ It is thought to be represented in the hydraulic limestone at the Louisville Rapids, on the south border of the State.’ Genesee, Portage, and Chemung, or Ohio shale series —[J)nder the names Genesee, Por- tage, and Chemung there are included in New York a complex series of shales with occasional beds of flagstone and sandstone. This series in Ohio appears to be represented by a single great shale formation, now known as the Ohio shale, but designated by the geologists of the first Ohio survey the “shale stratum” or ‘black slate.” The apparently equivalent formation in Indiana is commonly called the ‘black shale.” The Genesee shale of western New York bears a striking resemblance to the Marcellus shale in color and general characteristics, but differs from it in fossils as well as in stratigraphical position. It is a thin formation, — having a thickness of only 25 feet on the borders of Lake Erie and about 150 feet on the shores of Seneca Lake. It appears in the gorge of the Genesee at Mount Morris. The Portage of western New York “presents an extensive develop- ment of shale, shales and flagstones, and finally some thick-bedded sand- stone toward its upper part.” It has excellent exposures in the gorge of the Genesee at Portage Falls. Hall has called attention to the influence of the sandstone im preserving the high ridges between the deep valleys of western New York, and also to their influence in producing cascades.* The entire thickness of the Portage group on the Genesee is estimated by Hall to be fully 1,000 feet. At the New York-Pennsylvania line it is thought by White to rise 475 feet above Lake Erie, but near the Pennsylvania-Ohio line it passes below lake level.“ Its outcrops in Erie County, Pa., are described by White as containing a succession of alternate ‘See Phinney: Eleventh Ann. Rept. U. S. Geol. Survey, Pt. I, 1891, p. 636. *W. W. Borden: Fifth Ann. Rept. Geol. Survey Indiana, 1873, pp. 150, 161, 172. ’ New York Geol. Survey, Fourth Geol. District, p. 225. *Second Geol. Survey Pennsylvania, Rept. Q*, 1881, p. 119. OUTLINE OF ROCK FORMATIONS. 59 layers of gray shale and thin layers of hard sandstone. Above the Portage in Erie County, Pa., is a shale formation about 225 feet in thickness to which White has given the name Girard shale, from Girard, Pa. It imme- diately underlies the typical Chemung formation and is regarded as a transition from the Portage to the Chemung. The Chemung group of western New York is described by Hall as con- sisting of a ‘series of thin-bedded sandstones or flagstones with intervening shales, and frequently beds of impure limestone resulting from the aggre- gation of organic remains.” Occasionally a coarse conglomerate appears as in the ‘“‘rock cities” near Salamanca and Panama, _N. Y. The name of the group is taken from the Chemung River, along which this group of rocks is finely displayed. The southern tier of counties in western New York is largely occupied by this formation, and it outcrops for a short distance southward in northern Pennsylvania. It forms the highest eleva- - tions in the eastern part of that region, attaining a height of about 2,500 feet above tide and 600 to 1,000 feet above the larger valleys which traverse it. At the western limits of the State the altitude of its surface has decreased to about 1,800 feet. The thickness of this group in the vicinity of the Chemung River was estimated by Hall to be not less than 1,500 feet, but it apparently decreases westward. There is some difference of opinion concerning the limits of the Chemung in northwestern Penn- sylvania, it being uncertain whether it should include the Venango oil sands. The area of outcrop of the undoubted Chemung in northwestern Pennsylvania is restricted to a narrow belt lying a few miles south of Lake Erie in Erie and northwestern Crawford counties and in the larger valleys of Warren and McKean counties. The Venango sands also have outcrops on ridges in the midst of the Chemung area and in a narrow strip on its south border. At the Pennsylvania-Ohio line the Chemung outcrop extends less than 20 miles scuth from the shore of Lake Erie. This formation constitutes the main part of the escarpment south of Lake Erie in north- western Pennsylvania and northeastern Ohio. The shales of northeastern Ohio as mapped by Read’ include the Venango sands of the Pennsylvania survey, as well as the undoubted Chemung and the transition beds between the Chemung and Portage 1Geology of Ohio, Vol. I, 1873, p. 483. 60 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. formations. The entire group here consists almost wholly of shale, there being few layers of hard rock so much as a foot in thickness. Because of this absence of hard rock the slopes are worn down to regularity and do not present the benches or abrupt changes characteristic of the eastward extension of the upper members of the group. The area of outcrop extends southward well toward the head of Grand River Basin in northern Trumbull County, but returns on the west side of that basi to within 10 miles of Lake Erie. It extends up Chagrin Valley to about Chagrin Falls, 20 miles from the Lake, and up the Cuyahoga Valley about 25 miles, or nearly to Peninsula. Aside from these exten- sions its outcrop from the Grand River Basin westward to the Huron River is but 5 to 15 miles wide, with an average of perhaps 10 miles. It extends northward beneath Lake Erie to an undetermined distance. The basin in which Lake Erie lies no doubt owes its existence chiefly to the soft and friable character of the rocks of this group. The thickness of the group near the south border of its outcrop south of Lake Erie is found to be about 950 feet at Elyria and 1,300 feet at Cleveland.’ It apparently becomes much thicker in passing eastward from Cleveland into Pennsyl- vania and New York. From near the mouth of Huron River, in Erie County, the belt of out- crop of this group turns abruptly southward, passing west of Norwalk, Galion, and Mount Gilead, and east of Delaware and Columbus. Below Columbus it occupies the Scioto Valley to the vicinity of Chillicothe and also for a few miles below Waverly. It appears also in valleys or narrow strips of lowland to the west of the Scioto, to and beyond the Ohio Valley. Its thickness, as reported by Orton, decreases from about 900 feet on the borders of Lake Krie to 450 feet in Crawford County, to 350 feet in Ross County, and to about 250 feet in Highland County. Throughout the entire line of outcrop from the Ohio River northward to Lake Erie, as well as eastward into Pennsylvania, this group consists almost entirely of soft shales. These have not resisted erosion as well as the overlying beds, and hence are found mainly in basins or at the base of hills. In this respect they are in contrast with the New York portion of the outcrop, which, as above noted, occupies some of the highest ridges and hills of the western part of that State. ‘See Orton: Geology of Ohio, Vol. VII, p. 24. OUTLINE OF ROCK FORMATIONS. 61 These shales also immediately underlie the glacial deposits in the north- western part of Ohio and neighboring portions of Michigan and Indiana. They are, however, covered to a depth of 100 to 500 feet, as the drift in that region is exceptionally thick. The rock surface is consequently very low, a considerable part of it being below the level of Lake Erie. The thickness of the shales is not so great as in the eastern district, being but, 100 to 150 feet in much of northern Indiana. Another line of outcrop of these shales in Indiana is found in a narrow strip leading from the Ohio River at New Albany, in a course west of north, across the State, crossing the White River below Indianapolis and the Wabash River above Lafayette. Near Monticello it swings westward and enters Illinois west of Kentland, Ind. Along this line also its surface has a low altitude, but it is covered throughout much of its length by heavy deposits of drift. The southern end is nearly free from drift and presents the appearance of a broad valley. The thickness of this belt of shale, like that of the one farther north, is only 100 to 150 feet, or even less. Waverly or Bedford shale—T"his is the lowest formation in the complex series to which the geologists of the first Ohio survey gave the name Waverly, a series which, in Ohio, embraces the entire interval between the Ohio shales and the Conglomerate Coal Measures. This series of rocks has given rise to much discussion, but seems now to be more closely allied to the Eoecar- boniferous than to the Devonian formations.’ The series between the Ohio shale and Conglomerate Coal Measures, as developed in Ohio, contains the following formations, given in order from older to newer: (1) Waverly or Bedford shale; (2) Berea grit and shale; (3) Cuyahoga shale; (4) Logan conglomerate; (5) Maxville limestone. In Indiana it is commonly known as the ‘‘Subearboniferous,” while in western Pennsylvania it was classed by I. C. White as the Subconglomerate series. It probably comprises much of the Catskill and Pocono formations of eastern Pennsylvania. White thinks it probable that the red Bedford shale and the Berea grit are of Catskill age. The Waverly shale includes not only the formation in southern Ohio, thus described by the Ohio survey, but also the Bedford shale of northern Ohio as defined by Newberry, with its included Euclid and Independence building stone. 'For a summary of the questions in dispute see Herrick: Geology of Ohio, Vol. VII, 1894, pp. 495-515. 62 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. A shale which is, perhaps, the equivalent of the Waverly is present in northern Indiana in greater thickness than in Ohio, the thickness as reported by Phinney being 143 feet at South Bend, 215 feet at Elkhart, and 200 feet at Goshen.’ The formation occupying the base of the Waverly series in southern Indiana is the Rockford (Goniatite) limestone. It may not, however, be the precise equivalent of the Waverly shale. Eastward from northern Ohio the Waverly shale changes from a blue- gray to a red color. It is thought by Carll to be developed only in a narrow belt in northeastern Ohio and northwestern Pennsylvania, and that mainly under cover of later rock formations.” Berea grit and shale (Catskill?).—The Berea grit, although but a few feet in thickness, is one of the most persistent and easily recognized formations in eastern Ohio and northwestern Pennsylvania. Concerning it Orton has remarked: ‘Its persistence as a stratum is phenomenal. Seldom reaching a thickness of 50 feet, its proved area in Ohio, above ground and below, is scarcely less than 15,000 square miles, and beyond the boundaries of Ohio it appears to extend with certainty and strength unbroken into at least four adjacent States.”* The name is taken from Berea, in northern Ohio, where it is extensively quarried. It constitutes the ‘‘Waverly quarry stone” of southern Ohio. It has had considerable influence in producing cascades in northern Ohio. In both the exposed and the covered portion it consists of a sandstone of medium coarseness, which in northern Ohio includes a thin pebble bed. Above the Berea grit is a dark shale 15 to 20 feet in thickness, which has been reported by Orton to form a constant cover throughout its entire extent in Ohio. It is usually sharply in contrast with the blue beds of the overlying Cuyahoga shale, but from Cuyahoga County eastward the line of separation is in places not easily traced. Cuyahoga shale (part of Pocono sandstone of Pennsylvania) — his formation, which in Ohio has a thickness of 150 to 400 feet, receives the name Cuyahoga from extensive outcrops along the Cuyahoga River. It constitutes the main member of the Waverly series, though the Logan conglomerate of central and southern Ohio rivals it in strength. It consists, in the main, of light- ‘Eleyenth Ann. Rept. U.S. Geol. Survey, Pt. I, 1891, p. 638. * Second Geol. Survey Pennsylvania, Rept. I’, 1880, map, p. 92; discussion, pp. 96-97. * Geology of Ohio, Vol. VII, p. 28. OUTLINE OF ROCK FORMATIONS. 63 colored, blue or gray shales, but carries occasional thin beds of sandstone. In southern Ohio, notably in Ross, Pike, and Scioto counties, the sandstone beds become more prominent. The sandstone is extensively quarried at Buena Vista, on the Ohio River, a few miles below Portsmouth. There are also developments of sandstone in northeastern Ohio, notably in Trumbull County, where numerous quarries have been opened. Its outcrop usually covers a width of several miles. From the Ohio River northward to Chillicothe the Cuyahoga shale outcrops on both sides of the Scioto River, but north of that city it lies east of the river and forms the east border of the Scioto Basin. It outcrops in a narrow strip south of Lake Erie from Lorain County eastward to Geauga County, but there swings southward around the head of Grand River Basin. In northwestern Pennsylvania this formation, under the name of Pocono sandstone and Crawford shales, covers the uplands in a belt 10 to - 15 miles wide in Crawford and southeastern Erie counties and extends southeastward along the lowlands into Mercer and Venango counties. It forms much of the surface in the northern half of Warren County and extends southward along valleys and low parts of the upland beyond the limits of that county. It outcrops only on a few ridges in southwestern New York. This formation apparently constitutes the lower part of the Knobstone group of Indiana, so well developed on the west border of the Cincinnati arch. It there forms the slopes of the prominent escarpment west of the trough occupied by the Devonian shale, but it lies mainly outside the limits of the region under discussion. Logan conglomerate (part of Pocono sandstone of Pennsylvania. —The Logan conglomerate is well developed from Wayne County, Ohio, southward into Kentucky, but seems to be feebly developed or wanting in the vicinity of the Cuyahoga Valley. It is characterized at two horizons by a conglomerate which carries small pebbles. The conglomerate phase is not so conspicuous in southern as in central Ohio, and in the latter district occupies only a small part of the formation, there beimg fine-grained sandstones and even shales embedded with the conglomerate. The average thickness of the Logan conglomerate group is about 200 feet, but the maximum is much above the average, reaching probably 400 feet. The resistance of this conglomerate 64 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. to erosion has produced a marked effect upon the contours of the valleys, causing, in some instances, notable constrictions, as shown below. This formation constitutes part of the Knobstone of Indiana. The name Knobstone, there as well as in Kentucky, arises from the topographic features resulting from its persistence as a protective capping on the sum- mits of the ridges and hills. The knobs of southern Indiana rise abruptly 300 feet or more above the shale lowland to the east. Above the Logan conglomerate there is a local development of lime- stone in south-central Ohio, which was classified by: Prof. EK. B. Andrews, from a study of fossils, as an equivalent of the Chester limestone of Illinois and Missouri, or the latest of the Eocarboniferous series. It is known as the Maxville limestone, from a locality in Perry County, and is probably best displayed on Jonathan Creek in Muskingum County. It has a thick- ness of only a few feet and the outcrops are mainly on valley slopes. Pottsville, or Conglomerate Coal Measures—'["he series of formations in which the coal seams are embraced are found in a large basin extending from northern Pennsylvania and northeastern Ohio southward to eastern Tennessee. The Ohio River traverses the northern half from Pittsburg, Pa., to Marietta, Ohio, below which it bears toward the western margin of the basin and leaves it a short distance above Portsmouth, Ohio. The area covered by these formations in Ohio is estimated by Orton to be about 10,000 square miles, or about one-fourth the area of the State. Pennsylvania and West Virginia each have an area about as extensive as that of Ohio. A few square miles im southwestern New York, chiefly in the portion of Catta- raugus County south of the Allegheny River, fall within the limits of this basin. By reason of being in a basin which was in process of filling, the lowest members appear on the Borders, while the highest are found in its interior portion. _At the base of these formations there is found a series of conglomerates and sandstones with thin beds of shale and limestone, and with local developments of coal, to which the general name Conglomerate group has been applied. In the Pennsylvania reports it has the names Seral con- glomerate and Pottsville conglomerate, and constitutes No. XII of the rock series of that State. Allegheny, or Lower Productive Coal Measures.— Next above the series of conglomerates and sandstones just discussed come the Lower Productive Coal Measures, which have a thickness about as great as the entire Conglomerate group. OUTLINE OF ROCK FORMATIONS. 65 They carry not fewer than nine workable coal seams in Pennsylvania and six well-defined seams in Ohio These are thrown into three groups, known as the Clarion, the Kittanning, and the Freeport, each of which in Pennsyl- vania carries three coal seams. The outcrops are around the borders of the coal basin, but the formation probably underlies the interior portion. Conemaugh, or Lower Barren Coal Measures Above the Lower Productive Coal Measures there are 300 to 600 feet of sandstones and shales in which the few coal seams that appear are thin and wanting in persistency. For this reason, and because of a similar series at a higher horizon, they are known as the Lower Barren Measures. One coal seam, the Mahoning, is worked in Columbiana County, Ohio. These barren measures outcrop extensively in southeastern Ohio at a distance of 30 to 50 miles back from the Ohio River, but come to the border of the Ohio Valley in eastern Ohio and western Pennsylvania. Monongahela, or Upper Productive Coal Measures— I'he [ower Barren Measures are overlain by the Upper Productive Coal Measures, which carry the widely known Pittsburg coal (the most valuable seam of this great field), and a less important seam, known as the Meigs Creek coal. The thickness of these measures has been estimated by Orton to be 250 to 300 feet, though the upper limits are not well defined. The extent is much greater than the limits of the productive portion of the Pittsburg coal. Dunkard beds (Permian?) —Above the Upper: Productive Measures there is a formation which attains, where best developed, a thickness of several hundred feet, and which has long been known as the Upper Barren Coal Measures. But since the fossil plants of this formation are of Permian rather than Coal Measures type, the formation can scarcely be retained as a part of the Coal Measures. The name Dunkard, taken from a creek in southwestern Pennsylvania, where the beds are well developed, has been substituted for the former name. This formation, as interpreted by Orton, covers only a small area in Ohio, being confined chiefly to Belmont and Monroe counties, but it occupies a large area in West Virginia between the Ohio and Monongahela rivers, and encroaches slightly on southwestern Pennsylvania. This is apparently the newest rock formation in the region under dis- cussion. Only the residuary clays and a few beds of gravel at high levels are present to bear witness to the several long periods that intervened between Carboniferous and Glacial times. MON XLI —) CHAPTER TE PHYSICAL FEATURES. ALTITUDE. If the basin of Lake Ontario be included, the altitude of the glaciated portion of this region has a range of about 3,000 feet, the lowest part of the Lake Ontario Basin being nearly 500 feet below sea level, while the highest ridges on the Allegheny Plateau are fully 2,500 feet above the sea. This range is found within a distance of about 100 miles. The shore of Lake Ontario stands about 250 feet above tide, the level of the lake ranging from 244.5 to 249 feet, thus reducing the variations of the exposed land surface to about 2,250 feet. The areas embraced between 5UV0-foot contours are approximately shown on PL. I. This region attains its highest altitude in the vicinity of the headwaters of the Allegheny and Genesee rivers, in Potter and McKean counties, Pa., and Allegany and Cattaraugus counties, N. Y. These counties include nearly all the area that rises above 2,000 feet, though there are a few square miles in the adjacent portions of Warren County, Pa., and Chautauqua and Wyoming counties, N. Y., which rise above that elevation. It will also be observed that the portion of this region rising above 1,500 feet is confined almost wholly to the States of New York and Pennsylvania, there being scarcely 1 square mile of Ohio that is known to rise above this height, while the highest points of Indiana are only about 1,250 feet. The 1,000-foot contour embraces all of western New York and northwestern Pennsylvania except the lowlands that border Lakes Ontario and Erie and a few of the deep valleys. This contour also embraces much of the eastern half of the State of Ohio; also large areas in the western half. The main areas standing below 1,000 feet are the Grand River, Scioto, and Maumee basins and a large part of the watershed of the Great Miami River. In Indiana a small area in the northeastern part and a larger area in the eastern part rise above 1,000 feet. With these exceptions only a few isolated ridges and hills, chiefly in the southern part of the State, rise above that contour. The 66 ALTITUDE AND TOPOGRAPHY. 67 greater part of Indiana and large areas in Ohio fall between 500 and 1,000 feet. The only portions of the region falling below 500 feet are a narrow strip in New York, on the south border of Lake Ontario, and a portion of the valley of Ohio River and the lower courses of its tributaries in southern Ohio and Indiana. Near New Albany, Ind, the 500-foot contour recedes a few miles from the Ohio River into the lowland formed in the Devonian shale, but returns to the river just below that city. TOPOGRAPHY. In the description of the rock formations it was shown that all the earlier formations from the Trenton eroup up to the Hamilton contain a large amount of limestone and easily disintegrated shale, while the later formations contain very little limestone, and often are made up largely of resistant sandstone, This difference in constitution and texture has resulted in a marked difference in topography. The formations which contain a large amount of limestone or soft shale have become broken down to a markedly lower elevation and a more even surface than the resistant sandstone. The sandstone or hilly country, being mainly on the borders of the Appalachian Mountain system, occupies the southeastern part of the region under discussion The border between it and the lower plain underlain by shale and limestone may be roughly indicated as follows: From the Genesee Valley at Mount Morris it takes a westward course, passing a few miles south of Batavia and Buffalo, N. Y., to Lake Erie It follows the lake border southwestward to the vicinity of Cleveland, Ohio, lying usually but 5 to 10 miles south of the lake, though at the Grand River Basin in northwestern Ohio it extends southward about 40 miles. A short distance west from Cleveland the hills bear away from Lake Erie to the vicinity of the continental divide in Medina, Ashland, and Richland counties. From near Mansfield in Richland County the border turns southward and main- tains this course for nearly 100 miles, constituting the eastern rim of the Scioto Basin. It then swings westward across northern Ross County, passing a short distance north of the city of Chillicothe, and enters the northern part of Highland County. Here it again turns southward and passes through Highland and Adams counties into Kentucky, crossing the Ohio River near the mouth of Brush Creek, a few miles above Manchester, Ohio. On the borders of the Ohio the plain is so dissected as to appear less 68 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. strikingly in contrast with the hills than in districts farther north, yet the regular crest lines of the dividing*ridges are a rather striking feature even there. The plain extends westward across the Cincinnati arch into Ken- tucky, Ohio, and Indiana, to the Knobstone formation of southern Indiana and northern Kentucky. It covers northern Kentucky, northwestern Ohio, and the southern part of Michigan, and thence stretches westward far beyond the Mississippi River, constituting the great interior plain of the United States. In both the plain and the hilly country there are variations in topog- raphy which need to be considered in some detail. The hard and resistant rocks of the plain country stand in relief as escarpments or, m some cases, as low dividing ridges, while those of the hilly country remain as elevated divides between drainage lines or occasionally as island-like outliers. The glacial deposits have greatly concealed the topography of the rock forma- tions and disturbed the old systems of drainage. In the plain portion of the region the old valleys have been so greatly filled that they can be traced only in limited districts. In the hilly portion the drift seldom fills up the lowlands to the height of the uplands or ridges, yet it obscures the old drainage lines to a great degree. The present discussion is naturally devoted chiefly to the eastern part of the region, where the old topography is least concealed. Inasmuch as the topographic features depend largely upon the rock formations, they are to some extent discussed in belts that follow the outcrops of the formations. The plain south of Lake Ontario in western New York is first discussed, and then the region lying southward and westward, comprising the later formations, is described. LOW PLAIN SOUTH OF LAKE ONTARIO. The low country south of Lake Ontario in western New York is separable into three distinct plains, with two escarpments above the level of the lake shore. These features are in part represented on Pl. III. The first or lowest plain extends from the lake southward to the Niagara escarpment, a distance of 6 to 12 miles; the middle plain extends from the Niagara to the Corniferous escarpment, a distance of 10 to 15 miles; while the highest plain extends from the Corniferous escarpment southward to the base of the hilly country, with a width averaging less than 10 miles. These plains are underlain by shale formations, except for a short distance er f , i 1 i 7 nine : at Ne ae ae ee > aa NOE aa AT TEE ee on ee ‘oe ; ne, t. Rect ted pa ss FS oeehlanes 4 sete a Ag vebyenses ane + ait ae : EE ROLER “ us Li Lx . Li ty ICT BETWE | By Fraj uy a, a ae Ve q A % Py ieee Ee 4 =e 2 Se — w . 75° Si Gant Fx MONOGRAPH XLi PL I f - U.S GEOLOGICAL SURVEY : , : : : : : | aoa | . _ eee |g ——_—— ; oth, : A—t1|. ted ‘ I sal Hone] > Z LEGEND | Asie A a Mo P in ee “ a_ | | aiwan aii \ | o's ~ Y 4 eo ] AA i TN a : E : N t= od i | 7 ? i H) ae | Tosti Lake Tnxjucis i : : the : lak ik murs | Ne ? Py I Y ~_—_ =~ se i‘. a a FH GMAN) ) sigh Pos v7 " / Sey cal ye ) ¥ clin SYP Hgeevay J = ty ‘ J f ‘ iti Y 3 wT aoa Vise tie Ky ae : ce N= AMO eS in oN — ae RT oy 7 ol a aE ape 7 .

3 aa a (ule Ohya lon cle X Levey a . ROCK ISLANDS IN OHIO VALLEY. 85 mile. Like Monument Hill, it is separated from the uplands east of the river by a narrow channel, less than half a mile in average width, with a gravel filling that extends down about to river level. The cause for the excavation of a double channel at this place is not yet apparent. Opposite the mouth of Middle Island Creek, which enters the Ohio at St. Marys, W. Va., a rock island is found on the Ohio side which stands about 300 feet above the river. It is separated from high land on the north by a channel about one-third of a mile in width, whose surface is only 50 to 60 feet above the river, and is still utilized at extreme high water. It is probable that this island has been cut off from the uplands on the north by the encroachments of the Ohio River. The stream is now encroaching upon the east side of the island, and it appears formerly to have made an ox-bow curve, which encroached on its west side. At the mouth of the Little Kanawha River, at Parkersburg, W. Va., there is a rock island which stands about 180 feet above the river. It is separated from the east bluff by a gravel-filled valley about one-half mile wide, whose surface is 75 to 80 feet above the river. The width of this channel is only one-third as great as that occupied by the Ohio west of the island, but about the same as the valley of the Little Kanawha south of the island, and it may have been excavated by the latter stream. Well data suggest, though they are not full enough to demonstrate, that the abandoned channel has a lower rock floor than the present channel of Little Kanawha. This being the case, the island has probably been cut off from the upland south of the Little Kanawha River. Encroachments, either by the Little Kanawha or by the Ohio, may have opened a passage for the present course of the stream. An island or irregular group of hills in the north part of Cincinnati, known as Walnut Hills, stands 800 to 400 feet above the river and sepa- rates a broad abandoned channel on the north from the narrower present valley of the Ohio on the south (see Pl. V). At the west it is bounded by Mill Creek Valley. The Walnut Hills island apparently once had connec- tion with the uplands south of the Ohio, between the Licking and Ohio rivers, but through a diversion of the Ohio has been separated from thosé uplands. In this connection it may be remarked that the old Ohio appears to have taken a northward course from Walnut Hills to the Great Miami near Hamilton, Ohio, and to have received the Licking through the lower ‘ 86 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. course of Mill Creek (reversed), along the west border of Walnut Hills. The triangular tract lying between Mill Creek, Great Miami River, and Ohio River, and comprising several townships of Hamilton County, Ohio, is also surrounded by stream channels as completely as Walnut Hills, and apparently for the same reason, the present course of the Ohio from the mouth of Mill Creek to the mouth of the Great Miami being comparatively new. This matter is discussed more fully later (pp. 116-118). A few miles below the mouth of the Great Miami River a rock island appears on the Kentucky side, and rises about 200 feet above the river. It is separated from the east bluff by a channel nearly one-fourth mile in , width which stands scarcely 100 feet above the stream. Well data indicate that its rock floor is above river level. The island seems to have been cut _ off from the east bluff by the Ohio, probably because glacial deposits filled the main channel sufficiently to give the stream opportunity to flow on each side of the land which forms this island. These deposits filled the main channel in that vicinity to a height of 150 to 200 feet above the stream. . Immediately above the mouth of the Kentucky River, and back of the city of Carrollton, Ky., there is an island or prominent group of hills stand- ing 200 to 300 feet above the Ohio, and now separated from the uplands to the east by a gap one-half mile wide that has been filled with glacial deposits to a height of 100 to 150 feet. This separation was probably effected by the encroachments of the Ohio and Kentucky rivers. The gap is much narrower than the valley of either the Ohio or the Kentucky, and this seems to indicate that it is not an old line of drainage. Just below Madison, Ind., there is a rock island nearly 300 feet in height, separated from the north bluff by a channel only half as wide as the present stream. This channel, though now above the reach of the river, may have been utilized down to comparatively recent times. The’ opening of the channel was perhaps begun by a small tributary of the river which now enters just above the island, but a fully satisfactory interpreta- tion has not been made. Some of the most conspicuous of the island-like uplands are found where the Ohio leaves the resistant conglomerate Coal Measures and enters the friable Coal Measures. ‘These are well shown on the Owensboro topo- graphic sheet (Pl. VI, in pocket), and have been discussed in some detail ROCK ISLANDS IN OHIO VALLEY. 87 by Veatch." From Rockport the maim channel, with a width of 24 to 4 miles, takes a southward course to Owensboro, while a narrower channel, known as Lake Drain or Lake Plain, leads westward and connects with the lower course of Little Pigeon Valley through a channel which is reduced at its narrowest ‘place to a width of about two-thirds of a mile. The island inclosed by these two channels and the lower course of Little Pigeon Creek rises barely to the 500-foot contour, while the Lake Drain channel falls slightly below 400 feet. The river at Rockport is about 345 feet at low water, or only 50 feet below this channel, while at the highest floods it passes through the channel. Another much smaller island, known as the Bon Harbor Hills, appears on the Kentucky side of the river west of Owensboro, and stands in the midst of the broad valley. It rises slightly above the 500-foot contour. The channel back of it falls a little below the 400-foot contour, having very nearly the same altitude as the Lake Drain channel. There is some uncertainty as to the interpretation of this peculiar drainage. The Bon Harbor Hills are separated from uplands on either side by such broad channels, their width in each case being nearly 3 miles, that this hilly tract seems likely to have been an isolated one for a long period. But the hills back of Rockport appear to have become separated in comparatively recent times from the uplands to the north. Possibly the separation took place atter the partial filling of the Ohio Valley with loess. It will be observed that the local divides are broken down in that vicinity to an altitude so low that but a slighigpmount of valley fillmg would be necessary to make it possible for a stream to be diverted across them. There are several island-like tracts along the borders of the Ohio Valley west of the limits of the Owensboro quadrangle, one of which, near Shawneetown, Illinois, is as conspicuous as either of the tracts shown in this quadrangle, but the majority are low and of small area. The history of their development is not as yet understood. This somewhat hasty sketch of the present valley leaves untouched a number of important features which throw light upon the development of this great river, and these will now be considered. The several antecedent drainage systems are taken up m order, beginning with the Upper Ohio and passing westward to the lower course of the river. 1Arthur C. Veatch: Jour. Geol., Vol. VI, 1898, pp. 257-272. 88 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. UPPER OHIO OR OLD MONONGAHELA SYSTEM. THE OLD DIVIDE. For some years it has been considered highly probable that the Ohio has been thrown across an old divide somewhere on the projecting portion or “Panhandle” of West Virginia, but the precise position of the divide has remained in question. It has also been held as probable that the portion of the Ohio above this supposed divide, together with the Monongahela and the lower part of the Allegheny, had their former discharge northward, along a line leading through the Beaver and Grand river valleys of western Pennsylvania and northeastern Ohio, to the basin of Lake Erie, forming what has been aptly termed the old Monongahela system of drainage, the Monongahela being the main affluent.’ The apparent extent of this old drainage system is indicated in fig. 1. The portion of the Ohio Valley in the 80 miles along the Panhandle and for 50 miles farther down receives no large tributaries, the sources of the streams, from both Ohio and West Virginia, being usually within 25 to 30 miles of the river. This feature of itself should arouse suspicion that this tract has been the headwaters of old drainage systems. An examination of the altitudes of its bluffs and of the bordering uplands confirms the suspicion, for they are found tu be higher than the bluffs and the uplands bordering the Monongahela to the east and the Muskingum to the west, and 1 The following reports and papers discuss or touch upon this lect: Discovery of the preglacial outlet of the basin of Lake Erie into Lake Ontario, by J. W. Spencer: Second Geol. Survey Pennsylvania, Rept. Q‘, 1881, pp. 357-406, especially pp. 387 and 405-406. Same paper appears in Proc. Am. Philos. Soc., Vol. XIX, 1882, pp. 300-337. Preglacial drainage and recent geologic history of western Pennsylvania, by P. Max Foshay: Am. Jour. Sci., 3d series, Vol. XL, 1890, pp. 397-403. Pleistocene fluvial plains of western Pennsylvania, by Frank Leverett: Am. Jour. Sci., 3d series, Vol. XLII, 1891, pp. 200-212. Further studies of the drainage features of the Upper Ohio Basin, by T. C. Chamberlin and Frank Leverett: Am. Jour. Sci., 3d series; Vol. XLVII, 1894, pp. 247-283. Origin of the high terrace deposits of the Monongahela River, by I. C. White: Am. Geologist, Vol. XVIII, 1896, pp. 368-379. ; Descriptions of terraces in that region may be found in the following reports and papers by J. J. Stevenson: Second Geol. Survey Pennsylvania, Repts. K, 1876, pp. 11-19, and K*, 1878, pp. 251— 263; Am. Jour. Sci., 3d series, Vol. XV, 1878, pp. 245-250: Proc. Am. Philos. Soe., Vol. XVIII, 1880, pp. 283-316. Also in the following reports and papers by I. C. White: Second Geol. Survey Penn- sylvania, Rept. Q, 1878, pp. 9-17; and Rept. Q’, 1879, pp. 10-20; Am. Jour. -Sci., 3d series, Vol. XXXIV, 1887, pp. 374-381; also discussions of drainage features incorporated in the detailed geology of the several counties of western Pennsylvania covered by Repts. Q, Q’, Q°, and Q+ of the Second Geol. Survey Pennsylvania. UPPER OHIO DRAINAGE SYSTEM. 89 yet are located in similar rock formations. The uplands also show an increase in height in passing down the Ohio from western Pennsylvania to the southern end of the Panhandle near New Martinsville, W. Va., the altitude of local divides between the tributaries in western Pennsylvania being about 1,300 feet, with occasional points 1,400 feet within a few miles back from the river, while in the vicinity of New Martinsville the divides attain an altitude of fully 1,400 feet on the immediate borders of the river and about 1,600 feet within a few miles east. Below New Martinsville the alti- tude declines rapidly, falling to 1,000 feet or less in the 50 miles to Marietta. ‘The trend of the tributaries also suggests a reversal of drainage along the Panhandle. From the most. ele- vated parts, near New Martinsville, northward to the end of the Panhandle, they show a decided tendency to point up the valley at their junction with the Ohio, as may be seen by reference to fig. 2. If, therefore, attention were given simply to altitudes of bordering uplands and to the trend of the tributaries of ; the Ohio, the old divide would be ee located near New Martinsville. It was 6 5 r $ Scale of miles from these criteria that this location of eStore goss g the divide was suggested by Chamber- lin and the writer in 18942 While Fic. 1.—Probable preglacial drainage of the Upper Ohio this still appears to have been an early ORES Taira ee divide, subsequent study of the gradation plains and valley deposits has led to the impression that the divide had migrated before the establish- ment of the present drainage. The gradation plains along the Panhandle show an exceptional intricacy. Instead of a single prominent system of gradation plains, such as is commonly displayed in the Upper Ohio region, ' Am. Jour. Sci., 3d series, Vol. XLVII, 1894, p. 253. 90 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS... there are rock shelves and remnants of old valley floors on the border of the Ohio at all levels from about 1,050 feet above tide down to about 0. 5 Statute Miles E.Liverpool, = a Ser St Clairsville (t <9 an Bellaire 4\°Ben\yood. Fic. 2.—Map of part of the Upper Ohio drainage system near the supposed old diyide. 800 feet. The full correlation will involve more accurate measurements and a closer study of rock textures and other features than has yet been UPPER OHIO DRAINAGE SYSTEM. $)il attempted. The writer can at best present only an imperfect and tentative interpretation. The features may perhaps be best discussed by beginning at New Martinsville, where the divide was first located, and passing from there up the Ohio to the mouth of the Beaver. Although the trend of the tributaries and the high altitude of bordering -uplands near New Martinsville suggest that the divide at one time stood near the site of that village, it evidently had become shifted to the north when the best-defined system of gradation plains of that region was formed. Fishing Creek, which enters from the southeast at New Martinsville, and Fish Creek, which enters from the east 14 miles farther up the Ohio, have a well-defined gradation plain which is in harmony with that on the portion of the Ohio below New Martinsville, and which is too low to permit of northward discharge. On Fish Creek at Littleton, W. Va., about 30 miles from the Ohio, the gradation plain stands only 930 feet above tide, while at the mouth it is not far from 825 feet. On Fishing Creek observations were made only near its mouth; the gradation plain there is about 800 feet above tide, and this plam is found to continue down the Ohio with gradual descent. The first place above New Martinsville where features occur that suggest a change or disturbance of drainage is at the series of sharp curves in the Ohio Valley below Moundsville, W. Va., 8 to 12 miles above the mouth of Fish Creek, where the stream describes a letter S in its curves. But these curves do not seem to be accompanied by any features that make evident the crossing of an old divide. The height of the bluffs does not appear to differ from that of neighboring parts of the valley above and below; the width of the valley is also as great as the average width in that region. Furthermore, just above Moundsville, on the east side of the Ohio, a rock shelf capped with gravel appears at an altitude about 250 feet above the river, or 850 to 860 feet above tide, which seems to fit in well with the gradation plains farther down the valley. There is, however, one feature which seems to suggest a divide below Moundsville. There is a remarkably high gradation plain on Grave Creek, a tributary which enters at Moundsville from the southeast. Its altitude at Easton, only 8 miles from the Ohio, is 1,017 feet above tide, as estimated from the railway station, and it is capped by a deposit of gravel several feet in depth. Four miles below and almost in sight of the Ohio 92 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. its altitude by aneroid is 975 feet, or 125 feet above the system that has been traced up to this point along the Ohio. Probably it belongs to an older stage of drainage development, and perhaps to a north-flowing system. If the latter be true these curves in the Ohio are probably at the place where an old divide has been crossed or a piracy in favor of the western system had taken place. This question may perhaps be considered to better advantage after features farther up the Ohio have been discussed. On the tributaries which enter above Moundsville, and also along the bluffs of the Ohio, rock shelves which appear to be remnants of old grada- tion plains are conspicuous at much higher levels than have been noted farther down the stream. The highest have an altitude of about 1,050 feet, and others about 1,000 and 960 to 975 feet. The altitudes here given pertain to the part of the valley near Wheeling, just above Moundsville. Farther north they become lower, being between 965 and 870 feet at the mouth of Beaver River. The remnants above 1,000 feet are not so con- spicuous as those at about that level or slightly lower. As the series declines from south to north it seems probable that the gradation plains are the product of a northward-flowing drainage line which had deepened its valley to about 965 feet at Bellaire and Wheeling before reversal took place. The gradation plain near these cities, which stands at about 1,000 feet, probably connects at the mouth of the Beaver with one standing about 965 feet above tide, and at intermediate points includes the 990-foot terrace on Buffalo Creek back of Wellsburg, and the 975-foot terrace on the borders of the Ohio near New Cumberland, W. Va. The gradation plain which stands at about 965 feet opposite Bellaire and Wheeling probably connects with the 870-foot terrace at the mouth of the Beaver, and includes the 960-foot terrace at the mouth of Short Creek and the 925-foot terrace at the mouth of Yellow Creek. Probably the north-flowing system had cut down far enough before reversal took place to form a terrace south of Wellsburg which stands at about 930 feet and a terrace of similar height near the mouth of Cross Creek, south of Steubenville — 1Tt should be remembered that nearly all of these measurements of terraces have been made with a barometer, and are consequently only approximations to the real altitudes. The elevations at neighboring points may differ a few feet less or a few feet more than these figures indicate. In the case of the terrace in the northern part of Wheeling the writer had opportunity to compare an aneroid reading with an accurate survey made for the Wheeling Terminal Railway, which has tunneled beneath this terrace, and found that the difference was only 9 or 10 feet; the altitude given by the railway survey being 992 feet, and by the barometer 1,001 or 1,002 feet. UPPER OHIO DRAINAGE SYSTEM. 93 From an examination of these gradation plains it appears probable that the divide between the old systems was somewhere south of Bellaire at the time the present Ohio was formed. Whether it was between Bellaire and Moundsville or at the curves of the Ohio below Moundsville may not be easy to determine. There are features which suggest that it may have been within 2 miles south of Bellaire, at the place where the high ridge south of McMahons Creek comes to the river bluff from the west. A similar high ridge sets in on the east bluff, separating Boggs Run, a north- flowing stream, from Cemetery Run, a south-flowing stream, and leads thence eastward to form the local divide between Wheeling and Grave creeks. Within 2 or 3 miles of the river this ridge attains an altitude of 1,350 to 1,400 feet, and is nearly 1,200 feet at the river bluffs. In addition to its prominence, there is also a difference in drainage features on opposite sides of the ridge, which may favor the view that it constituted an old divide, though not necessarily a very long-continued one. South of the ridge the uplands generally show a greater dissection than to the north, such as would result from connection with the system of drainage to the south, which, as shown by the gradation plains of Fish and Fishing creeks, is more than 100 feet below that of the gradation plains immedi- ately north of this ridge. There is, however, south of this ridge the gradation plain on Grave Creek, which stands so high as to suggest that it once belonged to the north-flowing system. There is also the fact that the Ohio Valley is exceptionally large just below this ridge, as if the strata there were very weak in their resistance to erosion. In the present state of knowledge, therefore, it can scarcely be decided whether the divide at the time the Ohio was established was at the ridge above Moundsville or at the curves in the Ohio below that city. Possibly it stood for a time at the curves below Moundsville, and was shifted by stream piracy to the ridge above that city. Indeed, as previously indicated, the divide may have migrated northward, through stream piracy, from the elevated country near New Martinsville to the points in question. An inspection of the map will show that Moundsville seems to be in the midst of an old drainage system, rather than at an old divide. ‘To place a divide there certainly gives to the section between Moundsville and New Martinsville the appear- rance of a truncated drainage system, but to place the divide near New Martinsville, either above or below Fishing Creek, gives a natural appear- \ 94 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. ance to both the northeast and the southwest system, and assigns to piracy no more than might be expected of it, in view of the fact that the southwest system was at least 100 feet the lower. In the portion of the Ohio Valley between Moundsville arid the mouth of the Beaver there are very few rock shelves or remnants of old fluvial plains at levels below those which appear to belong to the old north-flowing system, but on the tributaries rock shelves are present at all levels as incidents of the cutting down of their valleys. The general absence of rock platforms or terraces along the main valley may be assigned to the increased volume of the united stream. The most conspicuous of the rock terraces formed after reversal is found north of New Cumberland, W. Va. It stands about 100 feet lower than any of the gradation plains of the north-flowing system in that vicinity, being only 200 feet above the river and 835 feet above tide. It is preserved for a distance of nearly a mile with a width of 30 to 40 rods, and carries a few feet of gravel on its sur- face. In gullies which cut into this gravel Unio shells in large numbers secur, which have the weathered appearance to be expected if they are native to this old river bottom.’ The gravel was evidently deposited by a stream flowing southward in the present direction of the Ohio, for it con- tains material of glacial derivation brought down from the glaciated districts to the north. | THE NORTHWARD OUTLET. The question of a northward outlet for the Upper Ohio, Monongahela, and much of the Allegheny drainage through the Beaver was raised by Spencer nearly twenty years ago, being presented as a working hypothesis in connection with a general discussion of the origin of the lower Great Lakes.” Evidence in support of this hypothesis was brought forward by Foshay in 1890.* He called attention to the great breadth of the main gradation plain on the Beaver, to the apparent northward slope of the rock floor, and to the occurrence of potholes on this rock floor which appear to have been formed by a north-flowing stream. His discussion was limited 1 For notes on the occurrence of Unio shells on a terrace of the Monongahela at a similar height above the stream, see Stevenson’s paper in Am. Jour. Sci., 3d series, Vol. XV, 1878, pp. 245-250. 2Proc. Am. Philos. Soc., Vol. XIX, 1882, pp. 330-337, with maps; also published as an appendix to Rept. Q* of Second Geol. Survey Pennsylvania, 1881, pp. 357-406. See pages 387 and 405-406 for this reference. Am. Jour. Sci., 3d series, Vol. XL, 1890, pp. 397-403. UPPER OHIO DRAINAGE SYSTEM. 95 mainly to the southern end of the Beaver Valley, since the gradation plain there is but little obscured by glacial deposits, though the interpretation of northward drainage was extended to the Lake Erie Basin by way of the Mahoning and Grand River valleys, and was applied to the rock floor beneath the present stream as well as to the high-level terraces. Soon after the publication of this paper the present writer discussed the nature of the evidence and dissented from that part of the interpretation which assigned a northward drainage for the channels that are buried beneath the present streams,’ while admitting the force of the evidence of the high terraces in favor of northward drainage. In a paper prepared in 1894, Chamberlin and Leverett? discussed this outlet, together with other features in the Upper Ohio region. The evidence was thought to favor a northward discharge through the Beaver prior to the excavation of the deep trench in which the lower portion of the river now flows, but the interpretation of northward drainage through buried channels was shown to be incorrect. ' Two years later I. C. White discussed this outlet in connection with a paper on the terrace deposits of the Monongahela River; he considered it a ‘pretty surely established” line of discharge; but, like Chamberlin and Leverett, he restricted the northward discharge to a time previous to the opening of the deep trenches of that region.’ Turning to the Beaver outlet, we find that a gradation plain a mile or more in average width extends the whole length of the Beaver River and descends northward from about 870 feet at the mouth to about 810 feet at the head of the river, or a fall of 60 feet in a distance of 25 miles in the reverse direction from the present flow of the stream. From the head of the Beaver, at the junction of the Mahoning and Shenango rivers. the grada- tion plain does not maintain so great a breadth, on either the Mahoning or the Shenango, as that presented by the Beaver. On the Mahoning, which is the line of continuation suggested by Spencer and adopted by Foshay, the breadth is reduced near the Pennsylvania-Ohio line to less than one-third of a mile, and the bordering uplands there become very prominent, with an altitude of about 400 feet above the river. On the Shenango there is a tAm. Jour. Sci., 3d series, Vol. XLII, 1891, pp. 200-212. *Tdem, Vol. XLVII, 1894, pp. 247-283. 5 Am. Geologist, Vol. XVIII, pp. 368-379, December, 1896. 96 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. similar constriction at the very mouth of the river, just below Newcastle. Hills 300 to 400 feet in height are separated by a channel scarcely one- third of a mile wide at the level of the river, which is not far from the level . of the gradation plain. Between these two valleys there is an abandoned channel leading north from the Mahoning at Edenburg, Pa., to the Shenango at Harbor Bridge, 4 miles above Newcastle, and this is a little wider than either of the other channels, though only about half as wide as the gradation plain on the Beaver. The continuation of the channel northward up the Shenango is in a valley one-half to three-fourths as wide as that of the Beaver gradation plam. From the Shenango at Sharon, Pa., there is an abandoned channel running westward to the Mahoning at Youngstown, Ohio, from which point a broad valley opens northwestward into the Grand River Basin, and this in turn opens into the Lake Erie Basin. Since the constricted portions of the Mahoning and Shenango valleys may appear to oppose the hypothesis of a discharge of the old Monongahela system through them, they will be considered before the routes just out- lined are discussed. From descriptions given by White’ it appears that the rocks forming the Carboniferous conglomerate measures are exceptionally soft for a few miles along the Beaver Valley, below the junction of the Mahoning and the Shenango, where the gradation plain is broadest, but contain firm and resistant beds of considerable thickness in the constricted part of the Shenango in the vicinity of Newcastle, and also on the Mahoning at its constricted part near the State line. These beds are also very firm and resistant on the Beaver in the vicinity of Homewood, but they dip rapidly southward and soon pass below the level of the old gradation plain. They cause a notable constriction in the inner valley or trench south of Home- wood, but lie mainly below the level of the broad gradation plain. The occurrence of ledges which are more firm and resistant in the narrow than in the broad portions of the old gradation plain tends to greatly reduce, if not remove entirely, the difficulty of carrying through a line of northward drainage. Concerning the variability of the upper part of this rock series White makes the following remarks: ” The rock in question is most variable. Only 3 miles south from the Lawrence County line we find it 155 feet thick in the great ledge at Homewood, but in coming 1Second Geol. Survey Pennsylvania, Rept. Q?, 1879. *Tbid., pp. 53-54. UPPER OHIO DRAINAGE SYSTEM. | ou north it gradually thins away, and where it enters the county has not more than half that thickness, while at Wampum, 4 miles above, it is still further reduced to 50 feet, and on going north along the Beaver a few miles from that point it disappears entirely as a massive rock, being reduced to a few feet of flaggy sandstone and shale. After thinning away almost entirely on the Big Beaver near Newport, it comes in again to the north below Newcastle, and is seen at the falls of Big Run, where it is 30 to 40 feet thick and quite massive. It also retains its massive character to the northward, along the Neshannock. As to the route pursued by the old drainage line from the head of the Beaver toward the Lake Erie Basin, the available data appear to indicate the one from Edenburg northward past Harbor Bridge to Sharon, Pa, and thence westward past Youngstown to the Grand River Basin. But as an alternative view it is suggested that there may have been more than one channel across the resistant portions of the Carboniferous conglomerate, between the head of the Beaver and Youngstown. While the main cur- rent followed the route suggested from Edenburg to Youngstown, a sub- ordinate one may have opened a narrower but more direct channel along the Mahoning Valley. The united breadth of these channels is scarcely equal to the average breadth of the Beaver Valley. The possibility of double channels bemg maintained during the opening of a deep valley finds such striking illustrations in the present Ohio Valley that this view at least merits attention im the interpretation of the drainage peculiarities. The difficulties of interpretation are intensified by the presence of the glacial deposits, which have greatly obscured the valley contours and buried the gradation plains. Although the gradation plain passes below the level of present drainage lines near the head of the Beaver, its altitude and slope may be interpreted with a fair degree of certainty by means of bormgs. In the abandoned valley between Edenburg and Harbor Bridge farm wells enter rock at about 800 feet above tide, or a few feet lower than the gradation plain in the north end of the Beaver Valley. In the abandoned valley between Sharon and Youngstown a boring at Hubbard enters rock at a level slightly below 800 feet. Wells in the Grand River Basin near Mesopotamia, only a few miles north from the present divide between the Mahoning and Grand rivers, reach’ the rock at about 650 feet above tide, and this probably marks the level of the old gradation plain. From the MON XLI——7 98 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. level of the rock floor at these wells it appears probable that the old river entered the Lake Erie Basin at a level at least as low as the present surface of the lake, 573 feet. EXTENT OF THE OLD MONONGAHELA SYSTEM. The old Monongahela system appears to have embraced the entire drainage of the Monongahela, the Allegheny as far up as Clarion River, the portion of the Ohio above Bellaire, the greater part of the present drain- age basin of the Beaver, and the lowland known as the Grand River Basin. The greater part of this drainage system lies outside the glacial boundary, but the trunk stream and its small tributaries northward,from the southern end of the Beaver Valley are within the limits of glaciation, and the Alle- gheny and Ohio valleys have been filled to some extent by glacial gravel transported by streams beyond the ice margin. The portion of the Ohio above the mouth of the Beaver, the Mononga- hela Valley, and the portion of the Allegheny below the mouth of Clarion River have a system of gradation plains that slope in harmony with the present lines of drainage toward the Beaver Valley. They fall less rapidly than the present streams, as is to be expected of such a system of gradation plains. Thus on the Monongahela, as shown by White,' the fall of the present stream is 190 feet in the 206 miles below Weston, West Virginia, while the gradation plain descends only 110 feet in the same distance. On the Allegheny the present stream falls 163 feet in 82 miles below the mouth of Clarion River, while the gradation plain descends but 120. feet in this interval. In the 26 miles from the head of the Ohio at the junction of the Allegheny and Monongahela down to the Beaver the gradation plain has a descent of about 30 feet. At this point it seems necessary only to consider the reasons for not including in the old Monongahela system the part of the Allegheny drain- age basin above the mouth of the Clarion River. These will be but briefly discussed, since the Allegheny drainage is treated in some detail farther on. THE OLD DIVIDE ON THE ALLEGHENY. The gradation plain which is found on the Lower Allegheny continues up the Clarion, as well as up tributaries which enter below the mouth of the Clarion. The portion of the Allegheny immediately above the mouth of 1Am. Geologist, Vol. X VIII, 1896, pp. 368-379. UPPER OHIO DRAINAGE SYSTEM. 99 the Clarion presents a very narrow valley, scarcely one-third the width of the gradation plain of the Clarion and Lower Allegheny. This valley has precipitous bluffs reaching a height of about 400 feet above the stream, or nearly 250 feet above the gradation plain at the mouth of the Clarion. It seems necessary to suppose either that a disproportionately small gradation plain with high cliff borders lay in the narrow gorge, or that there has been a reversal of drainage by which a small stream that had its source just above the mouth of the Clarion and flowed northward was reversed and its valley was recut to fit a new and larger stream. On the first supposition we naturally look to differences in the hard- ness of strata for a possible explanation of the differences in the size of the valley. If there has been but little change in the ancient Allegheny, we must explain the fact that a stream not less than three times the size of the Clarion excavated a valley only one-third to one-half as large. If the subsequent addition of the Upper Allegheny be granted, we must account for the fact that a drainage area about the size of the Clarion cut a valley but one-third to one-half as large. The strata along the narrow portions of the Allegheny, from Franklin to the mouth of the Clarion, as well as for some distance above F ranklin, are on the whole rather more resistant than those in which the gradation plain of the lower course of the Clarion was carved. On the Allegheny there is a considerable amount of the Lower Carboniferous conglomerate, in places reaching a thickness of 75 feet, while on the Clarion there are the more easily eroded Coal Measures sandstone and shale. The greater hardness and resistance to erosion would naturally lessen the size of the valley, though it scarcely seems adequate to produce so marked a difference. Upon turning to tributaries of this part of the Allegheny, a more decisive line of evidence in favor of a reversal of drainage is found. The tributaries of the Allegheny above the mouth of the Clarion have channels that were not deepened to levels in harmony with a gradation plain so low as that of the Clarion. While they have normal gradients on their upper and middle courses, the streams descend by rapids and cascades to the present Allegheny. This is done from a height of about 400 feet, while the tributaries of the Clarion and of the Allegheny below the Clarion descend in this way only 150 to 200 feet. This seems to indicate that tributaries above the mouth of the Clarion formerly discharged into a stream which had not reached so low a plain as that of the Clarion. 100 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Turning now to the bordering uplands, we find another line of evidence favoring reversal. Immediately above its junction with the Clarion the Allegheny cuts through an elevated tract which to the eastward constitutes the divide between waters flowing north and northwest into the Allegheny and those flowing south into the Clarion, while to the westward it constitutes the divide between the northward or eastward flowing tributaries of the Allegheny and the streams flowing south and west to the Beaver and the Shenango (see fig. 5, p. 135). The high divide is broken by a gap scarcely a mile wide and 500 to 600 feet in depth where crossed by the Allegheny. The altitude and relief of this divide appear to be due to its relation to draihage systems rather than to axes of upheaval, for its trend is in large part independent of such axes. That is to say, it constitutes a natural boundary between the Middle Allegheny and the Clarion-Lower Allegheny drainage basins. The slope of rock shelves and remnants of gradation plains north from the supposed divide bring further confirmation of the hypothesis of reversal. The rock shelves which stand 375 to 400 feet above the present stream, or 1,275 to 1,300 feet above tide, near the supposed divide, show a decline of about 200 feet in the 20 miles northward to the mouth of French Creek. This rate of fall would be natural only in a small stream descending from an elevated table-land. The combined force of all the lines of evidence is such that there seems no doubt that there was formerly a divide on the line of the Allegheny ust above the mouth of the Clarion separating the drainage of the old Monongahela system from that of the old Middle Allegheny system. MIDDLE OHIO OR OLD KANAWHA SYSTEM. Near the eastern border of the flat-topped crest of the Cincinnati arch the streams in the vicinity of the Ohio River have a trend which strongly suggests the former presence of a divide. Those to the east of the arch trend up the present Ohio toward the mouth of the Scioto, while those on the flat crest, from its very eastern border, lead westward down the Ohio. The posi- tion of the old divide at the border of the present Ohio seems to be very near the village of Manchester, Ohio. The valley of the Ohio presents higher bluffs in the vicinity of the supposed divide than at points above and below, and the general topographic expression seems adapted to the occurrence of a divide at the place suggested. To this is added the evidence from an abandoned northward outlet, discussed below. MIDDLE OHIO DRAINAGE SYSTEM. 101 Since the principal stream of the system east of the supposed divide is the Big Kanawha River, it seems pertinent to give the name Kanawha to the old system of drainage. It might also be appropriately termed the Middle Ohio system. THE NORTHWARD OUTLET. An abandoned channel leaves the Ohio at Wheelersburg, about 8 miles above the mouth of the Scioto, and, as shown in fig. 3, passes northward in a somewhat winding course, coming to the Scioto Valley at Waverly. That it was the py BR Tecan course of a northward-flowing : a stream is attested by the pres- ence of quartzite cobble and gravel, such as occur along the Ohio above this point. This material was derived from the headwaters of the Kanawha drainage basin. The rock floor of this old drainage line is far above the level of the present stream, being about 625 feet above tide where it leaves the Ohio, while the altitude of the pres- ent stream at that point is about 475 feet; at Waverly its altitude is fully 600 feet, while the Scioto at that point is about 75 feet lower. Its altitude corresponds with that of the system of gradation plains in that region, and its course must be determined by an examination of the 62” oa fy Aah, LP hm wl, % Mast oe D 7, wy, . POM Messty, op sii sll 2 £ % a Fic, 3.—The old Kanawha drainage system in southern Ohio. gradation plains on the Scioto. From Waverly the old Kanawha must Hive taken one of two courses, either northward into the Scioto Basin along the line of the present Scioto (reversed), or southward down the present Scioto Valley to the Ohio at 102 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Portsmouth. As the latter is the present course of drainage, we naturally turn to it first. An examination of the Scioto Valley below Waverly has brought to light an old oxbow channel immediately back of the town of Lucasville, which has about the same altitude as the channel of the old Kanawha east of that point, but which appears to have been formed by a much smaller stream than that which formed the channel of the Kanawha. Its breadth, as shown in fig. 3, is only about a half mile, while that of the old Kanawha Valley is more than a mile at its narrowest places and 14 miles or more at its broadest places. This small channel has every appearance of being the main if not the only line of discharge for the stream that opened it. It is such a channel as would be expected from a stream which drained only the small area that lies between Lucasville and the supposed divide near Manchester, Ohio. It certainly testifies strongly against the discharge of the old Kanawha southward from Waverly. A similar oxbow of a small stream was found on the south side of the Ohio near Quincy, Ky., about 10 miles below the mouth of the Scioto. It, however, stands so much higher than the oxbow at Lucasville (being nearly 150 feet above its level) that it seems likely to have been abandoned at an earlier date than the Lucasville oxbow; but it may, nevertheless, have been produced by the same small stream, it being not unnatural for oxbows to be abandoned during a process of downcutting in a valley. The correla- tion in agency rather than the correlation in date is the important matter, and on this the two oxbow channels are in harmony, for they each appear to show the agency of a much smaller stream than the old Kanawha. Turning now to the portion of the Scioto north from Waverly, it is found to carry a broad gradation plain similar to that of the abandoned part of the old Kanawha, which can easily be traced to the vicinity of Chillicothe, where it passes below the level of the Scioto and soon becomes deeply buried beneath deposits of glacial drift. The writer called attention to this northward line of discharge for the middle portion of the Ohio in his report to the Director in June, 1896, and suggested that it was probably tributary to the drainage basin of the Saint Lawrence.’ Ina paper prepared afew months later? this interpretation was 1Seventeenth Ann. Rept. U. 8S. Geol. Survey, Pt. I, 1896, p. 61. * Changes of drainage in southern Ohio: Bull. Denison Univ., Vol. IX, Pt. II, 1897, pp. 18-21. MIDDLE OHIO DRAINAGE SYSTEM. 103 qualified and four possible courses were suggested for the discharge from the southern end of the Scioto Basin: First, southward, down the Scioto from Waverly to the Ohio and thence down the Ohio; second, northward, along the axis of the Scioto Basin to Lake Erie; third, northwestward across western Ohio, along one of the several deep valleys brought to light in that region by the oil and gas wells, eventually to either the low tract on the lower course of the Wabash or the basin of Lake Michigan; fourth, north- eastward past the Licking reservoir and an old valley east of Newark to the Muskingum at Dresden, and thence northward along or near the pres- ent valleys of the Muskingum, Tuscarawas, and Cuyahoga to the basin of Lake Erie at Cleveland. It was since that paper was prepared that the writer discovered the oxbow channel back of Lucasville, above noted, which seems to testify strongly against the southward discharge down the Scioto and renders that line an improbable one. The writer also has since found decisive evidence against the suggested northeastward line, in the presence of an old divide now crossed by the Tuscarawas between Zoar and Canal Dover, Ohio, discussed farther on. Concerning the relative probabilities of the remaining two lines but little has been determined. If the present surface is examined both the northward and northwestward courses seem beset with difficulties. The northward route along the axis of the Scioto Basin encounters a general rise in the bordering plain of about 200 feet in the 100 miles between the south end of the basin, near Chillicothe, and the continental divide near Marion, north of which there is an even greater descent to the Lake Erie Basin. If the course of drainage was northward across the divide, and if the divide has not suffered recent uplift, there must have been channeling in it to a depth of about 300 feet. That an axis of uplift exists in this part of the continental divide is shown by the arching of the rock formations over it; but its extent and its date are not yet determined.’ The northwestward route leads across the limestone belt on the west side of the Scioto Basin, whose general level is about 200 feet above the continental divide at the north end of the basin and 500 feet above the gradation plain near Chillicothe. To pass through that region the 1See Geology of Ohio, Vol. VI, 1888, pp. 57-58, 312, 316. See also the sections of rock forma- tions from Cleveland to Marietta, and from Berlin Heights to Ironton, opposite p. 321 of same volume. 104 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. channeling would be so much greater than is required for a northward course along the axis of the basin that one can scarcely resist ruling out the north- westward course. Yet from what is found on the Lower Ohio, where the stream passes directly across the low Devonian shale area into the knobstone and sandstone formations that now stand much higher, such a ruling may be unwarranted. The presence of the low basin occupied by Lake Erie offers an additional argument in favor of the northward route. This basin would be reached by that route in less than half the distance required to reach a similar low tract in the Wabash region or the Lake Michigan Basin by the northwestward route. ach of these routes falls within regions so heavily covered with glacial deposits that the course of the channels can be traced only by means of borings, and these are so few and so poorly distrib- uted as to be inadequate to our needs. ; DEFLECTIONS OF DRAINAGE. In changing from its old course to its present one the Kanawha system has suffered several notable deflections. The principal one is that which turned the waters southward from the Seioto Basin to the present Ohio at Portsmouth, and thence westward into the Lower Ohio; a second deflection carried the waters of the Kanawha westward from Wheelersburg (where the old Kanawha tured north from the Ohio) to Portsmouth, thus abandon- ing the part of the old channel between Wheelersburg and Waverly; a third turned the Kanawha north from the east end of Teays (or Teazes) Valley (mear St. Albans, W. Va.) to the Ohio at Poimt Pleasant, thus abandoning Teays Valley from St. Albans to Huntington. It is not certain that these changes were made at one time, though they appear to have been made in close succession. The second and third appear to have been nearly contemporaneous from the fact that the abandoned channels are each at the level of the main gradation plain, about 150 feet above the present level of the Ohio River. It seems probable that the deflection to the Lower Ohio may have preceded the deflection from Wheelersburg to Portsmouth, there being apparently no sufficient reason for the latter to have taken place until the western line of discharge from Portsmouth had been opened. The change which resulted in the deflection of the old Kanawha into the Lower Ohio seems to have required considerable erosion in the vicinity of the old divide, even though it occurred when the streams of the old Kanawha system were flowing in valleys whose depth was much less than MIDDLE OHIO DRAINAGE SYSTEM. 105 that of the present Ohio. The removal of the col near Manchester, at the head of the southwestern tributary, probably represents but a small, part of the work accomplished, for the channel of this tributary seems to have been enlarged throughout its length of fully 50 miles. There was apparently, also, some enlargement of the headwater portion of the old west-flowing stream beyond the divide, for the Ohio River bluffs are excep- tionally abrupt for a few miles west from Manchester. The change to the present course from Wheelersburg to Portsmouth seems to have required but little work. The principal cutting appears to have been in the 3 or 4 miles between Wheelersburg and the mouth of Tygarts Creek, a north-flowing stream which reaches the Ohio just above Portsmouth and which apparently connected there with the stream above noted that'came in from the southwest. The ridge crossed east of Ports- mouth is prominent on each side of the Ohio, its altitude being about 300 feet above the old Kanawha channel. But the space sbove the bluffs is about 14 miles, and this may have contained a sag or broken-down part of the ridge, so that the cutting need not have been so much as the height of the present bluff would indicate. The maximum allowance for cutting can not exceed 300 feet in depth, 14 miles in width, and 3 miles in length, and the probabilities are that the cutting was much less than that amount. The abandoned line of discharge for the Kanawha River between St. Albans and Huntington, W. Va., known as Teays Valley,’ was brought to notice some years ago by White* and discussed more fully later by Wright,’ under the name of Teazes Valley. The rock floor of this abandoned valley stands 630 to 650 feet above tide, or 145 to 165 feet above the Ohio at Huntington, W. Va., where it connects with that stream. Measurements with Locke level show that the rock floor at the east eud near St. Albans has an altitude of 630 to 640 feet, while at the mouth of the Big Sandy River, just below Huntington, the rock floor of its broad terrace has an altitude of 630 feet. Between these places points were found where the rock floor reaches 650 feet, but it is not certain that the lowest part of the channel floor was exposed. The old gradation plain is now covered with a thick deposit of silt, whose surface stands 700 to 720 feet above tide, or 60 to 80 feet above the rock floor. This silting was sufficient to build up the ‘Geologic Atlas U. S., folio 69, Huntington, W. Va. * Appendix to Wright’s Glacial Boundary in Ohio, 1884, p. 84. * Bull. U. 8. Geol. Survey No. 58, 1890, pp. 86-88. 106 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. ~ valley to a level as high as low cols in the district north of it, thus making it possible for a stream to take a new course without having to open a channel. Not only the Kanawha but Hurricane Creek and Guyandot River (tributaries entering Teays Valley from the south) continue into channels north of that valley. The channel into which the Kanawha and Hurricane Creek were turned had gradation plains slightly higher than the rock floor of Teays Valley, measurements with Locke level showing the height of the gradation plain on the lower end of the present Kanawha, near the mouth of Hurricane Creek, to be 680 feet above tide, but as these channels had not become so filled with silt as Teays Valley, the drainage could pass into them. It is this fact of a lower line of escape that seems chiefly responsible for the diversion from a direct to an indirect course. Between the west end of Teays Valley and the south end of the aban- doned channel at Wheelersburg the old line of the Kanawha usually nearly coincides with that of the present Ohio, and its rock floor stands 150 feet above the present stream. There is, however, one deflection worthy of mention. For a few miles below the point where the Ohio passes the West Virginia and Kentucky line, the old Kanawha channel is separated from the present Ohio Valley by a narrow range of low hills. This valley, with its deposits of gravel, was noted by Lyon in an early report of the Kentucky geological survey,’ and was described more fully by Andrews in a report of the Ohio survey.” By both, the gravel deposits were erroneously referred to the glacial drift. In this old channel the silt filling is but little less than in Teays Valley, the surface of the silt being 680 to 700 feet above tide, or 50 to 70 feet above the rock floor. The gravel which underlies the silt is a thin deposit resting upon the rock floor. The accompanying map (PI.VIJ), which embraces a portion of the Ironton quadrangle, shows a part of this old valley and the present Ohio, with a range of hills between them. The hills occupy the interval between the mouths of White Oak Creek and Pond Run. Although they rise in places to a height of more than 100 feet above the silt filling in the old valley, they are interrupted by notches so low that small streams drain from the old valley through them to the present Ohio. It is probable that the Ohio took advantage of similar low gaps in changing from the old course to the present one. 1Sidney Lyon: Second Geol. Rept. of Kentucky, 1856 and 1857, p. 360. 2H. B. Andrews: Geology of Ohio, Vol. II, 1874, p. 441. a eee JPA2] DAS UDGU S2 UAC Jo25 OG TeAteFUT aN0}UTOD) S19} OULOPHy & ri T ri some z Ge 0g T ry ‘ ; 1 padans 006! UEC 4O UOKIpS OIHO “NO.UNOU AVAN SHY OLVA HOVNIVEC {SOW NM Rue ccmiel(Mecteleka Aydeusgodoy “WN 700 8 NSIS Sdnnar AAANYNS 1V9I90T1039 SN MIDDLE OHIO DRAINAGE SYSTEM. 107 How much of the present Ohio above the point where Teays Valley connects with it follows its old course may now be considered. Between the present mouth of the Kanawha, at Point Pleasant, W. Va., and the west end of Teays Valley, the Ohio is in a valley which for a few miles becomes so constricted as to suggest the crossing of an old divide. The width at Point Pleasant is about 2 miles, but it becomes reduced to 14 miles in the first 8 miles below that town, and to scarcely 1 mile at Crown City, 10 miles farther down. For 10 miles below Crown City the breadth is a mile or less. The valley then gradually expands to a width of nearly 2 miles at Huntington, 15 miles farther down the river. In this narrow por- tion the bluffs rise abruptly to a height of 200 feet, or to about 700 feet above tide, and the uplands reach an altitude 200 feet higher within a mile or two of the river. A thick-bedded, very resistant sandstone outcrops at about 700 feet throughout much of the narrow portion, and in several places" presents mural escarpments and often breaks in blocks 10 to 15 feet thick. This sandstone, no doubt, has had great influence in making the bluffs abrupt up to this altitude and in preventing a widening of the valley. Whether it fully accounts for the narrowness, or whether the narrow portion once contained a divide, the writer was unable to decide. In passing up the Ohio from the mouth of the Kanawha to the mouth of the Little Kanawha River, at Parkersburg, W. Va., the valley of the Ohio is found to be very winding and also exceptionally broad, its width rang- ing from 14 to nearly 3 miles. Throughout this interval its passage is through a region similar to that in the vicinity of Teays Valley, in which the divides have been greatly broken down, so that there are numerous cols at only 700 to 750 feet above tide. This portion of the Ohio Valley preserves but few rock shelves or remnants of a gradation plain that can be correlated with the gradation plain on the old Kanawha noted above. The tribu- taries, however, present remnants of a gradation plain which serve to show the height of the old valley floor above the present Ohio. They stand nearly as high as the lowest cols, being nowhere less than 660 feet above tide, and usually about 680 feet, while at the mouth of the Little Kanawha they are not far from 700 feet. The lowest observed altitude—660 feet— is found about midway between the mouths of the two Kanawhas, opposite the mouth of Big Mill Creek, above Letart Falls, West Virginia. The terraces there, by barometric measurements, stand only 120 feet above the 108 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Ohio River. But levels more precise than barometric measurements are needed to make certain of the altitudes and slopes of the terraces in this part of the valley. The widely meandering course of this portion of the Ohio apparently resulted from the former slack drainage and degraded condition of the region Conditions were such that shiftings of the course might easily have been produced. A large area in southern Ohio north of this part of the Ohio Valley carries low divides, which afforded good opportunities for changes of drainage. The neighboring portion of West Virginia is also similarly broken down. The changes which this part of the drainage basin has experienced are being made a subject of special investigation by W. G. Tight, under the auspices of the present survey. These investigations will, it is hoped, settle the question whether the old course of drainage continued from the mouth of the Little Kanawha down to the west end of Teays Valley—that is, to the old Kanawha—or, instead, took a northwestward course, more directly toward the Scioto Basin, into which the old Kanawha had its discharge. It seems well to defer the intro- duction of names for the old drainage lines in this part of the Ohio until this question is settled. From the vicinity of Moundsville, W. Va., down to the mouth of the Little Kanawha, at Parkersburg, the present Ohio appears to be following the line of an old stream, whose main gradation plain, now preserved as terraces along the valley borders, descends from about 800 feet at New Martinsville to but 700 feet at Parkersburg. The remnants are not con- spicuous in the Ohio Valley, but are well preserved on many of the tribu- taries. Pr The general width of the Ohio Valley from Moundsville down to St. Marys, W. Va., is 1 to 14 miles, though near Ravens Rock it is less than a mile, and in the vicinity of the villages of Moundsville and New Martins- ville it exceeds 2 miles. From St. Marys down to Parkersburg the width is 13 to2 miles. In explanation of the remarkable expansions at Moundsville and New Martinsville, J. P. Chaplin, a civil engineer residing at New Mar- tinsville, has suggested an unusual dip of the rock strata. In the 4 miles above New Martinsville, where the valley is exceptionally wide, the strata dip eastward at the rate of 80 feet per mile, which is much greater than in the portions of the valley immediately above and below this expansion. Chaplin states that the strata at Moundsville have a marked dip southeast- ; § : LOWER OHIO DRAINAGE SYSTEM. 109 ward, though not so great as at New Martinsville, and he is inclined to refer the expansion there to the increased dip of the strata. This enlargement of the valley seems to have antedated its filling with glacial gravel of Wis- ' consin age. Since the filling occurred the stream has been shifting its course over the gravel bottom, and at present, in both the Moundsville and the New Martinsville expansion, it is following the west bluff instead of the east. LOWER OHIO SYSTEM. PROBABLE EXTENT. Under this name will be discussed the portion of the Ohio below the old divide near Manchester, together with such of its tributaries as are concerned in the drainage and glacial history of the region. The Ten- nessee and Cumberland rivers, which now enter the Ohio near its mouth, are practically independent of the Ohio, since their mouths are within the Tertiary valley of the Mississippi. Green, Salt, Kentucky, and Licking rivers are the main large southern tributaries. These and the small south- ern tributaries have apparently suffered very little disturbance by glacia- tion. The northern tributaries, Little and Great Miami rivers, and the Wabash, with its main affluents, White and East White rivers, have had their drainage systems greatly modified by glaciation, so that it is difficult, if not impossible, to restore the preglacial system. It is probable, however, that a large part of the present drainage basins of these rivers was tributary to the Lower Ohio in preglacial time. Attention is called below to the question of a former northward discharge of part of the Ohio drainage basin through the Great Miami Basin. RELATION TO TOPOGRAPHIC FEATURES. In the portion of the Ohio below the old divide near Manchester several rock formations are crossed which have yielded very unequally to subaerial degradation, and now present a series of escarpments and basins that are more impressive as topographic features than the valley of the river. These topographic features, however, exert but little influence upon the course of the Ohio and its tributaries. They trend in line with the strike, while the Ohio takes a course more nearly in harmony with the dip of the rock formations. The river passes from the Cincinnati arch across the low Niagara escarpment, formed by. the Lockport limestone, down to the basin formed in the Devonian shale and thence on through ry 110 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the Knobstone escarpment at a point where it has a relief of over 200 feet above the shale basin. It then crosses a shallow basin in the St. Louis limestone, after which it passes through the prominent Kaskaskia and Conglomerate Coal Measure formations and reaches the low basin of the friable Coal Measures. Finally it traverses the elevated rim of Lower Car- boniferous sandstone and limestone and enters the broad valley of the Lower Mississippi. This disregard of topographic features is paralleled by some of the tributaries of the Lower Ohio. Green River takes a somewhat direct west- ward course across escarpments and basins in the formations between the Devonian and Coal Measures in a district south of the Ohio, while the East White River takes a similar course in a district north of the Ohio. Salt River passes westward across the low basin of Devonian shale into the Knobstone escarpment and joins the Ohio instead of turning northward along the axis of the low basin. The Kentucky River seems to have suffered more deflection by topographic and structural features than the tributaries just mentioned. In crossing the crown of the Cincinnati arch it makes a marked detour to the southwest, but turns back to the north along the east side of the low Niagara escarpment, as if guided by that escarpment. While the streams of this drainage system usually pass somewhat directly across the basins and escarpments, their courses are generally marked by a pronounced breaking down both of the escarpments and of the basins in the vicinity of the stream valleys. This is especially true of the major stream, 'the Ohio. In the passage across the Lockport (Niagara) limestone near Madison, Ind., the immediate bluffs rise 350 to 400 feet above the stream, or 750 to 800:.feet above tide, but the uplands 2 or 3 miles back reach fully 500 feet above the stream, and become still higher farther back. In the Devonian shales the Ohio bluffs are only 75 to 125 feet above the river, or 450 to 500 feet above tide, but back 20 miles from the Ohio, at the divide between this river and the East White River, the axis of the shale basin rises to an altitude of over 600 feet above tide, and a similar rise is found south of the Ohio along the axis of the basin. The Knobstone formation is much more broken or degraded in the vicinity of the Ohio than a few miles north or south of the river, as well as of lower altitude. Its highest knobs on the border of the Ohio scarcely reach 800 LOWER OHIO DRAINAGE SYSTEM. tal feet above tide, but a few miles back they rise to about 1,000 feet. There is a similar breaking down on the borders of the Ohio in each of the for- mations to the west. In view of this condition of the formations on the border of the Lower Ohio, there seem to be grounds for considering it a very old drainage line, whose course was adopted before the present pro- nounced escarpments and basins had been formed. TERTIARY FLUVIAL DEPOSITS. The great age of the valleys of the Lower Ohio and its tributaries is also shown by the occurrence, on high terraces bordering the canyon val- leys, of deposits of sand and gravel which appear to be fluvial and bear evidence of transportation to some extent in the present direction of drainage. These deposits were long ago recognized by Cox on the borders of the Ohio in southern Indiana,’ and by Safford on the borders of the Tennessee and other streams of Tennessee and Kentucky.* More recently they have been noted and described on the Cumberland, Kentucky, and Licking rivers by Miller,’ and on the Kentucky River by Campbell.’ The deposits noted by Cox cap the blufts of the Ohio near Cannelton, Ind., at an altitude of about 350 feet above the stream, or nearly 700 feet above tide. The present writer has traced them eastward or up the Ohio Valley from the points noted by Cox, and found that they are preserved in small detached remnants on the bold bluffs of the Conglomerate Coal Measures and Kaskaskia formation, on both the Indiana and the Kentucky side of the narrow river valley, as far as the eastern border of the latter formation. As now preserved, they are only 10 to 20 feet in depth, and the original thickness may have been but little more. Their altitude is above the general level of the basin which has been formed in the St. Louis limestone to the east, but in their rock constituents these deposits bear clear evidence of derivation from the cherty portion of that formation. The transportation must have been effected before the basin had been formed in the St. Louis limestone, a fact which testifies strongly to the great age of the deposits. lTertiary deposits, by E. T. Cox: Rept. Geol. Survey of Indiana for 1871 and 1872, p. 138. * The eastern gravel, by J. M. Safford: Geol. Tennessee, 1869, p. 438; see also pp. 434-437. ’ High-level gravel and loam deposits of Kentucky rivers, by A. M. Miller: Am. Geologist, Vol. XVI, 1895, pp. 281-287. *The Irvine formation, by M. R. Campbell: Geologic Atlas of the United States, folio 46, Rich- mond, Ky., 1898. 112 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The deposits on the Licking and Kentucky occur on what are termed by Campbell ‘intermediate valleys,” whose floor is about 300 feet above the present streams, and but 100 feet below the general level of the border- ing uplands. Miller calls attention to the presence of pebbles from Car- boniferous rocks, and notes that they are restricted to deposits on those tributaries of the Licking and Kentucky which have their sources in the Carboniferous formations. From these facts the inference, is drawn that they were deposited by streams which flowed in the present direction of drainage. He has traced the deposits down the Kentucky Valley to the vicinity of Frankfort, or across the crown of the Cincinnati arch. In a letter to the writer he reports that the altitude of the deposits declines from about 900 feet im the vicinity of Irvine, Ky., to 800 feet near Frankfort. They stand, therefore, at the latter point about 190 feet higher than the deposits above noted on the Ohio, and seem likely to be of similar age. As yet no attempt has been made to trace the deposits from Frankfort to the Ohio, but it is thought by Miller that the course will continue down the Kentucky rather than depart from that valley. The wide gaps made by basins which have been subsequently formed along the course of the Ohio will necessarily render it difficult to establish full-connection between the deposits of the Kentucky and those near Cannelton, on the Lower Ohio. There seem, however, to be no reasonable grounds for doubting that there was such a connection, and the degraded condition of the valley border from the mouth of the Kentucky to the deposits farther down the Ohio seems of itself sufficient ground for inferring that the course of drainage at the time these deposits were made was that which the Ohio still pursues. So far as the writer could discover, no better course is available. A course about as direct is found in a line leading westward from Madison, Ind., along the Museatatuck to the East White and White River, and thence down the Wabash to the Ohio. That there was an ancient westward drainage along the East White River is shown by the presence of Tertiary gravel near Shoals, Ind., that was brought in from the east. But the Kast White has a smaller channel than the neighboring part of the Ohio, and no channel — has been discovered near Madison to connect the Ohio with the Museatatuck Valley. It therefore seems a less favorable course than that down the Ohio. The gap to be filled between the Tertiary deposits on the Licking and those on the Lower Ohio is still wider and seems more dificult to bridge. LOWER OHIO DRAINAGE SYSTEM. WL} It is probable that at the time these deposits were made the Licking crossed the present Ohio at Cincinnati, and, together with the section of the Ohio between Manchester and Cincinnati, continued northward at least to the vicinity of Hamilton, Ohio. Possibly it maintained a northward course, passing Hamilton along the axis of the Great Miami Basin, though it seems quite as probable that it turned southwestward to connect with the Ohio at the mouth of the Great Miami and passed from there down the Ohio and connected with the Kentucky. The drainage, as indicated below, appears to have been along the latter course for a long period before the deposition of the Illinoian drift. GRADATION PLAINS BELOW THE LEVEL OF THE TERTIARY DEPOSITS. As may be seen by comparing the altitude of these Tertiary deposits on the Lower Ohio and its tributaries with that of the gradation plains of the Middle Ohio or old Kanawha system, the latter are far below the former. It will also be noted that the gradation plains of the Middle Ohio system pertain to valleys which had been cut to a much greater depth than those that carry the Tertiary deposits of the Lower Ohio system. Furthermore, the gradation plains are in a much better state of preservation in the Middle Ohio system than the floor of the valleys which carry the Tertiary deposits of the Lower Ohio system. These features suggest that the gradation plains of the Middle Ohio system and the ‘intermediate valleys” of the Lower Ohio system are not correlatives and lead us to examine the valleys of the latter system for correlative gradation plains at levels below the Tertiary deposits. The glacial deposits have obscured the contours of the Ohio Valley throughout much of the area between Manchester, Ohio, and Louisville, Ky., rendering it difficult to trace terraces or remnants of gradation plains on the valley borders. They have in a similar manner greatly obscured the northern tributaries of the Ohio. The southern tributaries should, there- fore, afford the best field for the examination of gradation plains. These, however, have been examined only to a limited extent by the writer. Observations were carried up the Kentucky only to the mouth of Eagle Creek, about 8 miles, and up the Licking River to Grants Bend, about 12 miles. Even less attention was given to other southern tributaries. On the Licking River no well-defined remnants of a gradation plain were found below Grants Bend; but for 2 or 3 miles in the vicinity of this MON XLI——8 114 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. bend a gradation plain is preserved, and in places occupies about half the width of the valley. Its altitude by aneroid is 640 to 650 feet above tide, or nearly 200 feet above the stream. Its rock platform is capped with a few feet of gravel and sand, among which are pebbles derived from the Lower Carboniferous rocks that outcrop at the headwaters of the Lickmg. A gradation plain of similar altitude above the river is reported by the resi- dents to be preserved at points farther up the valley. This gradation plain stands 250 to 300 feet below the neighboring uplands in a valley much narrower and more sharply outlined than that which carries the Tertiary deposits. Its relation to the uplands and also to the present drainage 1s similar to that of the gradation plain of the middle Ohio system, of which it is the probable correlative. On the Kentucky River but one place was found on the lower 8 miles of the valley which seems to representa gradation plain. This is a terrace standing on the east side of the valley opposite Lock No. 1, about 3 miles from the Ohio. Its altitude is by aneroid 175 feet above the stream, or searcely 600 feet above tide. A northern tributary of the Ohio (Indian- Kentuck Creek), entering 4 miles below the mouth of the Kentucky River has well-preserved remnants of a gradation plain near its mouth, standing by aneroid 610 feet above tide. These seem to harmonize with the single remnant found on the Kentucky and to support the view that it Ba: a gradation plain. One of the most conspicuous remnants which this region affords of a gradation plain on the immediate borders of the Ohio, and one which is rather difficult to interpret, is that of an abandoned channel which leads from Eagle Creek, now a tributary of the Kentucky River, northward to the Ohio River. It leaves Eagle Creek 2 miles west of Glencoe, Ky., and passes in a winding course to the Ohio Valley at the bend above Warsaw, Ky. It stands fully 200 feet above the Ohio, and has a width of about one-half mile. | An abandoned channel with a gradation plain of a similar height and width connects closely with this channel and continues northward, back of a range of hills east of the Ohio, to the south fork of Big Bone Creek, a stream which passes from there westward into the Ohio. This northward continuation of the abandoned channel was at first thought by the writer to indicate that the old course of drainage continued northward from the LOWER OHIO DRAINAGE SYSTEM. Tels mouth of Big Bone Creek, in the reverse direction of the present flow of the Ohio. This would bring support to a view recently advanced by Fowke,! that the Licking and the neighboring part of the Ohio continued from Cincinnati northward, past Hamilton, through the Great Miami Basin, and received this and other small tributaries along the line leading to Hamilton from the southwest, past Lawrenceburg, Ind. But upon further reflec- tion and a reexamination of the locality doubt has arisen concerning the validity of this interpretation. A strong element of uncertainty is found in the fact that the part of the Ohio near the points where this small abandoned channel makes its connections has the exceptional width of 14 to 2 miles, and carries worn and receding bluffs that seem to be as old as the abandoned channel at its side. There is also some uncertainty as to the interpretation that this abandoned channel was opened by Eagle Creek. Its size is more in harmony with that of Big Bone Creek, and markedly less than the portion of Hagle Creek Valley with which it connects. At present it is uncertain whether by the abandonment of this valley the Eagle has been deflected from the Ohio to the Kentucky, or whether the Big Bone has been deflected from the Kagle-Kentucky drainage to the Ohio. This question is, however, of less importance to the subject under discussion than that of the existence of a gradation plain which corresponds quite closely with the remnants of gradation plains found on the lower course of the Licking and Kentucky. | Upon passing below Louisville to the portion of the Ohio outside the limits of glaciation, remnants of a gradation plain have been found on tributaries which enter through the resistant sandstone formation They are especially well defined on Big Blue and Little Blue rivers, one of which enters above and the other below the abrupt bend made by the Ohio River at Leavenworth, Ind. Like the gradation plains of the Licking and Kentucky, they stand about 175 to 200 feet above the stream, but their altitude above tide is only about 550 feet, or fully 50 feet lower than the gradation plains near the mouth of the Kentucky. This is to be expected on the supposition that the drainage was along the present course. These gradation plains in the vicinity of Leavenworth stand about 150 feet below the level of the Tertiary deposits which, as above described, cap the bluffs of that portion of the Ohio Valley. 1 Bull. Denison Uniy., Vol. XI, 1898, pp. 1-10. 116 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. In the 100 miles between the outcrop of the resistant conglomerate Coal Measures near Cannelton, Ind., and the pomt where the Ohio opens into the broad valley of the Lower Mississippi near Paducah, Ky., the rock formations are so friable that the bluffs are in large part broken down to a lower level than the gradation plains would be expected to occupy. It is scarcely possible, therefore, to carry a definite tracing of the gradation plains across this interval and connect them with the equivalent deposits on the Lower Mississippi. It is possible, however, that discriminative studies will make clear the equivalents on the Lower Mississippi both of the grada- tion plains and the Tertiary deposits of the Lower Ohio system. DRAINAGE CHANGES NEAR CINCINNATI. , Reference has already been made to the old northward line of dis- charge of the Licking and part of the Ohio from Cincinnati, through the valley of Mill Creek, to the Great Miami near Hamilton, Ohio. The course of the Licking was through the western part of Cimcinnati along the lower course of Mill Creek reversed, while that of the Ohio was around the east and north borders of the Walnut Hills upland to the junction with the old Licking in the north part of the city (see Pl. V). James, some years ago, made the interpretation that the course of drainage just outlmed was continued from the Great Miami near Hamilton westward, through an abandoned valley, to the Whitewater River near Harrison, Ohio, and thence down the Whitewater Valley to its junction with the Great Miami Valley near the point where the latter joms the Ohio at Lawrenceburg, Ind? The Ohio is thus given a detour of about 20 miles to the north of its present course. This interpretation has recently been in part called in question by Gerard Fowke,’ who has suggested that the Ohio continued northward from Hamilton along the Great Miami Valley and that it received a tributary from the direction of Lawrenceburg instead of taking a course past that city. While the course of drainage suggested by Fowke may have been operative at some remote period, as already indicated, it seems quite certain that the course suggested by James was in operation in the period of deep valley excavation that preceded the deposition of the oldest drift of that 1 An ancient channel of the Ohio River at Cincinnati, by Joseph F. James: Jour. Cincinnati Soc. Nat. Hist., Vol. XI, 1888, pp. 96-104. 2Bull. Denison Uniy., Vol. XI, 1898, pp. 1-10. Also Ohio Acad. Sci., Special Papers No. 3, 1900, pp. 68-75. LOWER OHIO DRAINAGE SYSTEM. LAL locality (the Ilinoian drift). This abandoned course, unlike the abandoned course of the Middle Ohio from Wheelersburg to Waverly, was cut down before its abandonment to a level below that of the present Ohio. It corre- sponds apparently to the trenches or canyon valleys of the Middle and Upper Ohio systems. The rock floor of the valley being below the level of the present draimage lines, its slopes can be determined only by means of borings. From the data thus obtained along the abandoned course, as well as along the Ohio below the mouth of the Great Miami, it appears that the rock floor lies about 60 feet below the present low-water level of the Ohio, and has a descent in the present direction of drainage. From a level about 375 feet above tide at Cincinnati it falls to 360 feet or less at Rising Sun, Ind., and to 350 feet or less at the mouth of the Kentucky River. At Cincinnati the tests have been sufficiently numerous to show the full depth where the old Licking crossed the present Ohio. At other points the tests are not so numerous, but they are sufficient to show that the altitude of the rock floor becomes lower below the mouth of the Great Miami than it is at Cincinnati. Borings in the abandoned channel between Cincinnati and Hamilton show a rock floor as low as those in Cincinnati. So far as the writer is aware, no borings along the Great Miami above Hamilton have reached so low a level before entering rock as those on the Ohio below the mouth of the Great Miami. In addition to the slope of the rock floor, there is the further evidence for the route suggested by James, in the presence of a broader valley along that line than on the Miami northward from Hamilton. The latter becomes reduced just above Hamilton to a width of less than a mile, and that, too, at a height of fully 200 feet above the level of the rock floor, and its general width as far up as Dayton is but little more than a mile. The abandoned valley leading west from Hamilton, in the route suggested by James, is 14 to 2 miles in width, and there is no constricted place from there to the Ohio, nor down the Ohio to the mouth of the Kentucky. In this connection it may be remarked that constrictions farther down the Ohio near Madison, Ind., and Leavenworth, Ind., occur in the passage through escarpments of resistant rocks, where the valley has exceptionally high bluffs, and apparently do not lessen the size of the valley more than would naturally result from the greater resistance of the rock strata. The earlier paper presented by Fowke is accompanied by a map which 118 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. aims to show that the tributary streams below the mouth of the Great Miami enter through valleys which point up the Ohio Valley. There are, how- ever, streams which are omitted from that map, such as Gunpowder Creek and the North Fork of Big Bone Creek, which point very strongly down the Ohio Valley. It is also found that north from Hamilton tributaries of the Great Miami show a decided tendency to trend down the Miami Valley, not only at their poimts of entrance but througbout much of their course. This topographic feature, therefore, can scarcely be urged to sustain Fowke’s interpretation. From Cincinnati down to the mouth of the Great Miami the valley of the present river has scarcely half the width which it presents below the mouth of the Miami. Just below Cincinnati, where the stream is thought to have crossed an old divide (see PI. V), the bluffs reach the exceptional height of about 450 feet, and are very abrupt nearly to the top. Upon passing down the valley they soon assume the worn and receding slopes characteristic of an old valley, though so much smaller than that opened by the Ohio past Hamilton that it seems the natural product of a stream draining only the tract between Cincinnati and the mouth of the Great Miami. If we may judge by the boldness of the bluffs, a prominent col was crossed in the vicinity of the supposed divide. There may, however, have been a narrow notch of considerable depth whose borders have been cut away by the present large stream. The old divide crossed by the Ohio above the present mouth of the Licking River has been so greatly filled in by glacial deposits on the Ohio side of the river that its rock contours are much obscured. It is certain, however, that the blutts are greatly degraded, and it is probable that a very low gap existed here at the time the deflection was produced. RELATION OF THE GLACIAL DEPOSITS TO THE EROSION FEATURES OF THE OHIO VALLEY. ON THE LOWER OHIO. Before attempting to interpret further the changes of drainage which have resulted in forming the present Ohio River, it will be advantageous to consider briefly the relation of the glacial deposits to the erosion features. It so happens that the only part of the immediate valley of the Ohio which has been glaciated lies in the section called the old Lower Ohio, from GLACIATION AND EROSION IN OHIO VALLEY. ily) a point a few miles below Manchester, Ohio, down to the vicinity of Louisville, Ky. But along the entire length of the present valley assorted material derived from glacial deposits has been distributed, and much may be learned by determining the relation of this assorted material to the valley excavation. The portion of the Ohio Valley which has experienced glaciation covers nearly the interval from Louisville up to Maysville, Ky., 190 miles, for the glaciation fell short but 5 to 10 miles of reaching the site of each of these cities. The abandoned course of the Ohio near Cincinnati should also be included, and as this is less direct than the present course it increases the length of the glaciated portion of the valley to about 225 miles. Throughout this glaciated portion, including the abandoned course of the stream, the drift deposits are found to extend down to a rock floor lower than the bed of the present river, and as these include till or unmod- ified glacial material it is evident that the excavation of the valley to its lowest depth preceded that stage of glaciation which produced these deposits. This particular glaciation, as explained farther on, belonged to the Ilinoian stage. It is certain, therefore, that at that early stage this part of the Ohio was excavated to its full depth. ON THE MIDDLE OHIO. The Middle Ohio or old Kanawha system is less favorably situated than the Lower Ohio for determining the relation of the glacial deposits to the erosion features, for the part of the Ohio Valley which falls in that sys- tem was not reached by the ice sheet. It is also found that along the old northward outlet of that drainage system the Ilinoian glaciation extended but a few miles beyond the later or Wisconsin glaciation. ‘There are, how- ever, a few features outside the glacial boundary which throw some light upon this question. Above the level of the Wisconsin glacial terrace which leads down the Scioto to the Ohio there are deposits of gravel and sand derived apparently from Ilinoian drift. Their height is 60 to 75 feet above the Wisconsin terrace, and they have been found along the Scioto for about 30 miles south from the glacial boundary or nearly to the Ohio River. They have been observed only on the remnants of the gradation plain of the small stream, which, as above described, seems to have been a southern or southwestern tributary of the old Kanawha, but the presence of glacial 120 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. pebbles makes it certain that they were deposited by water moving south- ward. There is additional evidence that these deposits were derived from the Illinoian drift in the fact that the glacial pebbles show more weathering than is commonly displayed by similar rocks found in the Wisconsin gravel. Although these Ilinoian gravels have not been traced from the Scioto down the Ohio past the old divide, that course appears to have been the only available one for the stream which transported the gravel southward through the Scioto Valley. The gravels show a decided slope toward the Ohio from the glacial boundary. From an altitude about 700 feet above tide, at the point where the Scioto crosses the glacial boundary, just south of Chilli- cothe, their surface declines to about 650 feet near the mouth of the Scioto, 30 to 35 miles farther south. With the data now at command the writer is unable to make a definite estimate of the amount of trenching that had been accomplished in this part of the Ohio prior to the Hlhnoian stage of glacia- tion, but there was probably enough to give a downward slope from the mouth of the Scioto past the old divide near Manchester to the lower Ohio. There are features in the region which indicate that the trenching of the gradation plain had extended up the Scioto beyond the glacial boundary before the close of the Glacial epoch, but it is not entirely certain that the trenching had been accomplished prior to the Illinoian glaciation. The features referred to are found in the valley of the South Fork of Salt Creek. This valley, and also the abandoned portion of the old Kanawha, in southern Ohio, was greatly filled by silt deposits, which are apparently of glacial derivation, for they are in a sandstone region and yet are quite cal- careous. Boringsin the vicinity of Jackson, 20 miles above the mouth of the stream, show that the silt deposits on South Salt Creek extend below the level of the postglacial valley excavation, and are 40 or 50 feet lower than the rock floor of the abandoned part of the old Kanawha west of Jackson, less than 10 miles distant. The correlative rock floor of this val- ley should stand a few feet higher than the rock floor of the old Kanawha, since it had its discharge into that valley. he fact that it stands so much lower is a clear indication that the valley had been deepened fully 50 feet between the reversal and partial abandonment of the old Kanawha and the deposition of the silt. That this amount of trenching occurred here on a small tributary of the Scioto is a matter of far more consequence than if it had been found along the present Ohio, in the vicinity of the old divide, GLACIATION AND EROSION IN OHIO VALLEY. 121 or even on the Scioto. The time required would seem adequate for the Ohio to cut down the old divide about to the level of the Lower Ohio, with which it connected, and for the Scioto to have extended its trenching from the present mouth northward into the Scioto Basin far beyond the mouth of Salt Creek. Unfortunately there is an element of uncertainty as to the age of the silt which fills this trench. There is presumably a silt deposit in this valley which connects at the north with the Illinoian drift and perhaps silts of still earlier glacial stages. There was also in the Iowan stage of glaciation a widespread deposition of calcareous silt in this region, and the silts of the several stages have not been properly discriminated. If it can be shown that only the surface portion is of Iowan age and the deeper portion is Illinoian, the entire excavation would have occurred in pre-Illinoian time here, as well as in the Lower Ohio drainage system, and the two systems would probably have been connected at that early date about as at present. ON THE UPPER OHIO. It remains to consider the relation which the deposits that contain glacial material bear to the erosion features of the Upper Ohio. These deposits are of several classes and of different ages, and are found at all levels, from the rock floor under the river up to gradation plains which in one place attain an altitude nearly 400 feet above it. The deposits which occupy the valley bottom and rise to a height of 100 to 130 feet above the stream are generally referable to fluvial action during and subsequent to the Wisconsin stage of glaciation; but those which appear at greater heights are referable to earlier Pleistocene stages. At the Wisconsin stage the valley here as well as farther down appears to have been opened to its full depth. A sheet of drift much older than the Wisconsin, and probably also older than the [linoian, has furnished material for fluvial deposits which have been built up in the part of the Ohio Valley near the mouth of the Beaver to a height of about 980 feet above tide, or 100 feet above the main gradation plain, and 320 feet above the river. These deposits have as yet been found to cover the gradation plains of the old north-flowing system only as far as Toronto, Ohio, 35 miles below the mouth of the Beaver River. The surface of the gravel appears, from aneroid measurements, to descend in that distance 25 or 30 feet, being between 950 and 960 feet at Toronto. 122 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Between Toronto and Moundsville there are occasional remnants of gravel deposits, containing glacial pebbles, on slopes and narrow rock shelves below the level of the gradation plains and above the Wisconsin gravel terrace, but the amount is small compared with that between Beaver and Toronto. There are also small amounts of glacial gravel at higher levels than the Wisconsin terrace south of the old divide, from Mounds- ville down nearly to Marietta. In that part of the valley they are found on the old gradation plain as well as on the slopes below it, but, as above noted, the altitude of the gradation plain south from the old divide is much lower than that of the best defined gradation plain of the north-flowing system. The distribution of these deposits suggests that the valley at and above the old divide had been opened down about to the level of the gradation plain south of the divide prior to the culmination of the earliest glaciation, with its attendant deposition of the valley gravel. This subject, however, should not be dismissed until attention has been called to certain features which seem difficult to harmonize with the view - that considerable trenching across the old divide had occurred at the time of the first glaciation. On high rock shelves lying within the limits of the old north-flowing system south of Toronto there are scattering pebbles and thin deposits of loamy clay and fine sand. These deposits suggest a ponding of waters in the early stages of reversal, and there are suggestions of the presence of glacial material in the ponded waters. A deposit especially open to suspicion is a fine sand suitable for molders’ use, which has been obtained on the rock shelves near Wheeling and Bellaire at about 1,000 feet above tide, but its glacial derivation has not as yet been demonstrated. In this connection attention is directed to a feature that seems somewhat inharmonious with this view. The pebbles found on these rock shelves are usually of resistant sandstone, probably of local deriva- tion, and are deeply weathered; but on a rock shelf in the north part of Wheeling, standing 990 feet above tide, fresh-looking erratics were found. They are mainly small pebbles, an inch or less in diameter, of granite, green- stone, and quartzite. They are especially abundant in an open field south of the waterworks reservoir. Their fresh appearance, when in such an exposed situation, makes it seem doubtful if they were deposited by glacial waters at that high level. Possibly they have been brought up from a GLACIATION AND EROSION IN OHIO VALLEY. 123 terrace of Wisconsin age deep down in the valley, though upon inquiry no facts could be obtained to sustain this inference. From their general appearance they can scarcely be cited as evidence of the preservation of the old divide up to that altitude, but the molders’ sand may prove to be a point in support of that view. On the Ohio above the mouth of the Beaver, and also on the Lower Allegheny, glacial gravel has been found on the gradation plain all the way up to the supposed divide near the mouth of the Clarion, which is near the point where the Allegheny passes from the glaciated into the unglaciated region. It covers the gradation plain to a depth of 40 to 100 feet, the greatest filling being near the mouth of the Beaver, where the old drainage turned away from the present Ohio. The amount of trenching which this part of the old Upper Ohio had suf- fered before the deposition of the earliest glacial material is a matter which has been in controversy for some years. On the slopes of the trench which has been cut in the old gradation plain there are patches or thin sheets of glacial gravel which have afforded grounds for different interpre- tations, it being maintained by some that they demonstrate the preexist- ence of a trench at the time of the earliest filling with glacial material, while it has been held by others, among whom the writer is included, that they represent probably the incidents of degradation subsequent to the earliest filling. The following are the grounds set forth some years ago by Chamberlin and Leverett for doubting the preexistence of a deep trench:? Between the base of the undisputed high-level gravels and the summit of the low-level systems, gravel is found at numerous points on the sides of the Allegheny trench. This gravel is commonly found on sloping points in the inner bends of the river and in other localities where, in cutting down its valley, the river would be likely to leave remnants of gravels, if they were there before, or would permit their lodgment in the process of sinking its bed, if not there before. Herein lies the radical difficulty of their interpretation. A winding stream, which is cutting down its bed at a moderate rate, tends to extend its meanders as well as deepen its floor, and so it cuts outward as well as downward on the convexities of its bed and is dis- posed to permit the lodgment of material on its concave side, where the tendency of the stream is to recede. Now, the Allegheny, during the whole process of its descent from the level of the high terraces to its present position, was undoubtedly a gravel- bearing stream. It was not only engaged in the process of removal of the gravel along its own immediate course, but was receiving very much that was washed in from the drift region adjacent, so that a certain amount of lodgment of transported 1Am. Jour. Sci., 3d series, Vol. XLVII, 1894, pp. 275-277. 124 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. material may be assumed to have been inevitable. This is dependent upon the same principle of action that would permit the retention of gravels in such situations if they had been previously deposited within the trench. As the gravels on the slopes are usually thin sheets or patches, we have not found decisive evidence, in themselves, as to whether they are remnants of earlier gravels, or incidents of degradation. We have searched industriously for evidence that should be decisive on this point. Such evidence should be found in abandoned segments of the old valley, if it had been deeply excavated before the deposit of the gravels and had subsequently been filled by these up to the summit of high gravels. These high gravels fill oxbows and recessed shelves, and the stream which deposited them had, in many instances, alternative courses. This is notably true in the vicinity of Pittsburg. Here the old high plain of rock was extensively covered by the waters that deposited the gravels, as is shown by the presence of remnants. There are, in the eastern part of the city, four islands surrounded by broad channel ways, among which the waters distributed glacial gravels in greater or less degree. Now, if the present deep Allegheny and Monongahela trenches had been cut previously to the filling in of the gravels, there is only a small chance that, after the gravel-depositing period, during which they were flowing 50 feet or more above the rock plain, they would have descended the second time on precisely the same lines. Between the several broad channels open to them the possible combinations are 32 in number, and hence theoretically the chances of a combination repeating itself are one in 32. It it be objected that certain of the courses are more favorably situated than others, our answer is, first, why were these others then ever produced by the streams or occu- pied by glacial wash; and our second answer is, that if this be true of certain combi- nations, it does not seem to us to be at all true of many others. Besides this, along the Allegheny River above, and also along the Ohio River between Pittsburg and Toronto, to which point the high gravels containing Canadian pebbles have been traced, there are perhaps a score of oxbows, deep recesses, shelves, or available cols which would afford opportunities for the redescending river to locate itself on other lines than its old track with all its meanders. When these possibilities are added to the preceding it becomes exceedingly strange that, below the mouth of the Clarion, no abandoned channel is found which retains any old filling comparable in depth to the present trench. We find numerous channels containing gravels ranging from 50 to a little over 100 feet that represent such old courses on the higher plain. This demonstrates the truthfulness of the principle here urged, and shows its application to this particular field. The hypothesis that the river trenches of this region had been cut to essentially their present depth before the earliest glaciation encounters another serious difficulty in that it calls for a greater amount of valley filling than can well be postulated. It necessitates enough valley gravel during that glaciation to produce a filling fully 300 feet in depth for a distance of at least 250 miles, and that, too, while the ice edge occupied the narrow belt between the glacial boundary and the basin of Lake Erie. The amount of material RATE OF FALL OF ALLEGHENY RIVER. 125 required to spread a deposit 40 to 100 feet in depth over the surface of the gradation plain seems surprisingly great when the limited extent of elaciated country tributary to this drainage system is considered, but this must be doubled or trebled to fill the trenches. It would be far in excess of the outwash from the Wisconsin, for that has been sufficient to fill the trench to an average depth but little more than 100 feet, and it had the advantage of contributions from the earlier gravel deposits all along the line. It should not be inferred that the gradation plains of the Upper Ohio region had reached only an incipient state of trenching down to the time when those of the Middle and Lower Ohio had suffered trenching to their full depth. The glacial deposits of the Upper Ohio region apparently belong to a stage of glaciation much earlier than that which furnished the drift of the Lower Ohio region. The latter is of Illinoian age, while the former, as indicated below, seems to be fully as old as the Kansan drift, if not of pre- Kansan age. A sufficient amount of valley trenching may have occurred in the Upper Ohio region between the earliest glaciation and the Illimoian stage to bring it into harmony with that of the Lower Ohio system. The precise amount of trenching can scarcely be estimated in the present stage of investigation. ALLEGHENY RIVER. The Allegheny River, the main headwater tributary of the Ohio, drains an area of about 11,500 square miles, 2,000 square miles being in south- western New York, and 9,500 in northwestern Pennsylvania. The river rises in Potter County, Pa., near the sources of the Genesee and the Sus- quehanna, and runs northwestward into southwestern New York. It there turns southwestward and holds this general course to its mouth at Pitts- burg. The length of the valley is about 325 miles. The length of the stream is but little more, for throughout much of its course its meanders conform to the windings of the valley. In the headwater portion, for about 160 miles, the curves are less sharp than in the lower portion of the valley, though the course is far from direct. In the lower portion the valley makes several sharp oxbow loops, in some instances nearly severing the prominent ridges inclosed by them. RATE OF FALL. The source of the river is near the crest of the Allegheny Mountains, in passes which stand about 2,200 feet above tide. The highest ridges in 126 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. that vicinity exceed 2,500 feet. In the first 20 miles, to Coudersport, Pa., the fall is very rapid, but below this point the valley has been silted up and the rate of fall becomes very much reduced. In the 30 miles from Port Allegany, Pa., to Olean, N. Y., the fall is only about 50 feet, or less than 2 feet per mile, and this low rate continues to Salamanca, 20 miles below Olean. The following condensed statement of the fall of the river from Olean to Pittsburg is taken from Roberts’s Report on the Survey of the Allegheny River." Fall of Allegheny River from Olean, N. ¥., to Pittsburg, Pa. Feet per mile. Tait; BO) anvils loelkonyy OlleHin «22-55 ccscces] soe 25 sec scces os nde oa soe ceea sense csesesesssoccercss 1.7 Seeondl 20 mules... 5.55553s22sccctesce seco cce=2 soneb cose onsas cones coouosesereseassecoseses 8.7 Taine! HO) mallee. 2. 2 se ones ne ee secesoc scene neces ee oborossssraneose seas sacsecoccesscsceesse 5.0 Woyowla YO) wales. 222) oe pee se Sad sseece cst bet eoscoceas cose esas masosoessossesessersessece 3.5 IPH AO Tolley 2s. We ease scgcesc: ecoc ee esse sees cosese cece sen smass ssesaossecesseere 3.5 Thirty-two miles to Franklin _......_.-.------------------------------------------+--------- 3.0 [piermalkelliin tio) Wemiislownge, 23) iolles .. ono 2 eee 25) seoesee cece nee se secossossessoscosesesssesesse5 Pil Average Olean to Pittsburg, 255 miles --.-..-. .---------------------------------------------- 2.8 Average Olean to Franklin, 132 miles ----.-----------.------=2-------=---------------------- 3.4 From the same report it appears that there are 190 riffles between Olean and Franklin, with an average length of 617 feet and an average descent of 1.6 feet. These riffles have a combined length of 22.2 miles and an aggregate descent of 304.77 feet. This leaves 141.49 feet descent for the 110 miles not occupied by riffles, or a descent of less than 1.3 feet per mile. From an earlier report by Roberts” it appears that between Frank- lin and the mouth of Conemaugh River, 30 miles above Pittsburg, there are 58 riffles, with an average length of 1,460 feet and an average descent of 2.46 feet. There are 11 riffles in the lower 30 miles of the river, but their length and descent have not been ascertained. The most formidable riffle in the entire length of the portion surveyed is ‘“MeGinnis Rapids,” about 8 miles above the mouth of the Clarion River, where a descent of 11.23 feet is made in a distance of 6,900 feet. This is described to be a connected series of rapids, shoalest at the head. About one-half mile above the head of the rapids the river has a rock bed, but it is not certain that the rapids are over rock ledges; nor is it certain that the rock ledge over which the river flows extends entirely across the valley at a level as high as the river bed. 1Senate Doc. No. 89, Forty-sixth Congress, second session, 25 pages. 2 House Doc. No. 21, Forty-fiith Congress, third session, 17 pages. ROCK FLOOR OF ALLEGHENY RIVER. WF In this connection it may be remarked that the river has a rock bed at but few places in its entire length, and the rock floor lies usually 20 to 50 feet below the stream. In the headwater portion, as indicated below, it lies at a great depth below the stream; yet in that portion a rock ledge is crossed by the stream at Limestone Falls, about 7 miles above the point where the river returns from New York into Pennsylvania, and a fall of 3.84 feet occurs in a distance of 650 feet. The stream there is near the left bluff, and a buried channel is to be expected in the middle of the valley that will extend perhaps 200 feet below river level. ROCK FLOOR. In the upper 20 miles of its course the rock floor is but little below stream level, but in the next 20 miles it becomes covered to a depth of about 200 feet, while at Olean, and for nearly 30 miles below that city to Cold Spring Creek, it is covered to a depth of fully 300 feet. From the mouth of Cold Spring Creek, near Steamburg, N. Y., the Upper Allegheny, as indicated by Carll, formerly led away from its present course to enter the Lake Erie Basin.” Down the present Allegheny from Cold Spring Creek the rock floor shows a rise of about 150 feet in the 25 miles to Great Bend, Pa., 8 miles above Warren, where the old divide pointed out by Carll has been crossed. It drops about 70 feet in the 8 miles to Warren, below which, for 10 miles or more, it appears to hold a nearly uniform level about 1,100 feet above tide. A descent then begins, which apparently continues the entire 175 miles to the mouth of the stream, at a level 20 to 50 feet below low- water level. In this lower end of the valley, therefore, it resembles the rock floor of the Ohio, but in the upper part its relation to the present stream is different. Although the rock floor in the lower end of the valley shows a descent with the present stream, it does not follow that there has been no change of drainage. Here, as on the Ohio, the old divides have been cut down below the level of the stream sufficiently to give a gradient in harmony with it. But in the upper part of the Allegheny the old streams flowed in plains so far below the level of the present river that their rock floors have not been touched by it. 1Roberts’s Report, Senate Doc. 89, Forty-sixth Congress, second session, pp. 13 and 23. 2Second Geol. Survey Pennsylvania, Rept. I°, 1880, pp. 333-355. 128 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. DESCRIPTION OF THE VALLEY. At the source of the Allegheny the dividing ridges between the Alle- gheny, Genesee, and Susquehanna rivers have an altitude of 2,500 to 2,600 feet. Down the Allegheny the highest points on bordering uplands fall to about 2,500 feet near Port Allegany, to 2,425 feet near Olean, to 2,375 feet near Salamanca, and to perhaps 2,200 feet in the vicinity of Steam- burg, where the present channel departs from the old one. There is a slight rise southward from that point to the old divide near Kinzua, Pa., the uplands reaching an altitude of 2,150 feet on the immediate borders of the valley west of Kinzua. From this point there is a general descent toward the mouth of the present river, the altitude near Warren being about 1,950 feet, near Tidioute 1,750 feet, near the mouth of the Clarion River 1,550 feet, and near Pittsburg 1,200 to 1,300 feet. A comparison of these altitudes with the altitudes of the stream shows that the stream flows at a level 500 to 800 feet or more below the highest parts of the bordering uplands, while the rock floor in the deeply filled portions in northern Pennsylvania and southwestern New York was cut 1,000 to 1,100 ° feet below the bordermg uplands. The course of the stream, as may be seen by reference to the glacial map (Pl. IL), lies within a few miles of the glacial boundary, a large part being just outside the limits of the drift and none of the valley far inside the drift border. The Allegheny Valley increases gradually in width in fhe northwest portion from its source to the point where the present stream departs from the old course near Steamburg, N. Y., the width being one-fourth to one- half mile from Coudersport to Port Allegany, and one-half to three-fourths mile from Port Allegany to the bend just above Olean, N. Y., below which, as far as Cold Spring Creek, the width is a mile or more. Southward from the mouth of Cold Spring Creek the valley maintains a width of a mile only as far as the vicinity of the State line. From Corydon to Kinzua, Pa., it has a width of scarcely three-fourths of a mile. At the old divide below Kinzua it narrows abruptly to a width of but one-fourth mile, and remains narrow nearly to the mouth of Conewango River at Warren. It there expands to a width of about a mile, and main- tains this width from Warren to the bend near Irvineton, a distance of 8 miles. Upon passing south from Irvineton it soon decreases to less than one-half mile, being much narrower than the valley of Brokenstraw Creek, a> RL aD AA” Meso. BD Aly ge. aE ey gerigte OLD UPPER ALLEGHENY DRAINAGE SYSTEM. 129 which enters the Allegheny at Irvineton. It continues narrow as far as the mouth of the Clarion River, being in places scarcely one-fourth mile, and rarely exceeding one-half mile, in width. In this narrow portion there are occasional remnants of the fluvial plain of the small predecessor of the middle portion of the Allegheny, which, as indicated below, discharged northwestward along French Creek (reversed), and eventually reached the Lake Erie Basin. At the mouth of Clarion River a broad gradation plain comes in from that valley and continues down the Allegheny to its mouth. This has been trenched to a depth of about 200 feet below the level of the old rock floor. The trench or inner valley is usually about one-half mile in width, though it increases to nearly a mile near the mouth of the stream. At the level of the gradation plain there is a general width of about 1 mile. This grada- tion plain is capped by a deposit of sand and gravel, with an average thick- ness of perhaps 40 feet, that serves to accentuate the terrace-like appearance, for it fills up small trenches that had been cut in the gradation plain prior to the gravel fillmg. It is scarcely necessary to state that above the level ‘of this gradation plain the bluffs are far more worn and receding than in the inner or canyon valley lying below it. OLD UPPER ALLEGHENY DRAINAGE SYSTEM. Evidence that the upper portion of the Allegheny drainage basin for- merly discharged northwestward to the Lake Erie Basin was presented by Carll some twenty years ago.’ He called attention to the constriction of the present valley near Kinzua, Pa., and noted that the rock floor of the valley slopes northward or in the reverse direction from the present stream from this point to the mouth of Cold Spring Creek, where it is met by a a rock floor sloping with the present stream. He also noted a broad valley deeply filled with drift leading westward from the mouth of Cold Spring Creek to the headwater portion of Conewango Creek. Having no opportunity to examine the divide at the head of Conewango Creek, he suggested an outlet to the Lake Erie Basin along the rather broad valley of Cassadaga Creek, a tributary of the Conewango. In this suggestion he seems to have been in error, for a much broader valley leads northward across the low divide between Conewango and Cattaraugus creeks, and 1Second Geol. Survey Pennsylvania, Rept. I’, 1880, pp. 1-10, 330-439. MON XLI——9 130 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. thence down Cattaraugus Creek to the lake. In favor of the route across the divide between Conewango and Cattaraugus creeks there is not only the greater width of the valley, but also its more direct course to the lake basin and the presence of a channel deeper than is known to be preseut in the Cassadaga Valley. Three wells along it penetrate drift to depths of 284, 314, and 330 feet, respectively, without reaching rock, while a fourth, in Cattaraugus Valley, at the Indian Asylum near Versailles, penetrated about 200 feet of drift. The northward slope of the rock floor and:its wide departure from the bed of the present streams is in part shown diagramatically in fig. 4. Ona subsequent page it is shown that on this line, as well as on other ancient drainage lines of this region, the northward slope of the rock floor may be somewhat modified by surface warping. There may also have been consider- Randolph State Line Dayton (OG ie i Coryde Kinzua g ‘ Corydon 1325" : 1320" 7300" i 1256" TAS Bal Warren ' Conewango River \ = | Allegheny ' River we NR ade Q 10 20 miles Fic. 4.—Diagram to show the relation between the present stream bed and the old rock floor along the preglacial Upper Allegheny River. The numerals above the stream bed indicate surface altitudes, while those below show the depth to which wells have penetrated. The sign (?) indicates that rock was not reached. able rock excavation by an interglacial stream along this line in the vicinity of the lake basin, it being not improbable that an interglacial stream would have had its source somewhat south of the present divide, which is a moraine of Wisconsin or late glacial age. Both factors need to be elimi- nated in determining the rate of slope of the rock floor of preglacial times. The present rate seems too great for the nature of the valley. It may also be necessary to make allowance for excavation by ice or by currents of water underneath the ice in the portion of the valley within the glacial boundary, but such an excavation could not have occurred in the portion of the valley with northward-sloping floor which lies outside the glacial boundary, i. e., between Kinzua and Cold Spring Creek. The general configuration of the drainage features of the region sup- port this view of reversal or change in drainage, as may be seen by refer- ae wae —. caiman OLD UPPER ALLEGHENY DRAINAGE SYSTEM. 131 ence to the map of the restored drainage (fig. 1, p.89). The naturalness of this restored system lends support to the more positive evidence just cited. It should be noted that the old divide between the small streams which flowed south into the Upper Allegheny and those which flowed north into Cattaraugus Creek was farther south than the present divide. Above the village of Ischua the headwater portion of Ischua Creek appears to have discharged northward past Machias to Cattaraugus Creek. The changes on the headwaters of other tributaries are of less consequence. Cattaraugus Creek departs somewhat from the ancient line of drainage, as noted in the discussion of that stream. It is somewhat difficult to decide upon the extent of the basin drained by the western tributaries of the old Upper Allegheny, for the valleys and lowland tracts have been so greatly filled by glacial deposits that the old divides are concealed. Probably much of the draimage areas of Cassadaga Creek, Chautauqua Lake, and the lower portion of Conewango Creek were tributary to the Upper Allegheny along the valley leading from Jamestown eastward to Randolph, N. Y. It is possible that the Conewango Valley was a line of northward dis- charge for a small section of the present Allegheny between the old divide near Kinzua and a divide near Thompson station, about 12 miles below Warren, Pa., and also for the part of the Tionesta drainage basin above Barnesville, Pa. It is certain that the upper portion of the Tionesta dis- charged northward through Glade Run to the present Allegheny at Warren, as pointed out by Carll. The old divide where reversal took place is readily located near Barnesville, where, as noted by Carll, the stream enters a narrow gorge scarcely one-fifth the width of the abandoned channel. It also seems evident, from a constriction of the Allegheny Valley that sets in near Thompson and from other features discussed below, that the discharge could not have been down the present Allegheny. The only element of uncertainty is the course of the drainage—whether it was northward through the Conewango reversed, or westward through the lower course of Brokenstraw Creek and a deeply filled broad valley connecting Broken- straw Creek with Oil Creek along the line of the Dunkirk, Allegheny Valley and Pittsburg Railway. The rock floor in the lower course of Conewango Creek and on the Allegheny between Warren and the mouth - of Brokenstraw Creek is shown by numerous oil borings to be nearly level, 132 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. while on the old line of northward drainage for the Tionesta and on the portion of the Conewango north from Russellburg, Pa., the rock floor shows a perceptible northward slant. This singular feature may perhaps be due to a recession of the Thompson col through valley excavation, as suggested by Carll,’ and the formation of a pseudo-col north of Warren at a point where excavation and recession were interrupted by a later filling with glacial gravel. The valley leading westward from the lower course of Brokenstraw Creek into the Oil Creek Basin has been insufficiently tested by borings to furnish satisfactory evidence concerning the slope of its rock floor or the altitude of the floor compared with that of the Lower Conewango. A decision between these two routes can scarcely be rendered until a better knowledge of the western line is obtained. OLD MIDDLE ALLEGHENY DRAINAGE SYSTEM. This basin includes the lower portion of the Tionesta (below Barnes- ville post-office), the Allegheny from the old col at Thompson’s to near the mouth of the Clarion, and the tributaries of this part of the Allegheny, except the headwaters of Oil and French creeks, as indicated in fig. 6. Several lines of evidence unite in indicating that this district formerly discharged northwestward along or near the lower course of French Creek nearly to Meadville and thence past Conneaut Lake to Conneaut Creek and the Lake Erie Basin. Evidence in favor of the reversal in the part below the mouth of French Creek is found in the narrowness of the Allegheny Valley above the mouth of the Clarion, as compared with the Clarion- Lower Allegheny Valley. Evidence is also found in an elevated tract which is crossed by the Allegheny immediately above the mouth of the Clarion, and in the rock shelves or old rock floors of the Allegheny and French Creek valleys. Attention has already been called (p. 129) to the broad gradation plain, a mile or more in average width, which follows the Lower Allegheny at a level about 200 feet above the present stream, and to the fact that this gradation plain follows up the Clarion, but does not extend up the Allegheny above the mouth of the Clarion, for that part of the Allegheny has a narrow valley with precipitous blufts reaching a height of nearly 400 feet above the stream. 1Second Geol. Survey Pennsylvania, Rept. I*, 1883, p. 311. \ ! i . i . f . OP AONE ted MCS tly 144 OLD MIDDLE ALLEGHENY DRAINAGE SYSTEM. 133 The force of this evidence has also been noted in showing either that a disproportionately small gradation plain with high cliff borders lay in this narrow gorge (having a breadth of only one-third to one-half that of the Clarion and Lower Allegheny gradation plain) or that there has been a reversal of drainage by which a small stream that formerly flowed north- westward through this gorge to join the French Creek—Conneaut outlet was reversed and its valley recut to fit the new and larger stream. The' balance of probabilities in favor of the latter has also been set forth. There seems to be evidence that the portion of the present Allegheny between the supposed col near the mouth of the Clarion and the French Creek outlet has been derived from parts of two valleys, each discharging northwestward, but separated by a divide below the mouth of East Sandy Creek. This view is supported not only by a notable constriction there (to a width of scarcely 1,000 feet) but also by an abandoned valley leading northward from the bend of West Sandy Creek at Polk (Waterloo) to French Creek Valley, just above the mouth of Sugar Creek, which would afford a northward outlet for the western stream. The relationships of the present streams to this abandoned valley and to the supposed col may be seen by a comparison of figs. 5 and 6. This comparison will also serve to show how natural is the restored system compared with the disturbed and unnatural present system. Turning next to the line of evidence found in the rock shelves and terraces, a general inspection of the French Creek Valley shows that there has been broader and deeper excavation than on the Middle Allegheny. But inasmuch as the French Creek Valley lies within the glacial boundary, and its lower course nearly coincides with the direction of the ice flow, it seemed necessary to determine whether its greater size may not be due in the main to glacial excavation. An examination of the valley with this question in mind led to the discovery of old channels and ox-bow curves of preglacial streams whose preservation is so complete as to furnish decisive evidence that glacial excavation has been of little consequence in causing the size of the southern end of the valley. Along the valley which led past Waterloo from the highland tract near the mouth of the Clarion to the present French Creek Valley there are remnants of an old valley floor near the supposed divide at an altitude of 375-400 feet above the river, or 1,275 to 1,300 above tide, while at Waterloo, 134 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. in the abandoned valley which leads from Sandy Creek northward to French Creek, the rock floor is shown by several oil wells to have an altitude about 1,050 feet above tide. This valley is filled with drift apparently of early glacial age, and its rock floor has not suffered excavation since the drift deposition. Its rock floor is the probable continuation of the elevated rock floor of the headwaters and indicates a descent of somewhat more than 200 feet in 18 to 20 miles. This rate of fall would be natural in sucha small stream descending from the elevated table-land, and differs but little from the rate of fall in south- ern tributaries of the upper Alle- gheny of corresponding size—e. g., the fall on the Tuna, a similar stream, from De Golia, Pa., to the mouth of the stream, a distance of 14 miles, is 215 feet... At the north end of the abandoned valley, where it opens into French Creek, a rock floor is struck in wells at an alti- tude about 975 feet above tide, which seems to mark the continua- tion of the old valley floor. Turning now to the main stream of the old Middle Alle- gheny, it appears probable that the Heer drainage of part of the Middle Allegheny col at Thompson’s had a height of Gre a ea at least 1,220 feet. At Tidioute, 8 miles below, early glacial gravels rest on a rock shelf that represents the old river bottom at 1,160 feet above tide. At Reno a similar shelf stands only 1,040 feet; while at Franklin, in an oxbow filled with early glacial gravel (see Pl. VIII), one boring reached rock at 1,040 feet above tide, and another penetrated to a level only 1,015 feet above tide without reach- ing rock.. The gravel at these points rises to a level much above that of the terraces connected with the outer moraine of the Wisconsin or late ice inva- 1See Carll: Second Geol. Survey Pennsylvania, Rept. I’, p. 334. OLD MIDDLE ALLEGHENY DRAINAGE SYSTEM. sy sion, and sustains such relations as to show clearly that it has suffered no dis- turbance since deposition. The shelves, therefore, antedate the gravel, and are remnants of an old river bottom. The hill standing between the old chan- nel and the present river (see PI. VIII) seems to have been detached from the bluff south of the river. This change was probably brought about at the time the valley became filled greatly with glacial gravel, the amount of filling being sufficient to raise the stream above the level of the old neck that joined the hill to the south bluff. Following the supposed out- let northwestward, there is an old meandering valley lying near the present French Creek and in part coinciding with it (see fig. 5). On & a small eastern tributary of this old y . ~ aterloo valley 3 miles northwest of Frank- > ms 2 . 3 = lin, wells situated a mile or more A S pAlegreny Old Col. an S- back from the junction of the trib- utary with the old valley strike a ennerdell ( rock floor at about 1,040 feet above tide, which is about as low a level as the rock floor found in one of the wells in the Franklin oxbow, and is within 25 feet of the bottom of the other. These wells pene- 01 trate about 100 feet of drift of early glacial age. As they are Scale of miles 24 6 8 10 12 Fic, 6.—Probable preglacial drainage of part of the Middle back from the principal valley, the See ea aae Sea presumption is that the main channel is lower. Farther northwest along the valley, at a point 8 miles from the Allegheny, a well is found which reaches the rock floor at 1,025 feet above tide—i. e., at a depth intermediate between the depths of the two wells in the abandoned oxbow at Franklin. This well is situated near the southern edge of the valley and can scarcely be sup- posed to have struck its deepest portion. Again, in an old oxbow 3 miles north of Utica, similar in every way to the oxbow at Franklin except that it lies within the limits of the Wisconsin ice mvasion, the floor is shown by 136 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. one well to be 945 feet and by another 960 feet above tide—i. e., 70 feet and 55 feet, respectively, below the bottom of the lowest well in the Franklin oxbow. Still farther northwest, on French Creek, at Cochranton, Buchanan, and Meadville, there are wells showing excavation to even greater depths; the first two not reaching the bottom at 915 and 800 feet above tide, respec- tively, and the last finding rock at 605 feet above tide. The depth of drift at this last point is reported to be 475 feet, and the rock bottom is only 382 feet above Lake Erie. The low altitude at Meadville seems to be confined to a narrow trench,-for within short distances either side the rock floor is 100 to 200 feet higher. The conditions here are somewhat problematical, as in the north end of the old Upper Allegheny. The evidence seems very strong that the oxbow at Franklin, the old channel northeast of Utica, and the oxbow north of Utica are remnants of the floor of the same old meandering stream leading northwestward. The fact that the rock floor in the oxbow north of Utica is 70 feet below the deepest determination of the old channel where it left the present Allegheny renders it highly improbable, if not impossible, that it was formed by a stream discharging toward the Allegheny. It is even lower than the present rock bottom of the Allegheny, notwithstanding ail the erosion the latter is believed to have suffered since the deposition of the early glacial gravels. It is highly probable, therefore, that we have in these abandoned valleys a continuation of the old Middle Allegheny. An inspection of the general configuration of the old channel, as shown in fig. 6, will add to the force of these considerations. An objection to the northwestward outlet may perhaps seem to be presented by deposits of gravel which occur along the Allegheny Valley between the mouth of French Creek and the mouth of the Clarion. In several places, notably at the bends of the river at Brandon, at a point 2 miles below Brandon, at Kennerdell, at Black’s (Winter Hill station), and at Emlenton, there are deposits on the face of the gorge extending from ‘near the river’s edge up to heights of 200 to 300 feet or more above the stream. The occurrence of this gravel at low levels can not be accounted for by creeping or landslides, since in some places, notably at Kennerdell and 2 miles below Brandon, the gravels show clearly by their situation and bedding that they have not been disturbed since the stream deposited them. We are not, however, reduced to the one interpretation that the valley had ee ee ou. S._ GEOLOGICAL SURVEY MONOGRAPH XLI PL. VIII —— Eo C—AGAAA LZ OLD MIDDLE ALLEGHENY DRAINAGE SYSTEM. aif been opened to its present depth and had southward drainage before the beginning of the glacial period. These gravels are in every observed case situated on sloping points on the inner curves of sharp bends in the river. At such places a stream works outward as well as downward, there being erosion on the outer curve and liability of deposition on the inner curve. It is to be expected, therefore, on the hypothesis that the stream has greatly deepened its channel since the ice invasion, that such deposits should be present, and these deposits do ‘not, it is thought, necessarily oppose the hypothesis of former northwestward drainage, nor that of great erosion since the beginning of the Glacial epoch. Concerning the line of discharge for the Middle Allegheny from near Meadville to the Lake Erie Basin a few remarks seem necessary. It is certain that the old drainage line did not follow French Creek Valley northward beyond Meadville, for there is clear evidence of an old divide on the present creek a short distance above that city. The line described by Carll as the Conneaut outlet departed from French Creek about 4 miles below Meadville, followed up the outlet of Conneaut Lake to that body of water, passed northward across a low divide filled heavily with drift to the northward-flowing portion of Conneaut Creek, passed down that creek to the bend near Albion, then continued northward and entered the Lake Erie Basin a few miles east of the Ohio-Pennsylvania line. Another valley-like lowland leads from Meadville along Cussewago Creek (reversed) nearly to its source, and thence northwestward to the Conneaut outlet near Albion, through a region heavily covered with drift. The Cussewago channel is narrower than the Conneaut and seems, on the whole, a less probable line of discharge for the Middle Allegheny. The northern end, however, afforded a line of discharge for a portion of the French Creek valley above Meadville, as indicated on page 139. On both the Conneaut and Cussewago channels the borings are too few to afford a satisfactory knowledge of the rock floor. At the border of Lake Erie, for several miles each side of the place where the old stream entered, the rock surface seldom rises above lake level. It is probable that the channel of the old stream had reached a level in harmony with the bed of the lake. It was suggested by Carll’ that the headwater portion of the Shenango 1Second Geol. Survey Pennsylvania, Rept. I*, pp. 5-6. 138 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. connected with the Conneaut outlet along the line of the old Beaver canal. In apparent support of this view, there is found to be a very low divide on this line composed of drift. But within a short distance back from the canal on either side rock appears above the canal level, a feature which suggests that the drift here covers a low rock ridge instead of an old chan- nel. It seems probable, therefore, that the middle Allegheny received very little of the present Shenango drainage. OLD DRAINAGE BETWEEN THE UPPER AND MIDDLE ALLEGHENY DRAINAGE SYSTEMS. The greater part of Brokenstraw, Little Brokenstraw, Oil, and French Creek drainage basins appear to have been largely independent of either the Upper or Middle Allegheny. Instead of discharging, as now, in a southeastward direction to the Allegheny, they appear to have taken a northwestward course to the Lake Erie Basin. Only a smal! part of the ancient drainage can be readily traced, owimg to the deep filling of drift, -vhich completely conceals many of the low divides and renders it difficult, if not impracticable, to locate them. The borings, also, are not sufficiently numerous to afford a satisfactory knowledge of the slope of the rock floors, except in a few localities especially favored by oil-well borings. The present discussion can therefore set forth only a few of the points which bear upon the ancient courses of drainage. The enlargement of Oil Creek, a small northern tributary of the Mid- dle Allegheny, was brought to notice by Carll.’ He called attention to the old divide just south of Titusville, and to the fact that im the part of the present creek above this divide the rock floor slopes toward the Lake Erie Basin. The region now drained by French Creek seems to have suffered greater changes than that drained by Oil Creek. Indeed, the present stream appears to unite several areas which were drained by distinct lines. The lower course, as already indicated, formed the old line of discharge for the Middle Allegheny, while a small section in the middle of the present valley was occupied by the stream which drained the headwater part of the present Oil Creek Basin, and which may be called Muddy Creek, from the stream which now connects it with the Allegheny. Between these two lines of drainage there was a smaller line which crossed the present French 1 Op. cit., pp. 856-360. ee ee ee ee eee. SS — OLD DRAINAGE FROM UPPER TO MIDDLE ALLEGHENY. 139 Creek Valley at Saegerstown, which may, perhaps, be denominated the old Woodcock Creek, since a stream by that name now drains the headwater portion of the valley, entering French Creek at Saegerstown. French Creek crosses another old divide in the extreme southwest corner of New York. The drainage systems thus united may never have been entirely distinct, but they certainly have been greatly modified in their courses and connections. The old Woodcock Creek passed directly across French Creek through a depression, now deeply filled with drift, which leads past Mosiertown to Cussewago Creek, from which it apparently continued northwestward near Crossingville and Pleasant Valley to the old Middie Allegheny or ‘Con- neaut outlet” in the vicinity of Albion, Pa. At the point where the old stream crosses French Creek the width is nearly one-half mile, or about double that of the present valley of French Creek just above and below the line of this old valley. Although this ancient line drained an area much smaller than the present French Creek, its age was so many times greater than that of these new portions of the creek that the amount of excavation is greater. Wells at Saegerstown enter rock at only 30 feet below French Creek, or about 1,070 feet above tide, but it is probable that the deepest part of the old valley has not been struck by them. These wells, however, stand in the midst of French Creek Valley, and bear strong testimony to the absence of a deep channel between Saegerstown and Meadville. The old divide crossed by French Creek on each side of the old Woodcock Creek apparently stood but 50 to 60 feet above the present creek; at least the rock rises no higher than that on the immediate borders of the stream. No difficulty was experienced by Carll in tracing the old upper part of the Oil Creek drainage northwestward to French Creek through the broad lowland now oceupied by Muddy Creek; but the line of discharge from French Creek to the Lake Erie Basin was not so readily determined. There appear to be rock barriers on the line of the two principal lowlands leading from French Creek toward the basin, one of which is drained by Le Beeuf Creek and the other by Conneautee Creek. On account of these apparent barriers the old line of drainage was thought by Carll to have followed down the present course of French Creek to the Conneaut outlet near Meadville. In giving the stream this route he apparently overlooked 140 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the two old divides just noted, one of which is crossed by French Creek between Cambridge and Saegerstown, and the other between Saegerstown and Meadville. The presence of these old divides makes it necessary to give the stream a different course from Cambridge to the lake. The great amount of drift in the region through which it must have passed has nearly, if not quite, concealed the line of discharge, hence it is not possible at present to trace the line through to the lake. As indicated in the discussion of the Upper Allegheny, there is a possi- bility that a small section of the Allegheny, together with the headwater portion of Tionesta Creek and the lower course of Conewango Creek, formerly discharged southwestward into the upper part of Oil Creek drain- age basin past Grand Valley, carrying with it the lower courses of Broken- straw and Little Brokenstraw creeks, as well as several smaller streams now tributary to the Allegheny. This being the case, a much larger stream than the present headwater portion of Oil Creek (above Titusville) dis- charged through Muddy Creek channel. It seems more likely, however, as suggested above, that the drainage of this section of the Allegheny was northward through the Conewango. The valley at Titusville is nearly a mile in width, and becomes gradually larger upon passing northwestward along the line of the Muddy Creek channel, the width being nearly 2 miles along the portion of French Creek between the mouth of Muddy Creek and Cambridge. It is several times the size of the small valley which now forms the lower course of Oil Creek. The headwater part of Oil Creek drainage basin was excavated to a level below that of the lower part; that is, of the small drainage line south of the divide. The valley floor at Titusville, as shown by numerous oil wells, is only 1,100 feet above tide, and it falls to 1,034 feet in the Muddy Creek channel, 7 miles northwest of Titusville,’ thus reaching an elevation tion about as low as the lower Oil Creek reached at Oil City on the Middle Allegheny, 18 miles below Titusville as the stream now flows. The old divide near Titusville is found to consist of a narrow ridge situated but a short distance south of the line of the old upper Oil Creek. It was apparently quite similar to the divide at the head of Pithole Creek, a few miles east of Titusville, which almost overlooks the valiey of a head- water tributary of Oil Creek and yet stands about 400 feet above it. The 1See Carll, op. cit., pp. 357-358. OLD DRAINAGE FROM UPPER TO MIDDLE ALLEGHENY. 141 divide at the head of Pithole Creek rises to a height of 1,640 feet above tide, and the rock surface is about 1,560 feet, while the rock floor in the valley on the north is less than 1,200 feet. It is scarcely probable that the divide crossed by Oil Creek south of Titusville stood quite so high. The gap made by the creek is bordered by abrupt bluffs up to a height of only 1,320 feet, which probably marks the height of the old divide. South of this old divide is the small valley of the old lower Oil Creek, leading to the Allegheny at Oil City. Its width, including rock shelves, averages scarcely 100 rods, while the width inside the rock shelves is in places but 40 to 60 rods. It is similar in size to Pithole Creek Valley, which drains a small district on the east. This small valley had been excavated nearly to the present level of Oil Creek before the culmination of the earliest glaciation, for low rock shelves on its borders 40 to 60 feet above the stream are thickly covered with early glacial deposits. Its valley floor is in harmony with that of the neighboring portion of the Middle Allegheny, which was excavated nearly to the present stream level before the glacial deposition took place. An abandoned oxbow channel west of Petroleum Center has a rock floor as low as the creek level, 1,090 feet above tide, and yet it seems not improbable that its excavation preceded the drift deposition. At the Boughton Acid Works, within a mile south of the old divide, the valley floor appears to have stood only about 1,200 feet above tide, or 40 to 50 feet above the creek at the time the reversal took place. The headwater portions of French Creek and Little and Big Broken- straw creeks evidently have been greatly modified by the obstruction of old lines of drainage. In several places the waters now divide in the valley-like lowlands which probably were formed by ancient streams. It is probable that the headwater portion of Little Brokenstraw Creek discharged into the valley now occupied by Lake Chautauqua, there being an abandoned valley along the line of the Erie Railway from this creek at Grant, N. Y., to Lake Chautauqua. Evidence that the headwater portion of this creek was once distinct from the lower course is found in the lower altitude of its rock floor, and also in the fact that the headwater portion is in a larger valley than the lower course of the creek. A boring at Lottsville, Pa., in the headwater portion of the creek reached a level 150 feet below the rock floor at the mouth of the creek without entering rock. \ 1See Carll: Second Geol. Survey Pennsylvania, Rept. I*, 1883, p. 311. 142 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. It was suggested by Carll’ that currents under the ice may in this instance have excavated to a considerable depth below the level of the main outlet, but it seems hardly necessary to assume that so much excavation had been made through this agency. It is Carll’s opinion that the old drainage was northward from Lottsville to the valley of Lake Chautauqua through the abandoned valley just noted. Possibly a part of Big Brokenstraw Creek also discharged to the Lake Chautauqua Valley and carried with it the headwater portion of French Creek, there being lowland connection with Little Brokenstraw along Coffee Creek and Swamp Run near the north line of Pennsylvania and also from Clymer, N. Y., eastward into the headwaters of Brokenstraw,and the abandoned valley referred to above. But it seems more probable that the headwater portion of Big Brokenstraw Creek connected toward the north or west with French Creek and found a northward discharge to the Lake Erie Basin. The lowlands connecting Big Brokenstraw with French Creek are broader and have a slightly lower altitude than those connecting it with Little Brokenstraw Creek. At Corry a broad lowland deeply filled with drift connects Big Brokenstraw with the head of South French Creek. This lowland also connects toward the north through Hare Creek Valley with the main French Creek just above the old divide crossed by that creek in the southwest corner of New York. From the point where this lowland connects with French Creek an old valley leads northward to North French Creek at Findley Lake, and from North French Creek a lowland heavily covered with drift extends northward past Grahamsyville to the plain bordering Lake Erie near Northeast, Pa. The filling of drift is so great in these lowlands that at present it is not possible to determine whether there was formerly a northward discharge from Corry through these old valleys into the basin of Lake Erie. The portion of French Creek Basin in eastern Erie County, Pa., is connected with old valleys leading northward from South French to North French Creek and thence to the headwaters of small tributaries of Lake Erie. The valley of the present creek shows a marked constriction just south of the Erie-Crawford county line, being reduced to about one-fourth the usual width of that portion of the valley. These features seem to favor northward discharge rather than a connection toward the southwest with 1Second Geol. Survey Pennsylvania, Rept. I*, pp. 234-235. 4 oe AM ene LOWER ALLEGHENY DRAINAGE SYSTEM. 145 the old Muddy Creek (Upper Oil Creek) drainage. But as yet no line has been traced out to the lake and it is not certain that the constriction on French Creek Valley near the Erie-Crawford county line marks an old divide. THE LOWER ALLEGHENY AND ITS TRIBUTARIES. In the discussion of the old Monongahela system (p. 88), attention was called to the broad gradation plain found on the Lower Allegheny, and com- parison was drawn between the breadth of that gradation plain and the much narrower rock shelves, abandoned ox-bows, and gradation plains found on the Middle Allegheny system. The Lower Allegheny and all its tributaries lie in large part, if not entirely, outside the glacial boundary. Consequently the several fluvial plains are better displayed than in the Middle and Upper Allegheny where much of the drainage area lies within the glacial boundary and where the old fluvial plains have been greatly concealed by glacial deposits. But even on the Lower Allegheny there have been quite heavy deposits of glacial gravel (60 to 100 feet in depth), made by streams that led down this valley from the ice field to the north, after the old divide which separated the Lower from the Middle Allegheny had been cut away. The main gradation plain, as determined by aneroid, has a height of 1,020 to 1,040 feet in the vicinity of the mouth of the Clarion River or 150 to 170 feet above the present stream. It falls to about 900 feet at the junction of the Allegheny and Monongahela at Pittsburg and stands at that point very nearly 200 feet above the river. The glacial gravel which caps the gradation plain has an upper limit at about 1,135 feet near the mouth of the Clarion and about 975 feet near Pittsburg. The original lower limit is not known, inasmuch as the amount of trenching prior to the gravel deposition has not been settled. ; In the western part of the city of Allegheny a feature was observed which supports the view that the streams had cut somewhat below the level of the old gradation plain before the gravel filling took place. Upon ascending to the old gradation plain along California avenue north of Woods Run the contact between the glacial gravel and the underlying shales is well exposed. The shales are found to be deeply weathered, so that for 14 to 23 feet from ' the surface only a brown residuary clay remains. The surtace of the shale here stands about 890 feet above tide and very nearly at the general level of the old gradation plain. The amount of weathering which it had undergone 144 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. prior to the gravel deposition seems to indicate that it stood above the old stream for a considerable period before the gravel deposition occurred. But it does not throw light upon the depth to which trenching had reached. Within the trench cut in the old gradation plain there are a few rock shelves which seem sufficiently near a definite horizon to be correlated. They stand about 75 to 100 feet above the river, and vary in width from one-fourth of a mile to narrow strips but a few feet wide. Whether they are merely an incident in the cutting down of the valley or signify the ter- mination of an epoch of degradation which was followed by a notable halt and possibly a refilling, has not been determined. There remain two other fluvial plains to be considered. One is the rock floor beneath the present stream and the other is the gravel filling which took place in connection with the Wisconsin glaciation. The rock floor is usually but 20 to 30 feet below the stream bed, though in a few places it appears to reach 50 feet. The excavation down to the rock floor seems to have preceded the Wisconsin stage of glaciation, for the rock floor is found to be as low under undisturbed portions of the Wisconsin gravel as in the trench which the river has cut in that gravel. The filling connected. with the Wisconsin glaciation extends to a height of 60 to 80 feet above the present stream, and about 100 feet above the rock floor. In the table below the relation and altitudes of the several fluvial plains are set forth. The altitudes are largely. barometric, but as a base for cal- culation the Allegheny Valley Railway has furnished a series of levels extending the whole length of the Lower Allegheny. The altitudes of the stream, the surface of the Wisconsin terrace, and the rock floor below the stream were estimated with a fair degree of accuracy from these railway levels, but for the gradation plain, high rock shelves, and the upper limit of gravel on the gradation plain, the barometer was called into use. In the vicinity of Pittsburg, however, Jillson has made a series of measurements of the gradation plain and upper limit of gravel with a Locke level. LOWER ALLEGHENY DRAINAGE SYSTEM. 145 Height above tide of fluvial plains along the Lower Allegheny River. Miles. Feet. Feet. Feet. Feet. | Feet. Feet. Mouth of Clarion | Rivers ese he os 0.0] 1,135 1 O20= 16040 )in | aeons 910 870 (?) Parker ...-..----- 2 1,115 AON eat OGON Renan 900 860 840-+ Monterey. ...----- 4A |. 1,125 OOOH Lo 2sctlec. 885 Rj) ee Hillville.......... Bay Pa O50) |aeeears 707} gt oye eae amen Hast Brady --.----- 6.1 1, 115 (C2) Saeemtaey PR oe et 860 | 825 815 Redbank -....---- 5.5! 1,100 COs iaeeeimnaeel 5 850! 815 810 Reimerton.------- 3.6 (?) (GOL = ARN |e ae 840 SO (chal eee Mahoning ...--..- 4.7| 1,050 960 850 825 Stal iae et ree Kittanning ....... 10.6 | 1,010 BOO ramdk9 80) eae seen 810 PLO ileal Grd ce nu se eeed 4 1, 025 885 and 980 |......-..- 805 G5 ah | Aer Aladdin _.....---- 10 @ | (?) Wisco fey 800 740 710 INatronavsssese eee 4 WE OOQEE eerste Ses fees ell eae cee ee | 800 (Ue woe eae aae Tarentum .......- 5 1, 000 975 825 800 725 700— mold tele ae ee 1 TRO Tiibaet eee eee corte nt ey 815 800 Pst hee aes HultonicacGencUeu Ff \. WAOS ik SUS RGR pm rs ee aan 800 20 (4 ene Sharpsburg ---.--- edt |esccetoccaloondpceaascadonece|sqesescces 800 (LO) Nearer Pittsburg .......-- 2 972 904 BOOS er oese soa dA oot epee Allegheny .......- 3 975 co le 18008 mnGOSt 4) Rae sae Belleyuesssssse es [ese 274 978 S9Ssa) Ry Meta JEMSE atp Aedes cea (Na alee | The interesting series of channels connecting the Lower Allegheny with an old oxbow of the Monongahela River at Pittsburg were mentioned in the discussion of the old Monongahela system, but it may be of interest to consider them in more detail. An old channel of the Monongahela leaves the present stream near Homestead and passes northward to Hast Liberty (now a part of Pittsburg). It there curves around to the southwest through Oakland and Schenley Park, coming to the Monongahela again about 3 miles below Homestead. This channel, like the gradation plain of the Monongahela, is nearly a mile in average breadth. Its rock floor stands 175 to 200 feet above the present stream, or about the same as the gradation plain. Its northernmost part is only 1 to 2 miles from the Allegheny Valley, but is separated from it by a chain of hills which in places rise 200 to 300 feet above the old channel. There are, however, three gaps in the chain of hills which were sufficiently low to permit the waters of the Allegheny to enter the old oxbow of the Monongahela and MON XLI—— 10) 146 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. bring into it a heavy deposit of glacial gravel. The easternmost gap is along Negley Run, immediately north of East Liberty, and has a width of nearly one-half mile. The middle gap is along Haights Run, less than a mile west of Negley Run. This gap is scarcely more than one-fourth mile in width. The third or westernmost gap sets in at Allegheny cemetery and extends westward to the base of Herron Hill, being nearly a mile in width. These gaps were filled by glacial gravel to a height of about 75 feet above the rock floor of the old oxbow of the Monongahela, their highest points being 970 to 975 feet above tide, as determined by Jillson with Locke level. The gravel extends but little into the old channel of the Monongahela, a feature which seems to indicate that the gravel-bearing water from the Allegheny there encountered a lagoon with but little eurrent. All the important tributaries of the Lower Allegheny enter from the east, the divide on the west being but 10 to 20 miles distant from the river. The largest eastern tributary, Conemaugh River, has a drainage area of about 1,800 square miles, or nearly one-sixth of the entire basin of the Allegheny and fully one-third of the Lower Allegheny Basin. The Clarion has a drainage area of about 1,200 square miles, Redbank River 550 square miles, and Mahoning Creek 400 square miles. These four streams drain nearly four-fifths of the area tributary to the Lower Allegheny. Rising, as these eastern tributaries do, on the border of the Allegheny Mountains, they have very rapid fall and are subject to great freshets in the spring, at which time the melting of snow and heavy rains often unite to swell their volume. The Johnstown flood, on the Conemaugh, is a con- spicuous instance of the disasters occasioned by such freshets. These streams are also subject to extremely low stages in the summer months. Porter estimates that the Conemaugh is at times reduced to less than 90 cubic feet per second, or scarcely two-fifths its proportion of the average low-water discharge of the Allegheny River (1,330 cubic feet per second).’ It is conspicuously lower than the low-water discharge of tributaries that drain drift-covered districts. Thus, French Creek, which has a drainage area of but 1,130 square miles, is estimated to have a low-water discharge of about 700 cubic feet per second.’ 1 Water power of fine Ohio River Basin, ete., by Dwight Porter: Tenth Census oi United States, 1880, Vol. XVI, Pt. I, pp. 442, 445. 2 Op. cit., p. 448. 5 fi LOWER ALLEGHENY DRAINAGE SYSTEM. 147 Evidence that additions have been made to the upper drainage basin of the Allegheny, is furnished by the features of the tributary valleys. It is found that the trenching of the gradation plains on the tributaries is conspicuous only in their lower courses. On the Redbank River, which enters 22 miles below the Clarion, accurate data are obtainable, since the railroad follows its valley for 70 miles and has a grade nearly coincident with the stream and but a few teet (20 to 40) above it. The profile of this railroad (see fig. 7) brings out the significant fact that the stream has a much more rapid fall in the lower 20 miles of its course than for some distance above that point, which is the reverse of the normal law of mature streams. The average fall for this 20 miles is nearly 12 feet New Bethlehem 7080! Climax | Brookville 1678" 397° , 1 , 1397 R ay, oes as ee Benezelt ' » y) ’ 970 1070 1 ' ' ' p : ' Le- nets == li Rock Shelves _: a Level of Lake Erie 0 10 20 30 miles eS Fic. 7.—Profile along a portion of the Low-Grade Division of the Allegheny Valley Railway (so named because of the low altitude at which it crosses the Allegheny Mountains). It shows the increase in the rate of fall of Redbank River in its lower 20 miles, a feature due to the deeper trenching of that portion. The profile also shows the extreme narrowness of the col which separates the Redbank and Susquehanna systems, the tunnel beneath the col being but 1,950 feet in length. per mile, while for the next 20, or even 50, miles above, the average fall is less than two-thirds of this. In the upper portion the present floor of the stream nearly corresponds with an old floor. In the lower portion, this old floor continues on to the mouth with a rate of descent a little less than that of the upper portion, following the normal law. The later stream \ ~ here, however, enters the Allegheny about 150 feet below the old floor; but this lessens rapidly upstream, and at 20 miles above the mouth it is reduced to about 60 feet.’ It appears quite evident from these facts that there has been an abnormal deepening of the Allegheny since the formation of the old floor, and that this has been so recent that it has, as yet, made itself seriously felt 1Compare statement of I. C. White respecting the relative altitude of water deposits on the upper and lower courses of the Conemaugh, Youghiogheny, and Cheat rivers: Am. Jour. Sci., 3d series, Vol. XXXIV, 1887, p. 378. 148 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. upon the gradient of the Redbank only in its lower 20 miles. Such an abnormal deepening is accounted for by the sudden enlargement of the drainage area to several times its former size in consequence of the diver- sions of drainage previously discussed. It is improbable that a simple change in the altitude, or in the general slope of the region, would produce a result of precisely this nature. The main stream, of course, usually leads in rejuvenated excavation, but not in such a disproportionate degree as this nor in precisely this method. In the Clarion Valley the present stream has a fall of about 500 feet in the lower 75 miles below Ridgway and the old fluvial plain about 340 feet Redbank River falls about 400 feet in the lower 40 miles below Brookyille, but the old fluvial plain falls only about 280 feet. In the 62 miles from Falls Creek station to the mouth of Redbank River, the stream has a fall of 550 feet and the old fluvial plain a fall of 430 feet. The Conemaugh falls about 425 feet, and the old fluvial plain about 300 feet in the 64 miles below Johnstown. Of these old fluvial plaims the one on the Clarion shows the lowest fall, about 4.5 feet per mile. If these data are compared with those given in the table on the fluvial plains of the Lower Allegheny, it will be found that both in its present and in its old stream beds the Lower Allegheny has a much lower gradient than its main tributaries. BEAVER RIVER. Beaver River is formed by the junction of the Shenango and Mahoning rivers, and has a drainage area of about 3,000 square miles, of which, per- haps, 1,800 square miles are in Pennsylvania and the remainder in Ohio. Attention has already been called to the evidence that the Beaver consti- tuted the former line of discharge for the Upper Ohio and its main — tributaries as far to the northeast as the Clarion River. The restoration of the old systém of drainage given on fig. 1 (p. 89) serves to show its natural- ness compared with the present system. The Conoquenessing, an eastern tributary, has a northwestward trend to its junction with the Beaver, and formerly continued in this direction toward the Lake Erie Basin, but now it turns abruptly southward to enter the Ohio. The former outlet of Slip- pery Rock Creek was in a course north of west through the valley now drained by Big Run entering the Shenango at Newcastle. This finds a natural continuation northwestward along the old line to Sharon, Pa. The upper course of Mahoning iver is northward from its source in Columbiana BEAVER RIVER DRAINAGE SYSTEM. 149 County to the head of Grand River Basin near Warren, Ohio, through which it formerly evidently discharged. It now makes an abrupt turn to the southeast along a small valley which apparently headed near the Ohio- Pennsylvania line. Smaller tributaries illustrate still further the unnatural courses of the present lines of discharge. In connection with this drainage system, it is necessary to consider several distinct fluvial plains. The gradation plains and rock shelves which slope toward Lake Erie from the mouth of the Beaver are the earliest of the series. The gravel filling which built up the lower part of the Beaver and the Upper Ohio sufficiently high to give a discharge down the present Ohio comes next in the series. A rock floor cut to a lower level than the beds of the present streams apparently forms the next well-defined fluvial plain. A gravel filling which occurred during the Wisconsin stage of glaciation - evidently succeeded the deep excavation of the valleys, and comes later in the series. This gravel filling is now in process of excavation by streams whose beds form the last of the series of fluvial plains. Attention will be here directed only to the main gradation plain, to the rock floor buried beneath the present streams, and to the gradients of the stream beds ~The gravel fillings are considered in connection with their respective drift sheets. The gradation plain has been greatly disguised by a drift coating, except in the lower course of the Beaver. It apparently descends north- ward along the Beaver and the Shenango, as outlined on a preceding page, about to Sharon, Pa., but it does not appear to continue its descent along the Shenango north of that city. At Greenville, 25 miles above Sharon, a series of wells test the valley quite widely and strike a rock floor, appar- ently the old gradation plain, at a level about 35 feet higher than the level of the old plain at Sharon. This condition fits in naturally with the inter- pretation that the old drainage passed westward from Sharon imto the Grand River Basin. At Youngstown, Ohio, which is on the line apparently followed by the old stream, the gradation plain appears to be lower than at Sharon, though the valley has not been explored sufficiently to make certain the precise altitude of the gradation plain. At Niles, also on the old line, the rock floor in one boring was found to be 65 feet lower than at any ascertained borings in the vicinity of Youngstown. Borings in the Grand River Basin near Southington, Mesopotamia, and Rome, Ohio, have 150 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. in several instances reached a level only 70 to 80 feet above Lake Erie without striking the rock floor, but one bormg near Mesopotamia is thought to have reached rock at a level 70 feet above Lake Erie. As the gradation plain at the mouth of the Beaver stands nearly 300 feet above Lake Erie and is distant but 90 to 100 miles from some of these borings in Grand River Basin, it is evident that the northward slope is rapid. In the 30 miles from the mouth to the head of the present Beaver there appears to be a descent of fuliy 50 feet, and in the 50 miles to Sharon of about 85 feet, thus giving an average slope of about 20 inches per mile. This slope has possibly been made greater by Pleistocene changes in level, though specific evidence is not at hand. The old gradation plain and the rock floor of the valley excavated in it are widely separated in altitude near the mouth of the Beaver, but apparently approach each other rapidly in passing northward. ‘The evidence seems clear that the reversal of drainage took place before much of the deep channeling occurred. so In general the slope of the rock floor beneath the present streams is m harmony with the present drainage, and in the main is the reverse of the ancient system. There is, however, a part of the channel in which the rock floor appears to be excavated to a level too low to correspond with the floor at points lower down the stream. Such features were at first interpreted to signify that the drainage was in the reverse direction from the present line of discharge, but further examination has rendered it prob- able that the excavation has been accomplished by a stream running in the present line of discharge. On the lower course of the Mahoning the oil- well records show the rock floor to be fully as low as at the mouth of the Beaver and apparently about 90 feet lower than at the mouth of the Con- oquenessing, midway of the Beaver Valley and 15 miles below the mouth of the Mahoning. The piers of the railway bridge at the mouth of the Conoquenessing are reported by R.-R. Hice, of Beaver, to stand upon the rock floor, and are so distributed as to test the middle as well as the border of the valley. Upon passing up the Mahoning, a few miles from the deeply excavated part, the rock floor is found to have an altitude nearly 150 feet higher. There is‘ an abrupt descent just above Edenburg. Here the buried floor seems to fall 165 feet in half a mile, as shown by four wells reported by W. H. Raub, of Edenburg. ‘The declivity may be even BEAVER RIVER DRAINAGE SYSTEM. 151 more precipitous, as the wells are not situated so as to limit more closely the space occupied in the descent. The variations in the valley floor appear to be such as might result from the recession of a fall or cascade, and this suggestion harmonizes with the more clearly indicated history of the region, which appears to be as follows: Before the ice invasion forced the waters of the upper portion of the Grand River Basin across the divide, which apparently stood near the State line above Edenburg, there was only a small tributary leading down to the valley occupied by the old north-flowing Monongahela system. But when the waters of the upper Grand River Basin were forced over the divide in large volume and descended the steep slope of the little valley, deep scouring at the mouth would naturally result and the formation of cascades or falls would readily follow. These would work upstream as the erosion progressed. They appear to have reached a point just above Edenburg when a later incursion of the ice stopped the process and filled the deep valley with débris. The formation of a pool was favored by the softness of the rock in this portion of the valley and the hardness of the strata encountered near the mouth of the Conoquenessing. The present system of drainage displays considerable variation in the slope of its stream beds, some portions being very sluggish, while other por- tions present rapids and even low cascades. The Shenango falls but 2 to 2% feet per mile in the upper 22 miles above Jamestown, Pa., the source of the river being in a swampy lowland at an altitude only 1,025 feet above tide. In the next 30 miles, from Jamestown to Sharon, there is a fall of 4 to 5 feet per mile. From Sharon to the mouth of the Shenango, a dis- tance of 24 miles, the average fall is 24 feet per mile. The Mahoning has a fall of about 3 feet per mile in the 35 miles from Warren, Ohio, to its mouth, but the northward-flowing headwater portion is more rapid. In the 23 miles from its head to Beaver Falls the descent of the Beaver is only about 2 feet per mile, but in the lower 5 miles it makes a descent of 52 feet, or more than 10 feet per mile. ye, GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The principal data concerning the several fluvial plains which form the basis of the above discussion are grouped in the following table: Height above tide of fluvial plains along the Beaver and Shenango rivers. Location, Distance) (OPCs a pacer eeecad Miles. Feet. Feet. | Feet. \ IMoybIEN ONE IBieenieIr LRINGIe = 55 soc caseeneoeedoosaceasescan 0 865 to 880 605=- 664 Bean erpialll sameeren eee eae ee see einieie sis scien cise 5 850 |S OBE 716 Mouth of Conoquenessing River ------------------------ 9 840 | 682 734 HeadvonBeaverRivietioe = =ss5--sseeesee e=seeeee ase sees 14 810== 620 764° INGWIGRSUIG Soo cebu dosneosusse seed enbaeassebcenepRoucan Da ers SBS ISne Sas 645, 780 laleyd joye IBA os aan ocseseecooousessebeucseceoesds at 800 ? ~ 800 Sharon ....- Snes ee EE ON epee ee Aner 17 | 780 ? 840 lark. 355 cssc seb ossao ose sgas oT as HRSeneas ase soces b) 2 760— 860 Greenville etter wees Se ar la sae ee Ae cla Se aver 20 815 ? 940 JamMestowlaeeeee sere cerer crescent eee erase cece s 5 i ? 965 Outlet of Pymatuning Swamp-..----------------------- 13 ? 2 1, 000 Flerdtotebyanat unin oS wal serra ee eer weenie 9 ? ? 1, 025 LITTLE BEAVER RIVER. The Little Beaver, a small north tributary, flows into the Ohio near the Ohio-Pennsylvania line. Its drainage area lies mainly in Ohio, though the North Fork has much of its watershed in Pennsylvania. The northern half of the area drained by the Little Beaver has been glaciated, and its pre- glacial features are greatly obscured by heavy deposits of drift. Its general elevation is scarcely so great as the unglaciated southern half. This and other features suggest that much of this drainage basin once had a north- ward discharge to the old Beaver system. The lower course of the present stream is very narrow, and in preglacial times may have carried but a small fraction of the present drainage. The probable course or courses of northward drainage and the extent of change in drainage have not been determined. White reports that the North Fork has a sluggish flow through a region heavily covered with drift from its source nearly to its junction with the main creek at Fredericktown, Ohio, but that below that junction the stream falls at the rate of 25 feet per mile.’ MUSKINGUM DRAINAGE SYSTEM. 153 MUSKINGUM RIVER, The Muskingum River drains the greater part of eastern Ohio and has an area of about 7,740 square miles. The name Muskingum is applied only to the lower portion below the junction of the Tuscarawas and Walhonding rivers, a length of 109 miles. From the sources of the Wal- honding and Tuscarawas to their junction is a distance of about 100 miles, thus giving the basin a length of 200 miles. It is a broadly branching drainage system. at the north, with an extreme width of about 100 miles. At the south it receives few tributaries, there bemg none of importance below Zanesville. The following estimates of the areas of the drainage basin are taken from Porter’s census report: ’ Drainage areas of Muskingum River and its tributaries. Square miles. AWiallln orci SARGIVG Reece wtetetretey = erate lesie selects ae athe eee ai ota ae atta ae ee Seer eis ers 2, 159 MuscarawashRiveren-se= ees ned seca anesisecicsgee oe videe PR ches ar See ee ee ee Bee tee 2, 547 VAVAMUIS) CORSE Fe oe Ses ern A aS ee edt Ne ae She LSP Faas ae etapa Ae eee eStores 815 JUNTA IRIN Gres ee en io ee BO on ae Se ene hea a edt ans. os cere Spar Sho emu yeE 703 Muskingum and tributaries below Zanesville...........-...-..----------- Pel sae art 1,175 Motalvarcanofe Mus kin sums SteLae Mem hae sae oa eee a ee Sai an eret neers Sree peer ie Eee eee 7, 740 This drainage basin is mainly in the unglaciated portion of south- eastern Ohio, and the greater part of it is in soft Coal Measures strata, which have become greatly broken down under atmospheric and stream action. On the northwest border of this watershed the hard sandstones and conglomerates which underlie the Coal Measures come to the surface. These, in some cases, are preserved as outlying knobs and ridges, standing 200 to 300 feet or more above the lowlands that surround them. The most elevated parts of the watershed are found in, these outlying knobs, some of which are nearly 1,500 feet above tide. The eastern border of the watershed is also high, its altitude reaching about 1,400 feet. In the central portion of the watershed the uplands are but 900 to 1,000 feet and the valleys 700 to 800 feet above tide. Many of the valleys are broad and characterized by gently sloping bluffs. The old gradation plains in much of the area stand below the level of the present streams. The large amount of gravel filling in valleys that lead away from the glaciated area has built up the stream beds to such an 154 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. extent that the tributaries leading in from unglaciated portions of the basin have become silted up to a marked degree. In these respects a striking contrast is found between this drainage system and that of the Upper Ohio, which lies immediately east of it. Notwithstanding the low altitude of the gradation plains and conse- quent absence of trenches, the present system of drainage departs greatly from the ancient system. Not only have changes occurred in the glaciated district, but also outside, notably in the line of discharge for the main river. The filling of the valleys was sufficient to raise the streams above the level of the low cols that separated the ancient drainage lines without the neces- sity of much excavation at the cols. The present drainage lines are almost entirely in old valleys, for the divides crossed by them constitute but a small portion of the length of the streams. The position of the old divides is usually shown by a constriction in the valleys combined with a higher altitude of the rock floor. The changes are numerous in the headwater portions that lie within the glacial boundary, but only a few have been sufficiently examined to justify an interpretation. In some cases where constrictions occur in the valleys there have been no borings sufficiently deep to throw light upon the altitude of the rock floor, thus leaving an element of uncertainty concerning the significance of the constriction. The changes of drainage in the central and western portions of this watershed, and also along the lower course of the valley, have been investigated by W. G. Tight in some detail, but his latest results have not yet been pub- lished. The writer has given the region only a hasty reconnaissance. The changes in the northern portion have also been investigated by J. H. Todd, of Wooster, Ohio.’ In the eastern part of the watershed no changes of importance appear to have taken place. M. C. Read,’ of the Ohio survey, has outlined on a map, and to some extent discussed, the position of many pregilacial lines, some of which are not followed by the present streams, but he did not attempt such a full interpretation of the connections of the old lines of drainage as has been made by Tight and other later students. 1Qhio Acad. Sci., Special Papers No. 3, 1900, pp. 46-67. *Geology of Huron, Richland, Knox, and Licking counties, Ohio, by M. C. Read: Geology of Ohio, Vol. III, 1878, pp. 289-361. Also Geology of Ashland, Wayne, and Holmes counties, Ohio, by the same author: Ibid., pp. 519-561. MUSKINGUM DRAINAGE SYSTEM. 155 THE OLD WESTWARD OUTLET. Tight has shown that the greater part of the Muskingum drainage system was formerly connected with the Scioto system by a broad valley leading from Dresden (a few miles above Zanesville) westward past Newark to the Licking reservoir and thence into the Scioto Basin near Circleville? The present southward course past Zanesville is through a much narrower valley than the old line leading westward to the Scioto Basin, and the rock floor is markedly higher along the present course of the Muskingum than along the old course. Along the old line of discharge there is, for about 10 miles, an open ~ valley, 1 to 14 miles in width, leading westward from Dresden past Frazers- burg. This open valley is now drained by a small stream, Wahatomaka Creek, which enters it from the north near Frazersbure. The old outlet of the Muskingum continues broad and open as far west as the eastern border of Licking County, where it becomes obstructed by a great accumulation of drift, which fills the valley to a height of 150 feet or more above the level of the broad bottom on the east. This drift filling obstructs the valley in this manner for only a couple of miles, and even there but half fills it, for the bluffs rise about 300 feet above the broad bottom just men- tioned. At Hanover an open valley sets in, which extends westward to Newark and thence southwestward along the South Fork of Licking River to the vicinity of the Licking reservoir, where it is so filled with drift as to render its further course difficult to determine. A series of gas borings, however, indicate that it passes southward about to Hadley Junction and there turns westward, passing near Canal Winchester and Groveport and coming to the Scioto River about midway between Columbus and Circle- ville, where it seems to have joined the old Kanawha system. “The course or choice of courses for the old Kanawha from this point has already been discussed (p. 103). It should be stated, however, that Tight inclines to favor the northwestward course across the rim of the Scioto Basin into the old Wabash system rather than the northward course along the axis of the Scioto Basin to the Lake Erie Basin. The old line of discharge from the Muskingum into the Scioto Basin was excavated to a level much below the broad bottoms above described. 1 Bull. Denison Univ., Vol. VIII, Pt. II, 1894, pp. 35-61. 156 GLACIAL FORMATIONS OF ERIE AND OHIO: BASINS. A well about 1 mile east of Hanover is reported by Tight to have reached a depth of 218 feet without striking the old rock floor of the valley, though the bottom of the well is about 150 feet below the present level of the Muskingum at Dresden, or but 550 feet above tide. It is 50 feet or more below the level of the rock floor of the present Muskingum at points 30 to 40 miles below Dresden. At Newark the old valley was cut to a level about 250 feet below the present river, or to less than 550 feet above tide. Gas wells at Hadley Junction and other points along the old line between Hadley and the ‘Scioto River also reach a similarly low level before encountering rock. THE PRESENT LINE OF DISCHARGE. . Turning now to the present course of the Muskingum below Dresden, we find a much narrower valley than the old channel of discharge, the width ranging between one-half and three-fourths of a mile in the first 25 miles below Dresden. It there grows narrower, and in the vicinity of the line of Muskingum and Morgan counties, 33 miles below Dresden, it is less than one-fourth of a mile in width and is bordered by abrupt bluffs 200 to 250 feet in height. This is the narrowest place on the lower course of the river and is apparently the site of an old divide. The valley, however, remains narrow nearly to the mouth of the stream, its measured breadth at Lowell, 12 miles above the mouth, being barely one-half mile. No data concerning the elevation of the rock floor in the portion of the valley between Dresden and the supposed old divide have been obtained; but at Eaglesport, about 3 miles below the supposed divide, a gas well on the east side of the river about midway between the bluffs entered rock 30 to 35 feet below low water, or about 615 feet above tide. Another boring at McConnelsville, 7 miles farther down the valley, is reported to have entered rock 50 feet below low water at that point, or 590 feet above tide.! The rock floor here seems to be about as low as at Lowell, 35 miles farther — down the valley, the dam at Lowell being built upon the rock floor in the middle -part of the valley which there stands at 580 to 590 feet above tide. Concerning the height of the supposed divide above Eaglesport, there is good evidence from the contours of the bluff that it did not exceed 900 feet above tide, for the bluffs rise abruptly in this constricted portion to a 1Data concerning the borings at McConnelsville and Eaglesport were obtained from Dr. H. L. True, of McConnelsville. MUSKINGUM DRAINAGE SYSTEM. lor height of only 875 to 900 feet. Possibly the old divide was even lower. In districts both to the east and west of the supposed divide on the Muskin- gum, cols are found at an altitude not far from 900 feet above tide, and this also favors the view that the col crossed by the Muskingum stood equally low. DEPOSITS ON THE LOWER COURSE OF THE MUSKINGUM. In the portion of the Muskingum Valley between Dresden and the supposed divide, glacial deposits, probably of Wisconsin age, have been built up to a level 750 to 800 feet or more above tide, or about 100 feet above the present stream. They appear to be as high in Zanesville, at the mouth of the Licking River, as in the portion of the valley above, between Zanesville and Dresden. Below Zanesville the altitude apparently declines about as rapidly as the descent of the present stream, being by Locke level from the Government bench marks 85 feet above the river near Taylorsville, 90 feet at Eaglesport, 110 feet near the mouth of Meigs Creek, 119 feet at Beverly, and 105 feet at the mouth of the Muskingum. In the 75 miles from Zanesville to the mouth of the Muskingum the present stream descends from 683 to 570 feet above tide, while the gravel surface descends from 800 to 675 feet above tide. Before this gravel was carried down the valley there apparently had been an excavation at the supposed divide to a level 30 to 35 feet below the present stream or to less than 625 feet above tide. Deposits of waterworn material have been found in the lower part of the Muskingum Valley at higher elevations than the glacial gravels. In the south part of McConnelsville a rock shelf standing about 775 feet above tide, or 135 feet above the river carries a deposit of gravel several feet in depth. No rocks of glacial derivation were observed in this gravel, while in the gravel which appears at a lower elevation such rocks are abundant. Dr. True, of McConnelsville, reports that at a pomt about 1 mile above Stockport pebbles occur up to a level about 180 feet above the river, or 810 feet above tide. These include pieces of the Cambridge limestone, whose outcrop is up the river from this point, showing clearly that the deposit was made by a southward-flowing stream. Near this point a col was found at an altitude of about 830 feet above tide, which appeared to True to show evidence of excavation by a stream. At Luke Chute, True found pebbles on the slope of the valley up to a height of 160 feet above the river, or 780 158 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. feet above tide. In that vicinity he also found a few small quartz pebbles in a surface loam capping the upland at about 840 feet above tide. In this connection it may be remarked that small stones apparently derived from the drift, including greenstone, granite, and quartzite, are scattered over the uplands in the vicinity of McConnelsville at various altitudes up to 1,000 feet above tide. True has collected about a half bushel of these erratics. As the glacial boundary seems to lie seyeral miles northwest of McConnelsville, it may be necessary to refer the dis- tribution of these erratics to human agency. The Indians were perhaps responsible for their wide distribution outside the glacial boundary. The small pebbles found in the surface loam, which are usually a half inch or less in diameter, and are found at a depth of 1 to 4 feet from the surface seem more likely than these larger pebbles to have been deposited by natural agencies. The surface loam is apparently a water deposit, possibly a phase of the loess, as indicated on a subsequent page. The loam and its included pebbles point strongly to an interval of submergence which antedated the Wisconsin gravel filling in the valley of the Muskingum, but which may be more recent than the change of drainage just discussed. The subject is one requiring further investigation. STRIATED BLOCKS IN MUSKINGUM VALLEY NEAR M’CONNELSVILLE. True called the writer’s attention to striated sandstone blocks found on the slope of the east bluff of the Muskingum about 2 miles above McCon- nelsville, at an altitude 780 to 800 feet above tide. They apparently were derived from the ledges in the immediate vicinity. The striation consists of a series of shallow grooves, which vary a few degrees in trend and seem less regular than glacial striz. The writer has observed a grooving more marked and regular than is here exhibited on a rock reef in the bed of the Ohio River near Ravenswood, W. Va. As that locality is far outside the glacial boundary, the grooving is apparently due to river ice. It seems not improbable, therefore, that the grooving displayed by these blocks is referable to the transportation of stones by river ice when the stream was flowing at an altitude as high as these ledges. EXTENT OF THE OLD MUSKINGUM DRAINAGE BASIN. The old Muskingum drainage basin extended up the ‘Tuscarawas nearly to the mouth of One Leg Creek, a distance of 75 miles above the MUSKINGUM DRAINAGE SYSTEM ae old westward outlet. The eastern tributaries of the Tuscarawas and Mus- kingum between the mouth of One Lege Creek and the south line of Muskingum County probably had as great an extent then as at present; but the northern and western tributaries of the Tuscarawas and Muskingum all appear to have been quite small. The Walhonding, which now has a drainage area of more than 2,000 square miles, appears to have formerly drained scarcely 500 square miles, its basin being mainly in Coshocton County. It received only the 8 miles of the lower course of Owl Creek below Millwood and the lower 8 or 10 miles of Mohican Creek. How much of Killbuck Creek was tributary to the Walhonding has not been determined, though it appears probable that the old divide was below the village of Killbuck, or less than 20 miles from the mouth of the stream. Sugar Creek, which enters the Tuscarawas at Canal Dover, is almost entirely a new accession, the old divide being apparently south of Strasburg, only 6 or 7 miles from its mouth. From these observations it appears that the entire drainage area discharging westward past Dresden can scarcely have exceeded 3,000 square miles, which is but little more than half the area that now discharges southward past that point. It has not been decided whether the old drainage of the portion of the Muskingum south of the westward outlet led northward from Zanesville along the present stream (reversed) to the old outlet at Dresden or took a northwestward course from Zanesville, along a line followed in part by the Licking (Gn reverse direction), to enter the old outlet near Nashport. Along either line there is only a narrow valley scarcely one-half a mile in average width. Drift accumulations in the northwestward line so conceal its channel that some uncertainty is felt as to its continuity; but it is the more direct line and appears to be fully as capacious as the northward line. In its favor there is also a peculiarity of drainage at Zanesville. An old valley leaves the present Muskingum just below Zanesville and bears northwestward through the western part of the city, beng separated from the present river by a prominent ridge known as Putnam Hill. It there connects with the old channel leading up the Licking. It also connects eastward with the Muskingum, but this may be simply the old line of west- ward discharge for a small drainage basin north and east of Zanesville. In case there was an old divide on the present line of the Muskingum between Dresden and Zanesville it is more likely to have been near Ellis 160 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. than at points above or below, for the valley is exceptionally narrow there. The bordering uplands also reach a higher elevation there than in other parts of this section of the Muskingum. DRAINAGE TRIBUTARY TO THE WESTWARD OUTLET. The portion of the westward outlet between Dresden and Newark apparently received the drainage from about the same territory as is how tributary to Wahatomaka Creek and the lower course of Licking River. The headwater portions of the North Fork and the Middle or Raccoon Fork of Licking River appear to have discharged directly westward into the Scioto Basin, as determined by Tight, there being an old divide crossed by the Raccoon Fork near Granville, and by the North Fork south of Utica.’ The South Fork of Licking once received a larger drainage from the east than it does at present. Jonathan Creek, which now leads eastward into the Muskingum from near the Licking reservoir, crosses an old divide at the narrows in its lower course near Fultonham, as determined by Tight and Davis” The greater part of the old drainage was in the reverse direction from the present stream, and entered the old outlet near the Licking reservoir. Farther south the old outlet received the headwater portion of Hocking River from as far down as Rockbridge, in northern Hocking County, including the entire drainage basin of Rush Creek. It also received the drainage of the district now tributary to Little Walnut Creek, a portion of the outlet now being followed by the creek. CHANGES IN OWL CREEK DRAINAGE BASIN. Owl Creek, which drains the greater part of Knox County and adjacent parts of Morrow and Richland counties, unites with Mohican Creek in west- ern Coshocton County to form the Walhonding River. It is the first drainage line of importance that leads into the Muskingum from the west above the old outlet. The changes of drainage which it has experienced were partially worked out and discussed by Read prior to 1878.’ The writer examined the drainage basin in 1890, and subsequently it was examined by Tight and his assistants. It has been noted by each of the. persons who have examined this drainage basin that the stream crosses an 1 Communicated to the writer. 2 Modification in the Jonathan Creek drainage basin, by H. J. Davis: Bull. Denison Uniy., Voi. XI, 1899, pp. 165-173. 8 Geology of Ohio, Vol. III, 1878, pp. 325-326. OWL CREEK DRAINAGE BASIN. 161 old divide between Mount Vernon and Gambier, cutting off a spur that projected from the north, and separating a valley that leads southward from Mount Vernon from one that leads southwestward from Gambier. It was also noted by each that another old divide is crossed a few miles below Gambier, near Millwood. Concerning these changes Read remarks:! For a part of the distance between Mount Vernon and Gambier the stream has made for itself an independent channel through rock spurs projecting from the north, but the course of the old river can be traced a little to the south of it. At Gambier it is in the ancient bed of a channel extending southward toward Martinsburg, now filled with gravel and sand hills, and occupied by Big Run, which flows northward in a direction opposite to that of the old stream, and becomes a tributary of Owl Creek. At Millwood also the channel of Owl Creek is narrow, rock bound, and recent, but the old channel is easily traced to the south of the massive bluffs of the Waverly conglomerate, where it is now filled with modified drift bills of gravel and sand. The old channel referred to by Read leads past Danville to Mohican Creek at Gann, and is utilized by the Cleveland, Akron and Columbus Railroad. It is evident from the remarks just quoted that he thought the : old course of drainage from Gambier was southwestward, but it is not so clear that he thought the old channel that connects Mohican Creek and Owl Creek also had a southwestward discharge. To the writer and also to Tight it seems necessary to give the old channel a southwestward discharge, for it appears to be continuous with the channel to the southwest that discharged in that direction. Read thought that there was a line of southward drainage from Mount Vernon to Newark through a lowland tract followed by the Baltimore and Ohio Railroad, but he appears to have overlooked evidences of an old divide on this line south of Utica. Upon examining this lowland in 1890 the writer found low rock hills in its midst about 3 miles south of Utica, which seem to bar out completely a southward course for the old drainage. At that time no clue to the old course of drainage could be found, but subsequently it was ascertained by Tight, through data furnished by wells, that the dis- charge may have been westward from near Utica past Homer to the Scioto Basin. The drift filling is so great along this westward line as to completely conceal its course. At Homer the drift has a depth of 400 feet. It now seems probable that the greater part of the Owl Creek drainage basin above Mount Vernon formerly had a southward discharge to the bend 1 Some typographical errors in Read’s description are here corrected. MON xLI——11 162 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. of the North Fork of Licking River east of Homer, where it was joined by a drainage line leading in from the northeast past Danville and Gambier. The united waters then passed westward into the Scioto Basin. It is not yet known how much of the basin of Mohican Creek was tributary to this line, but judging from the small size of the old valley at Danville it was probably only a small part. Possibly it included only the section between the high ridge at the north line of Knox County aad a narrow part of the Mohican Valley a short distance below the point: where the old valley turns — off toward Danville, a section about 12 miles in length. This leaves a stream about 8 miles in length on the lower course of Owl Creek and a similar stream on the lower course of Mohican Creek to form the old headwaters of the Walhonding River. CHANGES IN CLEAR FORK OF MOHICAN CREEK. Clear Fork drains a small district immediately north of the drainage basin of Owl Creek. Its headwaters are in eastern Morrow and southwestern Richland counties in a moraine that forms the east border of the Scioto Basin. The moraine has in that vicinity an altitude of 1,300 feet or more. From the moraine the several headwater streams flow east and southeast and unite a short distance west of Bellville. The stream then passes into a more elevated hilly region whose highest points are nearly 1,500 feet above tide. The valley at the west border of these hills is more than one-half mile in width, but upon passing eastward down the present stream it narrows and finally becomes a contracted gorge just above Newville, where the rock bluffs are scarcely 100 yards apart. This evidently marks the position of an old divide. Below this divide the old drainage was eastward, as at present, but it apparently was a short distance north of the present stream, along a line now followed in part by Black Fork. The present course is across points on the slope south of the old valley. This departure from the old line is due to a moraine that follows the north side of the present stream from Perryville eastward and prevents the stream from following the old line. CHANGES IN OTHER HEADWATERS OF MOHICAN CREEK. There are several other headwater tributaries of Mohican Creek in Richland and Ashland counties which, like Clear Fork, have their sources outside of the highest country included in their basins. The most impor- MOHICAN CREEK AND ITS TRIBUTARIES. 163 tant are Muddy Fork, Black Fork, Jerome Fork, and Lake Fork. The sources of each of these tributaries is in a morainic system that here consti- tutes the continental divide. It is evident that this morainic system is north of the old divide, for it stands on a slope facing toward Lake Erie. Its altitude is 200 to 300 feet lower than the hills a few miles to the southeast. Furthermore, it is traversed by buried valleys, 250 feet or more in depth, which lead northward from the high upland just referred to toward the Lake Erie Basin. ‘These valleys are now nearly concealed, but well borings have shown their great depth. The old divide on each of these headwater streams of Mohican Creek was probably but a few miles south of the present divide, as the lower courses of the streams, as indicated below, appear to connect with a valley that leads eastward toward the old Cuyahoga Valley; but as yet the old divides have not been located with precision. At the present time the streams flow over passes or cols which were once much lower than the hills of that region. Probably some of these cols stood below the general level of the drift fillmg. In such cases they may per- haps be located by well borings or by careful examination of the valley contours; though, unfortunately, the drift in these old valleys is aggregated in knolls and ridges that greatly obscure the preglacial topography. On one of these tributaries, Muddy Fork, the valley filling was such that the stream made a detour of several miles near Lucas through a hilly district north of the old valley. This serves to show that there were low passes by which the drainage systems could easily be reversed or otherwise changed. J. H. Todd, has recently called attention to evidence that the lower courses of these tributaries of Mohican Creek had an eastward dis- charge.’ There is a continuous valley or lowland with an average width of about a mile, followed by the Pittsburg, Fort Wayne and Chicago Railroad from Mansfield to Wooster, Ohio. It follows down Muddy and Black Forks (except for the detour of Muddy Fork above noted) to Loudonville, thence eastward across the divide between Black and Lake forks and across the divide east of Lake Fork into Killbuck Valley near Shreve, up which it passes to Wooster. Hast of Wooster there is a great drift accumulation rising nearly 200 feet above Killbuck Valley, but it is Todd’s opinion that the old valley continued in that direction about 10 miles, to the vicinity of Orrville, where a valley is found with very low 1Ohio Acad. Sci., Special Papers, No. 3, 1900, pp. 49-55. 164 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. rock floor. This valley seems to have drained northward either to Rocky River or the Cuyahoga, passing near Sterling. The writer is inclined to favor the view that this valley had a course eastward from Sterling to Warrick, and thence north past New Portage and Copley Marsh into the old Cuyahoga, that being a larger valley than the old Rocky River Valley. Todd, however, favors Rocky River Valley as the line of discharge into Lake Erie. The valley under discussion, with its deep filling of drift, shows gen- eral eastward descent, as indicated in the table below. The available data concerning the rock floor shown in the table, though meager, also favor the view that it slants eastward. It furnishes a more natural trunk line than any other old line of drainage yet found in that region. The several tribu- taries of Mohican Creek converge toward this old valley, and seem to find in it a natural line of discharge. This old line may properly be termed the old Mohican. The table presents the railway stations in order from west to east between Mansfield and Wooster, showing elevations of the present surface and rock floor so far as known. The borings at Millbrook and Wooster fail to reach rock at the altitudes given. Altitudes above tide along the old Mohican drainage. Station. from Abia: Ereent SUT! Rock floor. field. antl Miles. Feet. Feet. _ Winmgit@N6l = =< sacs eeec ass oSsae2QeS se pea osesesoSeEaaSsasecsose 0 1,151 900 THNGAS coc ce soecoce SesesbooseousSaseeescess Sane soucoSScoSoouSssS ia 1, 090 (?) Perrysville ...---.--.------------------------------------------: 14 992 (?) Loudonville ....-------- Se ESBS ann nos See e a Sea cose poacadasdososs 18 974 825 Leal. ccscaceoce oossonadecontosnscSsspsuessosesasaconsedess 24 939 (?) MARE oc ccboosseodcosduounseanes Bosch Seen Eoetorsencsassascedas 30 911 (?) MiNMoROO soos cos coesososseSeous posse ssesoesess Sic acer Sess 32 900 715— WY GORI? dobas5 4d cose cco basedgesecosooeenbeussacouuamesecchonsad 40 901 790— Black Fork now turns south from this old valley at Loudonville, and passes through a range of hills to jo Lake Fork. Lake Fork passes across the old valley at Lakeville, and discharges through a much nar- rower valley toward the south. It seems probable that an old divide which separated this drainage system from the east fork of the old Owl Creek drainage was crossed just below the junction of this old valley and Black Fork. For a few miles north of Lakeville Lake Fork is in a broad valley, OLD UPPER TUSCARAWAS DRAINAGE SYSTEM. 165 but farther up the valley, near the mouth of Jerome Fork, it passes through a narrow channel among the hills. The old valley lies west of this narrow channel. Whether it connects at the north with Jerome Fork has not been ascertained. KILLBUCK CREEK. This creek now drains the western part of Wayne and the greater part of Holmes County, flowing southward into the Walhonding a short distance above the head of the Muskingum. It apparently is flowing in the main in the reverse direction from its old course. The headwater portion, down to within 8 or 10 miles of Wooster, found its old line of discharge northward past Lodi to the Black River, a tributary of Lake Erie. A boring recently made in this old valley near Lodi is reported by Todd to have reached a level less than 700 feet above tide without entering rock, the depth of the boring being 210 feet. It is quite certain that the old valley which leads northward along the Killbuck, as above noted, from Shreve to Wooster did not continue along this creek beyond Wooster, for there is only a narrow valley for several miles above Wooster, the width between rock bluffs being in places less than one-fourth of a mile. The continuation of that old valley (the old Mohican) was probably eastward, as suggested by Todd. A large part of Killbuck Valley apparently once discharged northward to the old Mohican, for there is a marked narrowing of the valley in passing southward down the present stream. Beneath the glacial gravel the valley is also filled with a fine silt, which was probably deposited in a pool of water that found outlet to the south only after rising above the level of a divide on the lower course of the creek. This silt is a conspicuous feature below Millersburg at least to the village of Killbuck, and seems to indicate that the divide was south of that village. That portion of the valley is narrow and winding, as if it had once constituted the headwaters of drainage lines, but the precise position of the old divide was not determined. After this divide had been surmounted the south-flowing stream carried down the valley to the Muskingum a large amount of gravel of Wisconsin age that is now preserved in the form of terraces on the valley borders. OLD UPPER TUSCARAWAS DRAINAGE SYSTEM. It was noted above (p. 158) that the Tuscarawas crosses an old divide between the mouth of One Leg Creek and Canal Dover. This is one of 166 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the most plainly marked instances of the crossing of an old divide to be found in northern Ohio. The Tuscarawas, whose valley above the mouth of One Leg Creek is fully one-half mile in average width, enters a gorge below the mouth of this creek which is scarcely twice the width of the stream, or but 150 to 200 yards. The gorge is a winding channel about 4 miles in length, which was probably mainly drained southward to the Lower Tuscarawas, for the old divide appears to be within a mile of its north end. In this gorge, 1 to 2 miles below the mouth of One Leg Creek, the river is running on the rock floor. Above the gorge, at the mouth of One Leg Creek, the rock floor is known to be more than 100 feet below the stream bed, a boring on its flood plain having failed to reach rock at a depth of 130 feet. A few miles below the gorge, at Canal Dover and New Philadelphia, borings have shown the rock floor to be nearly 150 feet below the stream bed. There is, therefore, not only the marked constriction of the valley, but also the presence of a concealed rock divide to prove that the Tuscara- was is there opening a new channel. The small size of this gorge compared with other channels across old divides in this part of Ohio is a matter on which further light is needed. The gorge is much smaller than the part of Sugar Creek Valley near Strasburg, which, as noted above, is thought to have been opened by a reversal of drainage. These disparities in size may prove to be due simply to difference in resistance afforded by the rocks in the two localities, for the valleys of that region present surprising variations in width, which seem due solely to rock texture. For example, the valley of One Leg Creek, whose usual width in its lower course is less than one-half mile, expands near New Cumberland to a width of more than a mile and then contracts near its mouth to a width of about one-third of a mile. The valley of the Tuscarawas at Canal Dover is exceptionally broad, being more than a mile in width, yet it appears to be the headwater portion of the old Lower Tuscarawas. In case rock texture proves inadequate to account for the exceptionally small size of this gorge across the old divide, it becomes nec- essary to consider whether its opening does not date from the Wisconsin stage of glaciation, while the opening of the broader channel in the lower course of Sugar Creek dated from an earlier invasion. The consideration of this question would also carry with it an inquiry into the question whether the lower course of Sugar Creek may have furnished the southward line of j : 1 : ; : OLD UPPER TUSCARAWAS DRAINAGE SYSTEM. 167 interglacial discharge for the Upper Tuscarawas drainage. These matters can scarcely be decided in the present stage of investigation. It can only be said that there appears to be nothing in the features of the region that would have seriously interfered with the interglacial drainage of the Upper Tuscarawas through the lower course of Sugar Creek. Above this old divide the drainage was formerly northward to the Lake Erie Basin. One Leg Creek was the main line of headwater drainage, but at Bolivar Sandy Creek entered from the southeast, and at Navarre Sugar Creek entered from the southwest. The course of the old stream from this point is less easy to determine, for the drift is so heavy in that region that the old valleys are in places completely filled. It may have left the Tuscarawas Valley and passed eastward along an abandoned valley, in which Richville stands, to the vicinity of Canton, though quite as probably that abandoned valley was the line of westward discharge for an eastern tributary that drained the headwater portion of Nimishillen Creek. In that case the old stream passed northward along the Tuscarawas Valley. That valley above Navarre seems wide enough as far north as Massillon to have carried the drainage of the old stream, but from Massillon to Clinton, a distance of about 12 miles, it seems much too narrow for the old stream. There was apparently an old divide at the bend of the present stream 3 or 4 miles north of Massillon, the valley being narrow and having a rock floor at slight depth. It seems not unlikely that the old stream had a westward discharge from Massillon along a depression utilized by the Pittsburg, Fort Wayne and Chicago Railroad, between Massillon and Orrville. It would there connect with the old Mohican Valley, which, as indicated above (p. 164), probably discharged northeastward to the old Cuyahoga. The thought that this may have been the line of discharge for the old Upper Tuscarawas did not oceur to the writer while in the field, and too little attention was given the valley to justify an opinion. While it is a somewhat indirect course, that may not be a serious objection. So little is known concerning the district east of the Tuscarawas that it is impossible either to suggest an alternative line of discharge or to rule it out. The old line may be found to have continued northward from the vicinity of Massillon on the east side of the present stream past Turkeyfoot Lake, which, apparently, lies in an old valley, and to have come to the Tuscarawas again a short distance above New Portage. It would there connect with an old valley coming in from the 168 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. southwest and pass northward through Copley Marsh to the old Cuyahoga, a few miles northwest of Akron. These courses are suggested on the assumption that the old line of dis- charge passed northward to Massillon; but as noted above there is a pos- sibility that it led eastward to Canton. In that case it is not certain that the discharge was into the Cuyahoga. It may prove to have been north- eastward to the Mahoning at Alliance and thence northward into the Grand River Basin. It seems, however, quite as probable that the discharge would have been northward from Canton past Turkeyfoot Lake and Copley Marsh to the Cuyahoga. Notwithstanding this uncertainty concerning the course of discharge, there is no question that the old Upper Tuscarawas was tributary to the Lake Erie Basin. This northward-flowing system apparently embraced the greater part of Sugar Creek drainage basin and all the eastern tributaries of the Tuscarawas from One Leg Creek northward to the source of the river, though these tribu- taries have had their drainage basins greatly modified. At the supposed old divide on Sugar Creek, near Strasburg, the valley becomes reduced to scarcely half the width of the portion above, though the narrowest part has a breadth of nearly one-fourth of a mile. The evidence for the former northward discharge of this creek is greatly strengthened by the presence of a broad, partially filled valley leading northward from the bend at Beach City to the Tuscarawas at Navarre, which is utilized by both the railway lines that pass through these villages. The possibility that the lower course of, Sugar Creek was a line of interglacial discharge for the old Upper Tuscarawas was considered above. It is probable that only the lower course of Nimishillen Creek was tributary to Sandy Creek, the old divide being 3 or 4 miles below Canton, where the valley becomes very narrow. As noted above, it is uncertain whether the headwater stream of this drainage system discharged westward past Richville through an abandoned valley to the old Tuscarawas at Navarre, or instead met the old Tuscarawas at Canton. The northern portion of this old drainage system is evidently not in harmony with pre- glacial lines. Whether the extent of the present system is about the same as the old system is not easy to determine because of the great body of drift in that region. HOCKING DRAINAGE BASIN. 169 HOCKING RIVER. THE PRESENT DRAINAGE. The Hocking drainage basin lies southeast of the southern part of the basin drained by the Muskingum. It has its headwaters on the east side of the Scioto Basin, near Lancaster, and connects with the Ohio at Hocking- port. The length of the main stream is searcely 100 miles, and the area tributary to it is only 1,200 square miles. The fall of the main stream is about 250 feet between Lancaster and the mouth, a distance of perhaps 90 miles. Of this fall about 100 feet is made in the first 25 miles. The headwater portion of the basin carries a drift filling of 200 to 300 feet, but the middle and lower portions have but a moderate filling. They lie outside the glacial boundary, and have received a train of gravel and sand which was carried down toward the Ohio, and which graded up the valley to a level 75 to 100 feet above the present stream. The stream has carried away much of this gravel and sand, leaving only narrow strips of it as terraces on the borders of the valley and a small fillmg beneath the stream bed. CHANGES IN THE HEADWATER PORTION. There is no doubt that the headwater portion of Hocking River, as far down as the glacial boundary, and also nearly all the tributary drainage within the glacial boundary, formerly discharged northwestward into the westward outlet of the old Muskingum. This is indicated both by the slope of the rock floor and by abandoned valleys which connect the headwaters of the Hocking and its tributaries with the portion of the Scioto Basin traversed by the old Muskingum. The rock floor is shown by numerous gas borings at Sugar Grove to be about 650 feet above tide, while at Lan- caster, 7 miles up the present valley, it is only about 600 feet, and at Had- ley Junction, near which it connected with the old Muskingum, 550 feet. The valley from Sugar Grove to Lancaster is nearly a mile in average width, and becomes still wider as it opens into the Scioto Basin northwest of Lancaster. Yet the bordering uplands near Sugar Grove are higher than in any part of the Hocking drainage basin below that village, the highest points being above 1,200 feet, or nearly 600 feet above the rock floor of the valley. Within 8 or 10 miles below Sugar Grove the uplands fall to about 1,050 feet. Within 3 miles the valley narrows to scarcely one-third its width 170 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. at Sugar Grove, or about one-fourth of a mile; it continues narrow for the next 5 miles, and below it is irregular and varies in width from one-fourth mile up to nearly a mile. The level of the rock floor in the narrow part below Sugar Grove, as shown by gas borings, is about the same as at that village, 650 feet, but farther down it appears to descend with the present stream. From the features just noted it seems probable that the old divide stood within a few miles southeast of Sugar Grove, but its precise position may be difficult to determine. Beginning a short distance below Sugar Grove there are shelves along the borders of the valley at a height of 50 to 75 feet above the stream, or about 800 feet above tide; these seem to be remnants of an old gradation plain. By means of these rock shelves it may be possible to determine the condition of the old divide, but this has not as yet been done. It is still to be determined whether the portion of the Hocking Valley below this divide belonged to a single or to two or more distinct old drainage systems. Upon turning to the tributaries of this headwater portion of Hocking River we find important changes. Clear Creek now drains a district east- ward into the Hocking that was in large part drained westward into the Scioto Basin. The old divide between the westward-flowing stream and a much smaller stream flowing eastward into the Hocking is found about 4 miles from the mouth of the creek. The creek here passes through a gorge only 100 to 150 yards in width, or but a small fraction of its width near its present headwater portion. Above this gorge the tributaries of the creek point westward, while in the portion below they point eastward. The bluffs at this gorge rise abruptly more than 100 feet, and it is probable that the pass or col stood nearly as high as this abrupt part. This old divide is very near the glacial boundary, but a terrace of glacial gravel appears farther down the valley, at an altitude about 100 feet above the stream bed. This gravel is apparently of Illinoian age; this being the case, the stream was thrown across this divide as early as that ice invasion. Changes of drainage on Rush Creek, the largest eastern tributary of this headwater portion of the Hocking, have been noted both by Tight and the writer. An abandoned valley, forming the old line of discharge from Bremen to Lancaster, was examined by the writer in 1890, and the cause for abandonment referred to great accumulations of drift immedi- ately below Bremen. The position of the old divide crossed by the stream wen ce ee ee ee — HOCKING DRAINAGE BASIN. 171 in its present course south of Bremen was not determined. Tight examined this drainage basin in 1896 and located the old divide about 6 miles below Bremen. He also independently reached the conclusion that the stream formerly discharged westward from Bremen to Lancaster through the par- tially filled valley noted by the writer. This change of drainage has been discussed quite fully by Tight, and his description is accompanied by photographs of the abandoned valley and of the old divide.’ Through a misinterpretation of the maps of that region, he has placed the old divide at the line of Fairfield and Hocking counties. Its position is really 2 miles below the county line, in section 10, Marion Township, Hocking County, where the photograph of the old divide was taken which appears in the paper referred to. At this old divide a ledge of rocks extends out fully halfway across the valley, reducing the width of the channel to scarcely 200 yards. This remnant of the col probably stands nearly as high as the old divide, and shows it to have been scarcely 50 feet above the present stream. The valley was filled with glacial deposits to a higher level than this remnant of the divide, for it is coated with gravel to a depth of several feet. The glacial boundary apparently follows somewhat closely the north side of Rush Creek from this old divide westward to its mouth at Sugar Grove. East from the old divide the drift border lies farther south than the stream, except in the extreme headwaters east of Junction City. A peculiar change of drainage is found at Sugar Grove, near the mouth of Rush Creek. There are two broad channels opening out from Rush Creek Valley into the Hocking just above its mouth, which stand less than 50 feet above the stream, and yet are not utilized by the stream. Instead, the creek has turned away from both of them and cut a narrow gorge across a rock point on the east side of the valley. The point thus cut off rises nearly 100 feet above the level of these broad valleys, but the stream probably found a notch or depression back of it at a somewhat lower level. It seems necessary to suppose that both of these broad valleys were at one time filled sufficiently to cause the stream to select its present course. Yet it is difficult to account for the removal of the obstruction unless, perchance, the ice sheet was the obstruction. The occurrence of two broad channels is also a puzzling feature. They do not appear to be in the natural position for an oxbow channel of 1Bull. Denison Univ., Vol. IX, Pt. II, 1897, pp. 33-37, Pls. D, E, F, and IV. 1742 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. either the old north-flowing Hocking or the lower course of Rush Creek. Each is about as broad as the valley of Rush Creek above the point of sepa- ration from the latter, being nearly one-half mile in width, but they are decidedly narrower than the Hocking Valley. They seem too broad to have been excavated by an interglacial stream, and it appears more probable that the double channel is a preglacial feature. A slight change in one of the eastern tributaries of Rush Creek, between the point where it leaves the old valley near Bremen and the old divide, should be mentioned. This tributary enters Rush Creek within a mile inside the glacial boundary, yet its lower course was so greatly obstructed by drift deposits that it has cut a new channel across a rock point south of the old channel. The North Fork of Rush Creek enters the main creek through a rock gorge between Rushville and Bremen. he headwater portion apparently discharged westward near the line of the Ohio Central Railway, leaving the present valley about 2 miles above Rushville. The course is so greatly concealed by accumulations of drift that it can be only approximately determined. RACCOON CREEK. Passing over a few small northern tributaries of the Ohio below the mouth of Hocking River we come to the valley of Raccoon Creek. The sources of this creek are in western Athens and southern Hocking counties, on the immediate border of the Hocking Valley. One branch heads near the line of Athens and Hocking County within 14 miles of the Hocking River and branches farther west are but 4 to 6 miles back from the river. The divide at the head of these tributaries is a prominent sandstone ridge with an elevation 200 to 300 feet above the Hocking Valley or 900 to 1,000 feet above tide. The heads of these tributaries are in valleys 100 to 200 feet below the crest of the dividing ridge, or about 800 feet above tide. “In the middle part of this drainage basin there are remarkable variations in the valley contours, the streams being partly in low lands which have the appearance of being old lines of drainage, and partly in narrow valleys, with abrupt bluffs, which have the appearance of being newly opened channels. The writer did not give these features sufficient attention to warrant an interpretation. They are, however, under investigation by Tight. SYMMES CREEK AND LITTLE SCIOTO RIVER. 173 SYMMES CREEK. Immediately west of the lower end of the Raccoon drainage basin is the basin of Symmes Creek. The stream heads a short distance southeast of Jackson and has a general southward course to the Ohio, which it enters opposite the city of Huntington, W. Va. An inspection of this drainage system suggests a northward discharge for the entire system except a sec- tion a few miles in length in the lower course. The writer was able to trace out a series of valleys connecting the two headwater forks in south- eastern Jackson County with the South Fork of Salt Creek. Grass Fork crosses an old divide within a mile north of the Jackson-Gallia county line. Its old line of discharge appears to have been in the reverse of the present course to the line of the Cincinnati, Hamilton and Dayton Railroad and thence westward past Clay, Vaughn, and Camba into Salt Creek. The region now drained by Black Fork appears to have discharged in part along the line of the railway just named from Gallia Furnace northward. The _ headwater portion of the creek may have discharged past Oak Hill, joing the other branch and Grass Fork at the swamp east of Clay. The present stream appears to have crossed an old divide in the vicinity of the county line a short distance east of Gallia Furnace. Tight reports the discovery of an old divide south of Aid about 15 miles from the mouth of the creek. The portion of the drainage basin between this divide and the one near Gallia Furnace may have found an eastward discharge into Raccoon Creek, passing near the village of Patriot; the divide there between Symmes Creek and Raccoon Creek is exception- ally low. LITTLE SCIOTO RIVER. This small stream drains the southern end of the abandoned part of the old Kanawha channel in southwestern Jackson, southeastern Pike, and eastern Scioto counties, Ohio. It is singularly out of harmony with the old channel, as may be seen by reference to the sketch map (fig. 3, p.101.) The east or Brushy Fork heads on the northeast border of the old channel about 3 miles north of Glade and takes a southward course, entering the channel at Glade and following it for about 6 miles. The stream then leaves the old channel near the line of Jackson and Scioto counties, and utilizes the channel of a little tributary. It is joined by Flat Fork, which leads eastward from California along the old channel, but which turns south 174 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. through a narrow rock-bound valley to enter Brushy Fork. The stream then follows the valley of this small tributary to its former head, 3 or 4 miles south of the county line. It then crosses an old divide into the valley of a larger stream coming in from near Mabees that discharged southwestward into the old Kanawha. It follows this valley down to the junction with Rocky Fork near Wallace Mills. The old valley of this tributary probably discharged westward from Wallace Mills to the old Kanawha along Rocky Fork (reversed), though possibly it continued down the line of the present stream and entered the old Kanawha channel near Harrison Mills. The distance to the old channel of the Kanawha, by either route, is only two miles from Wallace Mills. From Harrison Mills the Little Scioto River occupies the old channel nearly to the present Ohio. It, how- ever, cuts off a rock point west of the old channel, just before entering the present Ohio. Rocky Fork rises in the uplands west of the old Kanawha channel in southeastern Pike County, and follows that channel southward for several miles before turning east to joim Brushy Fork. In leaving the old channel it seems to have disregarded the most favorable line of discharge. The only cause for these incursions of the present drainage into the hills which has suggested itself to the writer is found in the large amount of filling which the old channel received, there being in places a depth of 60 feet of silt on the old rock floor. This amount of filling was perhaps suffi- cient to raise the dramage lines above the level of low divides among neighboring hills to the east and thus bring about the singular system of drainage presented by the Little Scioto and its tributaries. It is, however, somewhat doubtful if this silt fillmg caused all the changes, and they may prove to be independent of it. SCIOTO RIVER. The Scioto is the chief drainage system of central and southern Ohio. The main stream has a length of about 210 miles, and with its tributaries drains an area of 6,400 square miles. Its source is in eastern Auglaize County, and its mouth at Portsmouth, Ohio. The region drained by the Scioto and its tributaries has undergone a series of changes of peculiar interest, some of which have been outlined in the discussion of the Ohio and Muskingum drainage basins. The present SCIOTO DRAINAGE SYSTEM. 175 System presents very few lines which are identical in extent and direction of drainage with the old system; indeed a large part is quite independent of the old system. THE HEADWATER PORTION. In the northern portion of the present system from the source down to the glacial boundary near Chillicothe the extent and the direction of dis- charge for the main stream and its tributaries are determined chiefly by the slope of the great Scioto Basin, the drift filling being so great as to nearly conceal the lines of preglacial drainage. This basin slopes from the eastern and western borders toward a north-to-south axis, while the axis itself has a decided southward slope. Moraines govern the courses of drainage only to a limited extent. The Scioto itself leads down from the western rim to the axis of the basin in an eastward course, which is governed by a moraine lying on the north side of the river. It is met near Marion by a small northeastern tributary, Little Scioto River,’ whose course is along the south border of the eastward continuation of the same moraine. The united stream then takes a southward course, but flows a little to the west of the axis of the basin as far as Columbus. In this portion the axis of the basin is more nearly fol- lowed by the Olentangy River, which for a distance of about 40 miles lies only 4 to 8 miles east of the Scioto. The two rivers become united at Columbus, where the Scioto makes an eastward turn to receive the Olentangy. From Columbus to Chillicothe the Scioto follows nearly the axis of the basin. The Scioto receives three western tributaries above Columbus—Rush Creek, Bokes Creek, and Mill Creek. Each of these, like the main stream, rises on the elevated western rim of the basin. The courses of these tributaries are governed to some extent by morainic ridges, there being a ridge between Mill Creek and Bokes Creek, and another along a part of the north border of Rush Creek. Below Coluinbus three large western tributaries—Darby Creek, Deer Creek, and Paint Creek—are received. Darby Creek flows eastward from the western rim of the Scioto Basin along the south border of a morainic ridge to within a few miles of the Scioto. It there turns southward and joins the Scioto near Circleville. Its chief 1This stream must be distinguished from a tributary of the Ohio of the same name which, as above described, enters the Ohio a few miles east of the mouth of the Scioto. 176 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. tributary, Little Darby Creek, also heads in the elevated western rim of the Scioto Basin. Deer Creek heads in the western rim of the Scioto Basin and drains a narrow strip on the southwest border of the Darby Creek drainage basin, entering the Scioto about midway between Circleville and Chillicothe. Paint Creek with its several forks drains the southwestern part of the Scioto Basin and enters the Scioto at Chillicothe. As shown on Pls. II and XIII, the courses of several of its forks are governed largely by moraines. . The Scioto receives no eastern tributaries of importance above the mouth of the Olentangy River. The northeastern part of the Scioto Basin is drained by three south-flowing streams—Olentangy River, Alum Creek and Walnut Creek—each of which has a drainage basin but 5 to 10 miles in width. With the exception of the headwater portion of Walnut Creek, which is kept in a southward course by a moraine, these streams show little regard for morainic ridges. Their courses are in the direction of the most rapid slope of the basin. The Olentangy River, as above noted, enters the Scioto at Columbus, Alum Creek enters Walnut Creek a short distance south of Columbus, and the united stream enters the Scioto near Lockbourne, a few miles farther south. Just before entering the Scioto it is jomed by Little Walnut Creek, a stream which rises near the Licking reservoir and, as above noted, follows nearly the line of the old westward outlet of the Muskingum down to the Scioto. The portion of the Scioto drainage basin just described hes within the limits of the Scioto glacial lobe, which occupied the region as late as the Wisconsin stage of glaciation. The valleys are nearly all postglacial and are shallow and narrow, the depth seldom reaching 50 feet, while the width is commonly less than one-fourth of a mile. In places the valleys extend down through the drift into the rock, notably along the Scioto above Columbus and on the lower course of Alum Creek, but, as a rule, their beds are far above the level of the rock floor. It seems hazardous at present to attempt to restore the old systems of drainage in this northern part of the Scioto drainage area. In the area drained by Paint Creek it is possible to trace preglacial valleys for some distance back from the Scioto. The main creek from Bainbridge eastward nearly to Chillicothe occupies a preglacial valley about a mile in width and fully 300 feetin depth. Before joining the Scioto, SCIOTO DRAINAGE SYSTEM. 177 however, it crosses a rock point in the old south bluff, as indicated by Orton.’ The old drainage system, of which this valley is the lower course, probably drained an area of several hundred square miles, but as yet only a few of the old tributary lines have been traced. It was noted several years ago by H. W. Overman, county surveyor of Pike County, that the headwater portion of Brush Creek above Fort Hill formerly discharged to the preglacial valley of Paint Creek at Bain- bridge.” This interpretation was independently reached by the writer in 1889, and by Tight and Fowke a few years later.* There is a well-defined though partially filled valley connecting it at the north with Paint Creek, while at the south, near Fort Hill, the present stream is cutting a gorge across a low pass in the old divide. ‘The region now drained by Rocky Fork, a branch of Paint Creek, appears to have been drained by a line farther north, whose valley is only partially filled. A few suggestions of the old courses of drainage were obtained in northern Highland County and in Fayette County, but they are scarcely complete enough to justify a mapping or full interpretation of the lines of discharge. THE LOWER COURSE. The Scioto Basin terminates on the south at the hills of Ross County, just above Chillicothe. The Scioto there enters a district in which the hills rise 400 to 500 feet above the stream, and flows in a valley but little more than a mile in average width. The evidence that this lower course of the Scioto has now a discharge in the reverse direction from that of the old system has been so fully presented in connection with the discussion of the Ohio that only this passing reference seems necessary. WESTERN TRIBUTARIES SOUTH OF THE GLACIAL BOUNDARY. South of the glacial boundary the western tributaries of the Scioto are all small, and all are following their old lines. The most important one is Scioto-Brush Creek which drains the northwestern part of Scioto County and the eastern border of Adams County. Sunfish Creek drains much of the western half of Pike County, while Camp Creek and Bear Creek drain 1Geology of Ohio, Vol. II, 1874, pp. 653-655. 2Ohio Archeological and Historical Quarterly, Vol. I, 1887-1888, pp. 260-264. ’Bull. Denison Uniy., Vol. LX, Pt. 1, 1895, pp. 15-384. MON XLI——12 178 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. each a small strip between the two tributaries just mentioned. ‘The lower courses of these tributaries have been filled to some extent with silt and slack-water material, as a result of the filling of the Scioto Valley with glacial gravel. BEAVER CREEK. There are two important eastern tributaries of the Scioto entering south of the glacial boundary, Beaver Creek and Salt Creek. Beaver Creek is very small, but is of importance, as it occupies the broad channel of the old Kanawha from near Glade westward to the vicinity of Pikeville (see fig. 3, p. 101). It leaves the old valley near Pikeville and cuts across a rock point on its south border, passing into the Scioto below, while the old valley connects with the Scioto at Waverly, 3 miles above Pikeville. The silt filling in the old valley has perhaps been sufficient to cause this deflection of the present drainage. SALT CREEK. Salt Creek embraces a widely branching drainage system, with an area of about 500 square miles, which connects with the Scioto near the glacial boundary, a short distance below Chillicothe. There are really three drain- age basins, which become united at the east border of the Scioto Valley and have a common line of discharge across the Scioto bottoms into the river. These are known as North Fork, Middle Fork, and South Fork of Salt Creek. North Fork drains the southwestern third of Hocking County and adjacent portions of Fairfield, Pickaway, Ross, and Vinton counties, its line of discharge being southeastward from Fairfield County across the eastern edge of Pickaway into Hocking County, and thence west of south across western Vinton and eastern Ross County. Middle Fork drains a much smaller area, lying in western Vinton and northern Jackson counties. South Fork drains about half of Jackson County northwestward through south- eastern Ross County, and includes a few square miles of eastern Pike County. That the North Fork of Salt Creek has been greatly enlarged by headwater accessions is so evident that several residents of the region who _ have no knowledge of geology have made a clear interpretation of the changes of drainage. They have noted a troughlike depression leading from near the head of the North Fork, in Pickaway County, westward up Plum Run, and thence onward across a marshy divide to Scipio Creek, and down that creek to the Scioto. This depression is a mile or more in width, and SALT CREEK DRAINAGE SYSTEM. 179 is filled for a great depth with drift. They have also correctly placed the old divide at ‘‘the narrows,” just above the line of Hocking and Vinton counties. The stream follows the broad valley southeastward past Adelphi and Haynes to the mouth of Queer Creek. It there turns southward into a much nar- rower valley which soon contracts to a width but little greater than the stream, showing clearly the position of the old divide. After passing the old divide the valley gradually widens as the old southward-flowing drainage is entered. An oil boring recently made in the middle of this valley near the mouth of Queer Creek shows the rock floor to be only 35 feet below the present stream. The stream is estimated to be not far from 650 feet above tide at that point, making the rock floor fully 600 feet. This is sufficiently low to fit im well with the altitudes of the valley floors in the midst of the Scioto Basin, which are found to be not far from 550 feet above tide. Probably the drainage along the line of the old channel from Adelphi to the Scioto was somewhat different from the present, for the tributary valleys have usually been completely concealed by drift. Laurel Creek, which - enters at Adelphi, cuts off a rock point near its mouth. As a result of this filling it enters the stream a short distance east of the old mouth. At this place its valley is narrowed to scarcely one-eighth the width of the old valley. The portion of the North Fork south of the old divide lies outside the glacial boundary, and it seems to have suffered no change aside from that of the accession above described. The Middle Fork of Salt Creek lies outside the glacial boundary and apparently drains all of its old drainage basin. Only the lower course was examined by the writer, and this has a valley but 60 to 100 rods wide, which seems a natural width for a drainage basin of this size. The South Fork of Salt Creek has suffered some reduction in the size of its drainage basin. It formerly received the headwater portion of Symmes Creek, as indicated in the discussion of that stream. The present divide at Camba is in a valley which opens northward and carries a silt fill- ing of considerable depth. This silt is calcareous, a feature which indicates that it was derived from the glacial waters, for this is a sandstone region. The valley seems to have been ponded with water to such a height that an outlet was found across a low divide at its head. The amount of glacial 180 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. water passing through this valley was apparently very great, for it lef. a silt deposit nearly 100 feet in depth. This stream has a valley 80 to 120 rods in width from a point near the present divide at Camba northward to the junction with Buckeye Creek, 2 miles below Jackson. It there enters the Logan conglomerate and becomes narrowed abruptly to a width of less than 200 yards. It continues narrow nearly to its junction with Middle and North forks. This constriction does not appear to mark an old divide, but on the contrary seems to be due entirely to the great resistance of the conglomerate to erosion. LITTLE MIAMI RIVER. Little Miami River, which enters the Ohio just above Cincinnati, is the first large northern tributary below the Scioto, yet the distance between the mouths of the two streams is more than 100 miles. The source of the stream is a few miles southeast of Springfield, Ohio, and the course is west of south to the Ohio. The length of the stream is about 100 miles and the drainage area probably 1,850 square miles. The East Fork, which is a nearly independent drainage basin, rises in southeastern Clinton County, a few miles east of Wilmington, and enters the main stream about 10 miles above its mouth. Two other important eastern tributaries are Todds Fork, entering at Morrow, and Ceesars Creek, entering near Waynesville. There are no large western tributaries. RATE OF FALL. The source of the main stream and also that of Hast Fork are at an altitude of about 1,150 feet above tide, while the mouth is less than 450 feet. The fall is therefore rapid, that of the main stream averaging about 7 feet per mile, while that of the Kast Fork is fully twice as rapid. In the 35 miles from its source to a point opposite Xenia the fall of the main stream is nearly 400 feet, but in the next 35 miles, to Morrow, it is about 130 feet, or only one-third as rapid as the headwater portion. In the lower 30 miles the fall is about 180 feet, it being more rapid than in the middle portion. CHANGES IN DRAINAGE. The headwater portions, both of the main stream and of its tributaries, flow in shallow valleys 50 to 60 feet or less in depth, but from a few miles below Xenia to the mouth the valley is 200 to 800 feet or more in depth. LITTLE MIAMI DRAINAGE SYSTEM. 181 This deep portion apparently unites at least three old valleys which formerly discharged westward into the Great Miami Basin, as indicated below. In the headwater portion the streams are in places entirely independent of the old drainage lines, and there is evidently but little harmony between the present drainage system and the old one. A hint concerning the old discharge of a part of the Little Miami Basin into the Great Miami is given by Orton in his map of Warren County, Ohio, though his description leaves the direction of discharge uncertain.’ A drift- filled lowland departs from the Little Miami at Deerfield (South Lebanon) and passes northwestward. to the Great Miami just below Middletown. It appears to have been a line of discharge for the middle part of the Little Miami into the Great Miami drainage basin. The only element of uncer- tainty is the report that wells in the lowland near the present divide have in some instances entered rock at higher levels than those in parts of the lowland nearer Little Miami and Great Miami rivers. These, however, do not rule out the presence of a channel at a little distance from the wells. In the Little Miami near Fort Ancient, a few miles above Deerfield, there is a notable constriction, which was apparently the site of an old divide. Another divide was probably situated below Deerfield, near the south line of Warren County. Between these divides there appears to have been a drainage system which embraced most of the area now drained by Todds Fork, as well as a small section of the Little Miami which led north- westward through the lowland above mentioned to the Great Miami. The headwater portion of the Little Miami, down at least to the vicinity of Xenia, appears to have connected with the Great Miami through the lower course of Mad River. There is an open channel between the two rivers that is now drained to the Little Miami by Beaver Creek. This evi- dently was used as a southward discharge for glacial waters, but it seems probable that earlier it may have constituted a lme of northward discharge from the headwater portion of the Little Miami into Mad River. Possibly the course was not coincident with the open channel, for on the border of the channel there is a morainic belt that greatly disguises the old features. The East Fork is in an old valley in its lower course, but the headwater portions are largely independent of the old drainage lines. It seems prob- able that a part of the region now drained southward to the Ohio by Brush 1Geology of Ohio, Vol. III, 1878, p. 382. *Compare Bownocker: Ohio Acad. Sci., Special Paper No. 3, 1900, pp. 32-45. 182 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Creek once discharged westward through the lower course of the East Fork of Little Miami. This may have embraced the entire portion between the old divide crossed by Brush Creek near Fort Hill and another supposed divide located by Tight east of West Union.” The amount of drift is so great in the region between Brush Creek and the East Fork that few surface indications of the courses of the old drainage lines can be found. GREAT MIAMI RIVER. THE PRESENT SYSTEM. The Great Miami is the main drainage system of western Ohio. Near its mouth it receives Whitewater River, which drains an area of about 4 ,000 square miles in southeastern Indiana. The Whitewater, however, is here treated as a separate system. Exclusive of the Whitewater, the Great Miami has a drainage area of nearly 4,000 square miles, or about one-tenth of the State of Ohio. Its headwaters are im the divide which separates the Mississippi from the St. Lawrence drainage. It drains the greater part of the Cincinnati arch from that divide south to the Ohio River. The main stream has its headwaters about 1,000 feet above tide. Its main eastern tributary, Mad River, heads in a more elevated tract in Logan County, whose highest points exceed 1,500 feet. The source of Mad River, however, is in a valley-like depression, standmg about 1,300 feet above tide, which also constitutes the source of Rush Creek, a western tributary of the Scioto. Whitewater River, the main western tributary, heads in the most elevated part of Indiana, at an altitude of nearly 1,200 feet. The main stream and its headwater tributaries, as far down as the vicinity of Dayton, flow in comparatively shallow postglacial valleys, with courses largely independent of the old drainage lines, the amount of drift being so great as to completely fill. the old valleys. Mad River, it is true, occupies a broad trough-like valley throughout much of its course, but on its borders there are moraines which cause most of the relief, the immediate blufts beg generally but 20 to 30 feet in height. Furthermore, its course seems to be independent of the old drainage Below Dayton the Miami and some of its tributaries occupy old val- leys which were only partially filled with glacial deposits. The work of the present streams is mainly the reexcavation of the valleys. In this 1Communicated to the writer. GREAT MIAMI DRAINAGE SYSTEM. 183 work they have fallen far short of reaching the old rock floors, which lie 100 to 200 feet below their beds. The depth of this reexcavation is but 50 to 100 feet, and the width but a small fraction of that of the old valleys, seldom so much as one-fourth as great. The contrast between the southern and northern portions of this drainage basin, therefore, is not found in the work of the present streams, but is due to the less complete conceal- ment of the old drainage lines by glacial deposits. CHANGES IN DRAINAGE. J. A. Bownocker has recently presented a partial restoration of the old drainage in the headwater portion of this drainage basin. The course of the old drainage line has been made known by borings for oil and gas, which are numerous in that region. It is not perceptible on the surface except for a few miles in eastern Indiana, where a sag or shallow valley marks its course. The present systems of drainage show a nearly complete disregard of the old drainage lines. The course of the old line, as noted by Bownocker, is northwestward from near the Great Miami, in Shelby County, Ohio, past Anna and the Grand reservoir, to Rockford, Ohio, on the St. Marys River. It there turns southwestward, crosses the Wabash River at Geneva, Ind., and continues past Pennville into Blackford County, Ind., where the tracing was discontinued. The length of the line thus traced is about 90 miles. This old line received a southern tributary at the Grand reservoir, with a head probably near Xenia, but no other well-defined tributary was recognized between that point and Blackford County. Two channels were there found, one of which leads northward and the other westward, but the data are insufficient to show which was the main channel. The width of this old valley appears to be about 1 mile, with a possible range from three-fourths of a mile to 1$ miles. The filling of drift is found to range from 320 feet up to 514 feet, the variation being principally due to the different altitudes of the present surface. The rock floor is not far from 500 feet above tide in the eastern portion, but falls to scarcely more than 400 feet in eastern Indiana. It is markedly higher than the Ohio at the mouth of the Great Miami, whose rock floor is less than 400 feet above tide. The course seems to show that it was a tributary of the 1A deep preglacial channel in western Ohio and eastern Indiana, by J. A. Bownocker: Am. Geologist, Vol. XXIII, 1899, pp. 178-182. Also Ohio Acad. Sci., Special Papers No. 3, pp. 32-45, with map. 184 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. old Wabash system. The size of the valley indicates that it drained at most only a few counties of western Ohio. The old drainage of a consider- able part of the region now drained by the Great Miami appears to have been independent of this line. It is probable that the old drainage south from the latitude of Dayton followed nearly the course of the present limes to the Ohio. As already indicated, the old Ohio was entered by the Great Miami near Hamilton. The latter stream makes slight departures from the line of the old Ohio below Hamilton, the old Ohio channel being in part farther west than the Great Miami. WHITEWATER RIVER. OUTLINE OF THE PRESENT SYSTEM. Several streams which have their sources in a moraine in southern Randolph County, Ind., and southwestern Darke County, Ohio, converge southward to form the Whitewater River. These are known as West Fork, Martindale Fork, Greens Fork, Nolands Fork, and East Fork. The first four become united between Cambridge and Connersville to form the West Whitewater; the fifth (Hast Fork) unites with the West Whitewater at Brookville. The area of the entire Whitewater drainage basin is about 1,500 square miles. : The headwater portions for 15 to 20 miles are flowing in channels cut in the drift. The East Fork then, near Richmond, enters the rock, and has carved its course partly in rock from that point to Brookville. The West Fork encounters rock at only a few points. Below Connersville it is in a partially filled preglacial valley, with broad bottom and elevated uplands on either side. The West Fork, with its headwaters, constituted an important line of drainage for the waters from the ice sheet at the time the moraine above referred to was forming, and probably also at earlier stages in the Glacial epoch. It is im consequence a gravel-filled valley, and the work of the present stream has been merely a removal of a small portion of these gravel deposits. Above Cambridge it has cut scarcely 20 feet into these deposits. The depth gradually increases southward to Brookville. At Brookville and below that city it has formed a channel 60 to 75 feet in depth. The surface of the gravel deposits in the headwater portion above Cambridge has a southward descent of nearly 10 feet per mile. From Cambridge to the TRIBUTARIES OF THE OHIO IN INDIANA. 185 State lme at Harrison, Ohio, a distance of scarcely 70 miles, the gravel deposits have a descent of 350 feet, or fully 5 feet per mile. The present stream, having cut about 50 feet deeper into the gravel deposits at Harrison than at Cambridge, has a fall of nearly 6 feet per mile. CHANGES IN DRAINAGE. Possibly the northern part of this drainage basin, like that of the Great Miami, was formerly drained westward toward the Wabash, for channels of great depth are occasionally encountered by oil and gas borings in the dis- trict to the west. There is, however, some doubt as to such a drainage course, for the size of the lower end of the Whitewater Valley seems to require a drainage area nearly as large as the present, the width of the valley being about a mile and the depth 500 feet. Furthermore, the large valley occupied by the southern part apparently drained, as now, to the Ohio. The rock floor at Brookville is shown by gas borings to be about 490 feet above tide. At a boring 5 miles below Brookville it is only 450 feet; while at the mouth of the stream, 18 miles farther down, it is less than 400 feet. TRIBUTARIES OF THE OHIO IN INDIANA. Between the mouth of the Great Miami at the east line and the mouth of the Wabash at the west line of Indiana there are no large northern tributaries of the Ohio. This is owing to the fact that the drainage of the ereater part of Indiana is toward the Wabash, instead of directly to the Ohio. A tributary of the Muscatatuck heads within 2 miles of the. Ohio near Madison, Ind, and yet leads westward to the Kast White and thence across the State to the Wabash. Nearly all of the tributaries in southern Indiana head within the limits of the counties that border the river, and consequently have a length of less than 30 miles. Only two, Blue River and Laughery Creek, have greater length. In southwestern Indiana, where the altitude is low, the streams have very little fall, and are occupying broad, shallow valleys, which are not infrequently filled to depths of 50 feet or more with marshy alluvium. In the more elevated tracts, whose western border is crossed by the Ohio between Cannelton and Rockport, Ind., the streams present valleys cut to a corre- spondingly greater depth. Their bottoms are narrow and well drained, the e 186 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. fall of the streams being adequate to give rapid escape for the surplus rainfall. The streams make a descent of 300 to 500 feet, in some cases, within a dis- tance of 10 to 20 miles. Notwithstanding this descent there are very few waterfalls. The only notable ones occur in southeastern Indiana, where the drift deposits have obstructed the old valleys and led to the development of new lines of drainage. In the unglaciated portion of southern Indiana there are but few rock rapids, and, so far as the writer is aware, no waterfalls. The gradients of streams, though steep, show a gradual lessening in rate of descent in passing from source to mouth and a general disregard for hardness of strata, such as results only from maturing of a drainage system. The rapid rate of descent is not favorable to the development of broad flood plains, yet there is usually a flood plain having several times the breadth of the stream bed. In this respect the tributaries, as noted above, have accom- plished more work in proportion to their size than the Ohio. It is difficult to realize that the broad valleys of small streams in southwestern Indiana were begun at no earlier date than the narrow valleys of the higher district, yet such was probably the case. WABASH RIVER SYSTEM. The drainage basin of the Wabash embraces an area of about 33,000 square miles, distributed as follows: In Ohio, 400 square miles; in Indiana, 24,350 square miles; in Illinois, 8,250 square miles. It drains, therefore, slightly more than two-thirds of Indiana, the area of the State being 35,910 square miles. Of the portion in Indiana, about one-half is embraced in the drainage area of the Kast White and West White rivers. By including these drainage areas with the Wabash the entire watershed has a nearly symmetrical, broadly ovate form. Not including the White River system, the Wabash watershed is an unsymmettical, elongated tract, curving around White River. Only a small part of the Wabash watershed lies outside the glacial boundary. ‘The Wabash and West White rivers lie within that boundary for their entire length. The East White flows within the glacial boundary to western Jackson County, but from that point to western Martin County it is outside the drift. It enters the drift-covered district in its lower course near the corners of Martin, Davis, and Dubois counties, and remains within the glacial boundary from that point to its mouth. The greater part of WABASH DRAINAGE SYSTEM. 187 this system being within the limits of glaciation, and in a region where the drift coating is sufficiently thick to conceal more or less completely the pre- glacial valleys, it has been largely developed in interglacial and_post- glacial time. The lower courses of the Wabash, West White, and East White are, however, following nearly the preglacial lines. WABASH RIVER. The valley occupied by the Wabash River has not had a uniform development from source to mouth. In its upper part, from the source to Huntington, Ind., the valley has been formed chiefly by the present stream, and is a shallow and narrow trench. At Huntington the river enters the old outlet of Lake Maumee, a glacial lake that occupied part of the basin of Lake Erie. This outlet has a valley several times as large as that occupied by the Wabash above this point. It opened a new or postglacial line of drainage in its westward course across Indiana, except for a few miles in the vicinity of Lafayette, where it crosses or follows a preglacial valley for a few miles. It has been compelled to do considerable excava- tion in rock from Huntington down as far as Covington, and still carries rapids at several points. Below Covington the stream follows very nearly the line of a partially filled preglacial valley, and its work has been largely the removal of a portion of the glacial deposits left in that valley. It makes, however, some deflections into the edge of the uplands, cutting off points of the bluffs. At such places the channel is occasionally in process of excavating rock. The cause for these deflections is not in all cases clear, but it is probable that in the majority of cases the filling was such that the stream was free to pass across these points and thus take a more direct course than that of the old line around them. In some cases it is possible that the ice sheet may have had an influence in guiding the stream across projecting points beneath it or on its border. The length of the valley occupied by the Wabash is about 450 miles; but the length of the stream is much greater, for the river in its lower course makes several oxbow curves within the valley. The source of the river is about 1,000 feet above tide, while its mouth at low water is but 311 feet. The average fall, if we estimate the stream to have a length of 500 miles, is therefore about 164 inches per mile. The rate of descent is far from uniform, being much more rapid in the upper portion than in the 188 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. lower. There are also many rapids, separated by pools or sluggish portions of the stream. The elevation of the stream has been determined at many points, but in the absence of a careful measurement of its length the rate of fall is only approximately known. The portion of the river above the point where it enters the.old lake outlet, estimated to have a length of 100 miles, has a fall of about 300 feet, or 3 feet per mile. Railway levels and canal surveys at the point where the river joins the old lake outlet show its elevation to be very nearly 700 feet above tide, the altitudes reported varying between 696 and 699 feet. The canal survey below Huntington shows a fall of 32 feet to the mouth of the Salamonie, a distance of about 15 miles, and a fall of 34 feet between the mouth of the Salamonie and the mouth of the Mississinawa, a distance of perhaps 20 miles. In the next 20 miles, to Logansport, there is a fall of 50 feet. From Logansport to Lafayette, a distance of about 50 miles, there is a fall of 77 feet. From Lafayette to Attica, a distance of 25 miles, the fall is but 19 feet, and from Attica to Covington, a distance of 20 miles, but 17 feet. From Covington to Terre Haute, a distance of about 55 miles, there is a fall of only 22 feet, this being the lowest gradient for so long a section found on the river. From Terre Haute to the mouth of White River an accurate survey by the United States Army engineers shows a fall of 71.18 feet in a distance of 122.55 miles, or about 8 inches per mile. In this distance there are 13 rifles, each but a fraction of a mile in length, which have a combined fall of 17.86 feet. These reduce the fall of the 120 miles not embraced in the riffles to 53.32 feet, or 5.38 inches per mile. The greatest fall at a riffle in this section of the Wabash is at Grand Rapids, just above the mouth of White River, where it amounts to 4.5 feet.' The fall from the mouth of the White is 65 feet in a distance of perhaps 90 miles by the windings of the stream. 1 Thirteenth Ann. Rept. Geol. Surv. Indiana, 1883, pp. 69, 70. WABASH DRAINAGE SYSTEM. 189 The following table includes the data upon which the above statements are made: Table of altitudes and distances along Wabash River. Lean re ea ae Miles. Feet. Inches. SOURCE Me ears ea eeveeie aes interes eleialain Jo amis ae Sadia wiswwicececians 0.0 1, 000. 0 0. 00 Delano tii oto mse saree ere ete siete ein aiajaeaiaisayain'eisie Siete case e'Scle ects 100. 0 699. 0 36. 00 IMouthyohs Salamontertivienssas sree rass sae scenes aseee cece cece 15. 0 667. 0 25.56 Mouthlon Mississinawar River s-2esessses-coscescaee ee a seeecee 20.0 633. 0 20. 40 ILO GEMS\POIN) -2 cosoec se ses sc esse osasas sascsacoecnesecoseesoss 20.0 583. 0 30. 00 ILEANA CWS. - sos caso e noose sss aoco sas osaesSoosDorocoeSsecanSes 50. 0 506. 0 18. 48 JING) oc 5 Abo Bod GOS onrs Spot Soca Oe HOS OOO c RHE SESE aT SSB aaes 25.0 487.0 9, 12 (COyMNAO ssSekc-cbdacons saucourasbe Soom sees SOP BEDE ReBE oe 20. 0 470.0 10. 20 Thane TENG. Ge SSescosboe skeen ce LASS ORE Scone Ra Sheer sees 50. 0 447.7 4. 80 Stateline eacer omer ase se ce Sees ccicetisecm ee cae Monegan ta sce 14.6 440.6 5. 80 Efutsonvyallles Mec eee Soeae on es owe eee Cafes ook Ue 29.0 424.6 6. 60 Vai COMM CSP ere er ney esp iale eins apap cre ate epee yot ae eevee ayaa ae 46.4 398. 8 6. 60 AVlO Utz o DAV WnN COWEN. erie epee atersterians bene sre ere wee eee ey fen a 32.5 876.5 8.30 GreyAywllle, UM sees osteo scekodeass saepcee See ose eSeR eC oes se 28.0 365. 0 5. 00 MiGudiln Gi Ibe Wes jo 5 coeebosasceoaseoasbeeSeneeeoEaeeee 46. 0 323.0 11. 00 Mouthkotiniv cree ese serteceiss ote eins wicte ataicie sie eae sisaioe 16.0 311.0 9. 00 SALAMONIE RIVER. Salamonie River enters the Wabash from the southeast a few miles above the city of Wabash. It has a length of about 75 miles. Its source is on the northern slope of the elevated limestone district of eastern Indiana, at an altitude of about 1,000 feet above tide. Throughout the greater part of its course the river follows a plain on the south border of the Salamonie moraine. Its descent is measured by the descent of the plain, except in the lower 40 miles, where it has deepened its channel to enter the old lake outlet. Sufficient time has not elapsed since the river began flowing for it to form a regular gradient. It can scarcely be said to have developed a valley except in the lower 40 miles, the bed of the stream in its upper course being seldom more than 26 to 25 feet below the bordering plain. The descent from Portland to Montpelier is less than 3 feet per mile, but in the 40 miles from Montpelier to the mouth the average descent is about 4 feet per mile. 190 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. MISSISSINAWA RIVER. Mississinawa River, a southeastern tributary entering the Wabash near Peru, has a length of about 100 miles. Its source is in western Ohio, 10 or 12 miles beyond the State line, on the north slope of the elevated limestone district which occupies eastern Indiana and western Ohio. At its source the altitude is probably 1,100 feet above tide. In the 25 miles from its source to Ridgeville, Ind., the stream has a fall of about 5.5 feet per mile, descending with the plain which it follows on the south border of the Mississinawa moraine, and cutting but 15 to 30 feet into the plain. From Ridgeville to Marion, a distance of 50 miles, the rate of fall is but little more than 3 feet per mile. The stream in this distance has deepened its channel slightly, but at Marion is scarcely 50 feet below the bordering plain. Most of the work accomplished by the stream is in the section between Marion and the mouth, a distance of only 30 miles. Its fall in this section is about 5.5 feet per mile, or fully as great as in the headwaters. The depth of the channel increases from about 50 feet at Marion to fully 100 feet in the vicinity of its mouth. It is excavated mainly in drift, but at some points has extended a few feet into the underlying rock strata. EEL RIVER. Eel River, a northeastern tributary of the Wabash, entering at Logans- port, has a length of about 85 miles. Its source is on the inner border of the great Erie-Saginaw interlobate moraine, a few miles north of Fort Wayne, at an elevation of about 850 feet above tide. The average fall of the stream is very nearly 3 feet per mile, the elevation of the mouth being 543 feet. The following table of distances and elevations is based upon Williams’s list of altitudes, given in the Tenth report of the Indiana geological survey: Altitudes along Hel River. Ogee. Pout asta | Race sey Miles. Feet. Sourceyabowblpeseae aes ae ae ae ee ee omen sec ccmtice seo hens decee ae ose oe oseee 85 850 Columbian Ciivzae eterna eee met aaa ee es ceae So 28 55 eee eee eae 70 816 Golam aires St /Sae yes eetee rare ne atsit Saye ae aes la Festa s aiuto sae Se ise aoe ae Spas 08 } 768 Ibiberty< Mills Ses se scc ster eas cece see ete e oct bo Sas eae ao ana Eee ee 50 750 INontheManchestenter= = ec aseee ae nen Sa seaes os cleo eee Ba eden t 45 721 HelgRiverwallroadubnridse ime Viiamis Countyesssssee- 2 22 ee- eee sae eaaeee 30 688 Wout atpbopansponieeer ese seer reac ee seer ee a eee eee ee 0 583 WABASH DRAINAGE SYSTEM. 1S) The headwater portion of this stream, like that of the Mississinawa and Salamonie, has a poorly developed channel and a sluggish current. It is only in the lower 25 or 30 miles that erosion of any consequence has occurred. Hven here the valley scarcely exceeds 50 feet in depth. TIPPECANOE RIVER. Tippecanoe River is the main northern tributary of the Wabash within the State of Indiana. It has a length of about 125 miles, and drains a belt averaging perhaps 20 miles in width. Its source is in the midst of the great interlobate moraine of northeastern Indiana, at an elevation of nearly 1,000 feet above tide. It descends the northwest face of the moraine from southwestern Noble County into Kosciusko County, reaching a level 800 feet above tide north of Warsaw. It follows the north border of the moraine a few miles southwestward, to the point where the Saginaw and Erie moraines become differentiated. It then passes through a gap in the Saginaw moraine and enters a sandy plain formerly occupied by the waters of ‘‘old Lake Kankakee.” After traversing this plain for about 60 miles, it leaves the old lake area near Monticello and passes through an Hrie moraine which follows the northwest border of the Wabash River, and enters the Wabash from a narrow plain on the inner slope of this moraine. Although bordered in places by elevated knolls and ridges in the upper portion of its course, it has no well-defined valley, nor has it exca- vated a valley of much depth in the old lake bottom. The main excavation ‘occurs in the lower 30 miles of its course, and even here its channel is nar- row and scarcely reaches 100 feet in depth. In this lower portion the rate of fall is about 3 feet per mile. The fall is less in the section traversing the old lake bottom, being about 150 feet between Rochester and Monti- cello, a distance of 60 miles. The great fall of the upper portion is chiefly made in short sections, connecting marshes whose levels become successively lower in passing down the slope of the moraine. WEST WHITE RIVER. The chief tributary of the Wabash is West White River, which enters it from the east at a point about 90 miles from the mouth. If we include with the West White its entire system of drainage, it will embrace about one-third of the State of Indiana, or an area about as great as that drained by the Wabash and its other tributaries within that State. The West 192 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. White proper, however, drains only about one-sixth of the State, the drain- age basin of the Kast White, its principal tributary, bemg nearly as great as that of the main river. The source of the West White is in Randolph County, near the east line of the State. The course of the stream is westward to Hamilton County, a distance of nearly 75 miles, where it turns abruptly southward and leads in a course somewhat west of south to the Wabash River. The length of the valley of this stream is about 275 miles, but this does not represent the length of the stream, for in its lower part it winds greatly within its valley, adding perhaps another hundred miles to its length. The estimates given below are, however, based upon the length of the valley rather than that-of the stream. They indicate the condition when the river is out of bank, as is occasionally the case in high-water Stages. At its source the stream has an elevation of not less than 1,175 feet, while at its mouth the elevation is but 375 feet above tide. It has, there- fore, an average fall of nearly 3 feet per mile, or more than double the average fall of the Wabash River. In its upper 15 miles the fall is estimated to be about 8 feet per mile; in the next 25 miles, about 6 feet per mile, and in the succeeding 20 miles, about 5 feet per mile, making a fall of 375 feet m a distance of 60 miles, or to a point near the city of Anderson. Below Anderson the fall for the 50 miles to Indianapolis is nearly 24 feet per mile. Below Indianapolis for about 30 miles the fall exceeds 3 feet per mile. In the remaining 130 miles of its course there is a fall of but 185 feet, or slightly less than 14 feet per mile. Aside from its main tributary, East White River, there are but two tributaries of White River which exceed 50 miles in length, namely, Fall Creek, an eastern tributary entering just above Indianapolis, and Eel River, a western tributary entering at Worthington, in northern Greene County.) Fall Creek has an elevation at its source of at least 1,000 feet and at its mouth of about 700 feet. Fully half of the 300 feet of descent is made in the upper 20 miles, leaving a fall of 150 feet for the lower 40 miles. It derives its name from a cascade about 10 feet in height in the sandstone at Pendleton. Kel River has a length of nearly 100 miles. Its east fork, ‘This river should be distinguished froma stream of the same name entering the Wabash at Logansport. WABASH DRAINAGE SYSTEM. 193 known as Mill Creek, is about 40 miles in length, and its west fork, known as Walnut Creek, fully 50 miles. Below the junction of these forks the stream has a length of about 45 miles, if the minor windings of the channel are disregarded. EAST WHITE RIVER. This large tributary enters the West or main White River about 40 miles above its mouth. It drains the district immediately east of that drained by the main river and has an area nearly as great, there being about one-sixth of the State of Indiana tributary to it. The headwater portion above Columbus, Ind., is usually known by the name of Blue River, the pame East White being applied to the stream below its junction with Flat Rock Creek at that city. The name Driftwood is also applied to the lower portion of the river. Inasmuch as there is another stream within the State called Blue River, it is unfortunate that this name is applied to the headwater portion of Kast White River. The upper half of the drainage basin of Kast White River lies within the glaciated districts of eastern and southeastern Indiana. The streams find their sources in the elevated Upper Silurian limestone belt, in the eastern part of the State, and descend rapidly westward to the Devonian shale area. The main stream leads through the western part of the drainage basin, and hence receives nearly all its tributaries from the east. The drainage system is, therefore, very unsymmetrical. Although these headwater tributaries make a great descent in passing down to the basin of Devonian shale, they have carved very insignificant channels. The valleys are usually so shallow that their bridges may be seen for miles back from the borders of the streams. A portion of the Museatatuck drainage system is, however, characterized by deeper channels, a feature which is probably attributable to the greater age of that system. It lies outside the limits of the newer, or Wisconsin, drift, while the principal tributaries of the East White farther north flow throughout most of their course within the limits. of the newer drift sheet. The northern tributaries, Blue River and Flat Rock Creek, have their sources in northeastern Henry County at an elevation of about 1,100 feet above tide. They make a descent of about 500 feet in the 100 miles from their source to the junction at Columbus, or an average fall of about 5 feet perimile. In the lower 35 miles of its course, from Shelbyville to Columbus, 13 MON XLI 194 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Blue River has a fall of about 44 feet per mile, nearly as great as the fall of the headwater portion above Shelbyville. From Columbus to the mouth of the Muscatatuck, a distance of 55 miles, the average fall is very nearly 20 inches per mile. In the remaining 125 miles, where the stream is flowing in a preglacial valley, the fall is about 10 inches per mile. In this portion there are, however, occasional riffles and rapids im which a descent of several feet is made within a mile. The most conspicuous of these rapids is at Hindostan, where a fall of about 5 feet occurs. At this point the stream has cut off an old oxbow and is excavating the rock in the ridge encircled by the oxbow. The Muscatatuck River in its lower 25 miles has very little fall com- pared with the neighboring portion of East White River. At the railway crossing south of Seymour the bed of the Muscatatuck is 40 feet lower than at the crossing on the East White immediately north of Seymour. The difference in gradient is due to a filling of the East White Valley by deposits of gravel at the Wisconsin ice invasion. As the Muscatatuck drainage system lies outside the limits of this later ice invasion or the reach of its waters, its valley remains unfilled. The fall on the lower 25 miles of the Muscatatuck is apparently not more than 10 feet, while on East White River, in the 25 miles above the mouth of the Muscatatuck, there is a fall of about 50 feet. The portion of the East White River Valley lying within the ungla- ciated districts of southern Indiana is cut to a comparatively low gradient, notwithstanding the hardness of the rock formations through which its course is channeled. The valley at present is silted up to a height of per- haps 100 feet above the rock floor. The bluffs rise 200 to 300 feet or more above the present valley bottom, thus giving the preglacial valley a depth of 300 to 400 feet. If we consider this great depth and the hardness of the formation, the width of the valley, which is seldom less than one- third mile and probably averages more than one-half mile, is not surpris- ingly small. ‘The valley of this stream, like that of the Ohio in the corresponding section, presents a series of oxbow curves, with very little straight channeling. Within this unglaciated portion the East White receives one important northern tributary, Salt Creek. This stream has a length of about 60 miles from its headwaters, in Brown County, to its mouth, near Bedford, in Law- WABASH DRAINAGE SYSTEM. 195 rence County. It drains the greater part of the elevated district in Brown, Jackson, Monroe, and Lawrence counties. In its headwater portions, in Brown County, the valleys are cut to a depth of 300 and in places 500 feet below the level of the neighboring hills, and a dendritic system of draimage has been developed, which is strikingly in contrast with the irregular and unsymmetrical drainage systems of the streams within the drift-covered regions to the north and east. At its headwaters the valleys have been filled to a marked degree by deposits of sand and gravel made by streams issuing from the edge of the ice, which for a time overhung the northern portion of Brown County. The valley is apparently filled to nearly as great an extent as the portion of the East White with which it connects. Its rate of fall is more rapid than that of the East White, but is less rapid than that of some of the large streams of the glaciated district. The fall of the North Fork from Nashville, a few miles from its source, to the mouth of the stream is only about 150 feet, or scarcely more than 3 feet per mile. Lost River, a tributary entermg East White River from the east in southern Martin County, has a length of about 50 miles. This stream receives its name from the fact that it flows for a few miles in a subterra- nean passage in the St. Louis limestone. In times of freshet the stream can not be entirely absorbed by the subterranean channel, and it then flows on the surface in its former bed, which is now covered with a heavy forest. PATOKA RIVER. Patoka River, a distinct tributary of the Wabash, drains a narrow belt along the south border of the drainage basin of East White River. The stream has a length of over 100 miles, but its drainage basin nowhere exceeds 20 miles in width. Its source is in the hills of the Chester or Kas- kaskia sandstone, in southern Orange County, at an altitude of about 800 feet. Its mouth is just below that of White River, at an elevation of 375 feet above tide. This drainage system is made up of three small drainage systems, which were formerly distinct and discharged northwestward into the White and East White rivers. The upper system embraced the por- tion above Jasper, Ind., the old divide being at the northeast border of that village. The middle system embraced the portion between Jasper and Velpen, Ind., and the lower the part from Velpen down to the vicinity of Princeton. The old drainageway there turned north to White River, near 196 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Hazelton, but the present stream continues westward across a rock point into the Wabash Valley. A map showing the changes which this drainage system has experienced, and also changes in smaller tributaries of the Wabash in southwestern Indiana, appears in the monograph on the Illinois Glacial Lobe.! The changes are there discussed in considerable detail. WESTERN TRIBUTARIES OF THE WABASH IN ILLINOIS. The western tributaries of the Wabash are all comparatively small. Those whose courses lie within the limits of the Wisconsin drift are not goy- erned by the preglacial drainage, for the dritt has filled the region to a higher level than the old divides. But south from the border of the Wis- cousin drift the courses of streams are governed to a large extent by the preglacial drainage lines. The few changes or departures from the old drainage are discussed in Monograph XXXVIII, as are also the influence of morainic ridges of Wisconsin age upon the course of the streams. — CAUSES FOR CHANGES IN DRAINAGE. Of the several factors which are influential in causing changes of drainage, glaciation is known to have been widely operative in this region. Piracy seems to have been operative, at least to a limited extent, and possibly has had wide influence. In addition to these the influence of uplift or earth movements should perhaps be considered. GLACIATION. With the extension of the earliest glaciation into the lower courses of a northward-flowing stream there would have been a ponding of water in front of the ice field. This ponding would eventually reach a height at which discharge could take place over the rim of the drainage basin, and a new system of drainage would be inaugurated. With the advance of the ice field many streams would be thus affected, and in some cases the influence of the ponding might be felt at points many miles beyond the limits of the ice field. In the region under consideration streams which had been flow- ing from the Appalachian region northward into the basins now occupied by Lakes Erie and Ontario are likely to have experienced ponding in their lower courses before the ice field had encroached greatly on the basins of 1Mon. U. 8. Geol. Survey Vol. XX XVIII, Pl. VIII. CAUSES OF CHANGES IN DRAINAGE. 197 these lakes. This would perhaps at first result in lakes that drained south- westward through the Maumee Basin to the Wabash. But with the advance of the ice field the lake basins would become filled, and ponding would extend southward toward the present Ohio. New lines of discharge would then be opened. This process of shifting to new lines might continue in parts of the region down to the culmination of the glaciation, but in other parts the final shifting may have taken place lone before the ice field reached its extreme limits. A stream which suffered a late diversion should accomplish correspondingly less work than one that suffered an older diver- sion, so that by the amount of work the relative dates of diversion may be estimated. The effect of glaciation in diverting streams would in some cases be restricted to the time when the ice field was present, there being a return to earlier courses upon the withdrawal of the ice. But in other cases the first ice invasion produced a permanent diversion of drainage. In each succeeding stage of glaciation the streams would be subject to disturbances similar to those produced by the earliest glaciation. This field is liable, therefore, to contain examples of diversion of various dates, from the first obstruction of the northward drainage by the encroachment of the ice field on the basins of the lower Great Lakes down to the close of the last glacial stage and the final disappearance of the ice from these basins. Instances of diversion and of control by glaciation or glacial features, illustrating the wide differences in date, will appear in the course of the discussion of the glacial features. Turning to the Ohio, it will be found that the old Upper Ohio or Monongahela system was diverted to the present course at a date at least as early as the culmination of the earliest glaciation in the Upper Ohio region, a glaciation that was probably Kansan if not pre-Kansan. While a part of the change Gn the portion between New Martinsville and Mounds- ville, W. Va.) appears to have been produced through piracy at an earlier date than the first glaciation, there seem to be no grounds for inferring that the great diversion of the old Monongahela from the northward to the southwestward line of discharge took place through piracy. On the con- trary, the slope of the old gradation plain toward the Lake Erie Basin is so great that it seems scarcely possible for it to have been disturbed through _ piacy by the southwest system of drainage. It may be suggested that a 198 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. difference in the relative elevation of the Lake Erie Basin and the Ohio Basin has been produced, by which the slopes toward the Erie Basin have been greatly increased; but of this there is no specific evidence so far as the writer is aware. The available evidence seems to support the view that this diversion of the old Monongahela system to the Middle Ohio system took place as a result of the first glaciation, though it may have been brought about some time before the ice sheet had reached its farthest limits. This diversion seems to have been a permanent one; at least no evidence of a return to the Erie Basin after the earliest glaciation has been noted. This earliest glaciation appears also to have thrown the several pre- glacial components of the Allegheny into their present course, and so far as evidence is forthcoming the diversions were permanent ones. The diversion of the Middle Ohio or old Kanawha system into the Lower Ohio can not be referred so confidently to glaciation as the diver- sions just mentioned, nor is the available evidence such that any other factors can be cited to have caused the diversion. Further attention is given this matter under the subjects of “Piracy” and ‘‘Earth movements.” The diversions near Cincinnati are probably in large part due to gla- ciation. It is, however, possible that the diversion past the south side of the Walnut Hills resulted from stream piracy prior to the earliest glaciation of the region. Whether the diversion from the old channel past Hamilton to the present direct channel from Cincinnati to the mouth of the Ohio took place as late as the Ilinoian stage of glaciation or at an earlier stage has not been determined. The changes along the old Kanawha system by which Teays Valley and the valley south of Ashland, Ky., became abandoned are perhaps indirectly due to glaciation. The ponding of waters probably extended into these valleys at each glacial stage down to the lowan. The amount of erosion accomplished after the diversions took place is, however, so great that the diversions seem likely to have occurred as early as the earliest stage of glaciation. ; PIRACY. Where one drainage system has an advantage over an adjoining one, shiftings of the divides and even important changes in drainage courses may result. It is probable that such shiftings and changes have been common in early stages of development of drainage systems. They appear also to have taken place to some extent in drainage systems that are somewhat CAUSES OF CHANGES IN DRAINAGE. 199 mature. In the discussion of features on the portion of the Ohio between Moundsville and New Martinsville attention was called to evidence that the divide had shifted toward Moundsville because of an advantage held by a drainage line that led southwestward from New Martinsville over one that led northward. It is probable also that the channel which connects Big Bone and Eagle creeks with the Ohio near Warsaw, Ky., became abandoned through piracy, though the precise mode of capture is not yet understood. The changes in drainage just mentioned are of minor consequence compared with changes which were effected by glaciation; but there is a chance that piracy will prove to have been influential in causing changes of great consequence in this region. The diversion of the Middle Ohio or old Kanawha system into the Lower Ohio system seems so remote an event, if we may judge by the work accomplished since it took its present course, that one hesitates to refer it even to the earliest of the several stages of glaciation. But the difficulties of accomplishing this diversion by piracy are perhaps not less than in extending the glaciation far enough back to give time for the work to be done. In discussing this matter, Chamberlin writes: “It would seem to be a rather extraordinary feat of piracy that a river should be able to eat its course back across the Cincinnati arch and drain country in a synclinal beyond, when there were courses of drainage which essentially avoided the arch.” The applicability of piracy to this and also to other places in the Ohio drainage system can hardly be decided in the present stage of investigation. EARTH MOVEMENTS. Earth movement or crust warping may prove to have had influence in causing diversions in the old systems of drainage either by itself or in com- bination with stream piracy. As already suggested, it may have been through these agencies that the old Kanawha was diverted from the Scioto Basin to the Lower Ohio prior to the earliest glaciation. But it is perhaps idle to speculate on this question, since the date of the flexure at the north end of the Scioto Basin is unknown and various other conditions are uncer- tain. Not only here, but elsewhere in the region under discussion, the influence of earth movements upon drainage embraces a broad range of problems which can scarcely be dealt with at present. The possible varia- tions in influence are forcibly illustrated in districts adjoining the one under discussion, and with these illustrations the writer will leave this question. 200 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Recent investigations ‘by Gilbert, Spencer, Taylor, and others have brought to light evidence that earth movements have produced marked changes in the drainage of the Great Lakes and their expanded prede- cessors. Because of northward differential uplift the drainage of the three upper lakes (Superior, Michigan, and Huron) has been thrown into a course farther south than it formerly took, the old course being eastward from Georgian Bay to the Ottawa River instead of past Niagara Falls. The limits of change may not yet have been reached, for the movement appears to still be in progress, and if it continues to the amount of only a few feet the discharge of the upper lakes will be diverted from Niagara to Chicago, and they will then be connected with the Mississippi mstead of the St. Lawrence system. Changes of this class and magnitude illustrate the great influence which earth movements may have upon drainage under favorable, conditions. On the other hand, very great earth movements have taken place in some localities which apparently have had but little influence upon the drainage. The Susquehanna River crosses the entire Appalachian sys- tem, and yet seems to have maintained its course faithfully, notwithstanding it was antagonized by the maximum flexure of the mountain system. The Delaware, the Juniata, the Potomac, and even the upper waters of the Kanawha furnish illustrations of similar persistence. From these illustrations it appears that the rate of movement must be sufficiently slow for a stream to cut down its passage across the rising arch if there is to be no diversion. It may also be inferred that a stream flowing at a low gradient might be diverted, as well as a lake, by such a movement as that which has produced the changes in the drainage of the Great Lakes. Indeed, the South Fork of Chicago River will be changed to a lake and finally made to reverse its present course if the change in the discharge of the Great Lakes from Niagara to Chicago is effected. SECTION II. ST. LAWRENCE SYSTEM. In the present discussion only that portion of the St. Lawrence system is considered that les within the territory covered by this report. It includes the southern tributaries of Lake Ontario from the Genesee west- ward to the Niagara River, Tonawanda Creek, an eastern tributary of Niagara River, and the southern and western tributaries of Lake Erie in New York, Pennsylvania, and Ohio. ‘The discussion begins with the Genesee River and proceeds westward to the western end of the Lake Erie Basin. ST. LAWRENCE SYSTEM. 201 GENESEE DRAINAGE BASIN. GENESEE RIVER. Genesee River, which forms the east boundary of the region under dis- cussion, rises in the Allegheny Mountains in northern Pennsyl- vania and flows northward across western New York, entering Lake Ontario a few miles north of the city of Rochester. The accom- panying map (fig. 8), prepared by Fairchild, shows the leading fea- tures. The drainage basin is about 100 miles long and perhaps 40 miles wide. It is broadest in the northern half, the southern end for a distance of about 35 miles from the head of the basin being but 10 to 20 miles wide. The area of the drainage basin is estimated by Raf- ter to be 2,445 square miles.’ The upland surface at the head of this drainage system attains an altitude of about 2,500 feet, but there are passes connecting the headwaters of the Genesee with the headwaters of the Allegheny and with branches of the Susquehanna that are 250 to 400 feet lower than the high uplands. One of these near Bingham, Pa., is 2,174 feet; another near Ulysses is 2,252 feet; and one near Gold is 2,228 feet (Fairchild). There is a still lower pass (2,068 feet) connecting the 5, EAS BETHANY PeETHAN: DALE e Ni ; Promina. Of 2 ca 365 op GENESEO /o 600 JOMNSOND 17 9 3 elie \ 7? Se, y) WR ¢ tS) “s An a gscoTrssuns SPRINGWATER 2 Q PANSVILLE \2 689 0 "OARRPORT 0 CANEADEA "93 1238 G)BELFASY QHORNELLSVILLE 1313, “5S G4 o Fig. 8.—Hydrography of the Genesee Valley, by H. L. Fairchild. This map is reproduced from Fairchild’s paper in the Bulletin of the Geological Society of America, Vol. VII, 1895, Pl. XIX. Water partings are shown by heavy broken lines. Glacial lake outlets are indicated by bars transverse to the water parting. Figures indicate altitude aboye mean tide. West Branch of Genesee River with the head of Oswayo Creek, a tributary 1Water- eaten Babee U. S. Geol. sive ey No. 24, 1899, p. 26. 202 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. of the Allegheny River. There are other passes at the heads of tributaries which are markedly lower than the passes at the head of the drainage basin. The lowest connecting with the Allegheny drainage is near Cuba, New York, 1,496 feet above tide; but one near the New York and Pennsylvania State line, connecting with Honeoye Creek, a tributary of Oswayo Creek, is only 1,600 feet. The lowest pass connecting with the Susquehanna is at Burns, N. Y., 1,210 feet. In the southern half of the basin the tributaries are all small. The longest eastern one is Angelica Creek, with a length of 25 miles, and the longest western one is East Coy Creek, with a length of 25 to 30 miles. In the northern half there are four tributaries whose length is about 50 miles— Canaseraga and Honeoye creeks from the east and Oatka or Allens and Black Creek from the west." The Genesee River follows, in the main, the line of a preglacial valley; but, as pointed out by Hall many years ago, it makes slight incursions into the west bluff of the old valley at places where the preglacial valley was greatly filled with drift. It was also thought by Hall that the mouth of the preglacial: valley was at Irondequoit Bay.’ The principal deflections of the stream are between Portage and Mount Morris and in the vicinity of Rochester. The following concise description of the deflection at Portage was presented by Hall at the meeting of the Association of American Geologists and Naturalists in 1843, and reported in the American Journal of Science for that year. A similar description appears in his report of the Fourth District, also published in 1843: The river to the south of Portage flows in the bottom of a broad valley extending toward the north. At Portageville the stream bends around to the left, and, after flowing a short distance nearly south, turns to the north and northeast, cutting its channel through the rocky slate in some places to the depth of 350 feet, and forming in its passage three falls of 66, 100, and 96 feet, respectively. This channel is narrow, with mural banks; but a short distance below the lower falls it emerges into a broader valley in a line with the channel to the south of Portage before it is deflected from its course. The space between these two points is a deep, broad gorge, filled to a great height with clay, sand, and gravel. This is evidently the ancient channel of the river, and yet, after it had become filled with this drift, the stream found an easier passage by excavating the solid rock for 3 miles than by removing these loose materials. Still below this point the river leaves the broad channel and excavates a gorge through the shales, emerging into the broad valley at Mount Morris. 1Tt should be noted that the Genesee River has two western tributaries called Black Creek. The name Honeoye is also applied to two streams here discussed. * Geology Fourth Dist. of New York, by James Hall, 1848, pp. 344, 422. SEE U. S, GEOLOGICAL SURVEY MONOGRAPH XLI PL. IX este DRE gai ie sala Vea mays o Ae GENESEE DRAINAGE BASIN. 208 It has been pointed out by Fairchild that the valley followed by the Genesee between Portage Falls and the deflection at Mount Morris is the prelacial valley of some tributary of the old river.’ The preglacial course from Portage was apparently eastward, past Nunda, into the valley now occupied by Kishawa Creek, and thence north to the present Genesee just below Mount Morris. Grabau has suggested a westward course, past Castile, to the valley of Oatka Creek near Warsaw, and thence northward down that valley to the lowlands near Leroy, beyond which its course is not given.” In suggesting this course he apparently overlooked the broader and more direct line past Nunda. It is also a mere conjecture that a buried valley connects the Genesee past Castile with Oatka Valley. The present divide, it is true, carries a larger deposit of drift there than at points farther north and south, but it seems likely to be the site of one of the low passes or cols that characterize this region. At Rochester the Genesee enters another gorge, which extends to Lake Ontario, a distance of 7 miles. In this gorge there are three falls made in passing over the Niagara, the Clinton, and the Medina formations, with heights of 90, 20, and 94 feet, respectively. Concerning these falls, Hall has given the following interpretation: The different rates of recession in waterfalls is shown when the successive rocks are of different degrees of hardness, producing a series of falls. This happens when the highest are more destructible than the lower, and by this means the upper fall outruns the others. The Genesee River at Rochester presents an example of this kind, where the Medina sandstone, the rocks of the Clinton group, and the Niagara group have each produced a distinct fall. This, at one period, was doubtless a single cascade; but the upper shale wearing away faster than the rocks below, allowed the fall to travel rapidly southward till it came to the limestone surmounting the shale, where its progress was somewhat arrested. At the present time it seems probable that the lower fall is receding faster than the upper, which is thus protected. The upper fall is now upon the northern edge of the limestone, which increases in thickness for 2 miles south, being a medium of constantly augmenting resistance, while the Medina sandstone and the limestone of the Clinton group are no thicker _and no more difficult to wear away than they have been for centuries past. Thus it is plain that, under otherwise equal circumstances, the lower falls will advance upon the upper until the whole will become one. It will not then, however, be of the 1Bull. Geol. Soc. America, Vol. VII, pp. 427-429. ? The preglacial: channel of Geneseg, River, by A. W. Grabau: Proc. Boston Soc. Nat. Hist., Vol. XX VI, 1894, pp. 359-369. New York Geol. Survey, Fourth District, 1848, pp. 381-382, fig. 184. 204 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. height of all these; for the long rapid between the upper fall and the present place of the lower one ail be nearly as much. descent as the fall at present. These speculations are offered not with a view to any practical bearing, but to correct an erroneous impression which arises from the first view of these falls. Since there are now three falls, and since we suppose there was a period when only one existed, it is natural to infer that the same cause that first produced a separation would continue to operate to perpetuate the same condition. This would doubtless be true so long as the nature of the strata remained the same; but it is equally evident that any change in these will change all the other conditions. In Pls. X and XI views of the falls and gorge near Portage, and of the middle and lower falls near Rochester, are presented. GENESEE GLACIAL LAKES. It was Hall’s opinion that subsequent to the deposition of the drift the portion of the Genesee north from Mount Morris was occupied by a lake. The lake is supposed to have been held by a “barrier on the north,” but the nature of the barrier is not stated Later investigations point strongly to the ice sheet as the barrier. A special study of the evidence that lake waters occupied the Genesee Valley in the Glacial epoch has been made by Fairchild, whose results are given in the Bulletin of the Geological Society of America.” Attention is called to the peculiarly favorable conditions for the formation of glacial lakes during both the advance and the retreat of the ice sheet. The traces of the former have been obliterated, for at its culmination the ice sheet extended southward beyond the limits of the Genesee Basin. The paper is therefore devoted chiefly to a description of the features produced by the waters held in by the ice barrier during the northward retreat and later by barriers of drift that were formed by the ice sheet. Beaches or other shore-line features are necessarily weak, as the expanse of water was not sufficient to give rise to strong waves and as the waters were not long stationary at any particular plane, the height varying with the season and the downcutting of the outlets. Deltas formed by land streams and also glacial stream deltas were well developed. Wave-built and wave-cut terraces also are prominent features. It was found that these deltas and terraces harmonize in level with neighboring outlets on’ the borders of the drainage basin, and that in passing from the southern lNew York Geol. Survey, Fourth District, 1843, p. 344. 2Glacial Genesee lakes, by H. L. Fairchild; Bull. Geol. Soc. America, Vol. VII, 1896, pp. 428-452. U. S. GEOLOGICAL SURVEY MONOGRAPH XLI PL. X MIDDLE AND LOWER FALLS OF GENESEE RIVER AT ROCHESTER, N. Y. mippiss GENESEE DRAINAGE BASIN. 205 toward the northern end of the drainage basin one can recognize several water plains, each of which is in harmony with an outlet. The following summary of these stages is given by Fairchild: The first stage in the glacial drainage of the valley was from the headwaters to both the Susquehanna and the Ohio-Mississippi, with altitudes of water surfaces over 2,200 feet. The second, third, and fourth stages drained to the Ohio-Mississippi, with altitudes respectively 2,068, 1,600, and 1,496 feet. The fifth and sixth stages drained to the Susquehanna, with altitudes of 1,320 and 1,210 feet. The seventh and eighth stages drained to the Illinois-Mississippi, with altitudes from 1,200 down to 880 feet. The ninth stage drained to the Hudson, with an altitude of 435 to 440 feet.1 The tenth stage is the nonglacial St. Lawrence drainage, with present altitude of 247 feet. The several outlets utilized by these lakes show marked differences in the amount of cutting, suggesting great differences in the duration of the lake levels. The first outlet that shows evidence of long operation is the one at 1,600 feet, which discharged westward through Honeoye and Oswayo creeks to the Allegheny River. The amount of downcutting here, as esti- mated by a delta at the mouth of a gully at the east border of the col, is 60 to 70 feet, and the width of the rock gorge 1,000 feet. The excavation is in soft shales. The next lower outlet, 1,496 feet, which leads past Cuba, seems to have encountered no rock, but simply leveled the drift filling at the summit, the channel being spacious and near to grade. In the next stage the waters in the Genesee Valley apparently dropped to about 1,320 feet and discharged through a channel at the head of Canaseraga Creek into Dansville Lake, and thence by a channel past Burns to the Chemung- Susquehanna. But in course of the retreat of the ice sheet a passage was opened to Dansville Lake at a level sufficiently low to cause the Genesee Lake to drop to the level of the outlet past Burns, 1,210 feet. This outlet is reported by Fairchild to be the grandest of the abandoned water courses. Its width is about three-fourths of a mile and its length 12 miles. It has a fall of but 10 feet in the first 6 miles and of but 40 feet in the second. Flood plais are seen all the way from Burns to Hornellsville at a height of 15 to 30 feet over the channel. It is thought that the effective life may have been 1Since writing the above Professor Fairchild has recognized a stage of eastward discharge higher than this, which is marked by the Geneva Beach and which he calls the Lake Dana stage. The Geneva beach: Bull. Geol. Soc. America, Vol. VIII, 1897, pp. 281-284; Lake Dana: Vol. X, pp. 56-57. 206 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. shorter than that of some of the higher outlets, but it carried a much greater volume of water. The next stage marks the close of the Genesee Lake as a local body of water. It then became merged with the great body known as Lake Warren, and discharged westward to the Mississippi. At the Lake Warren and later stages definite beaches were formed, which are considered in Chapter XVI. MORAINAL LAKES. Passing over minor pondings of the river occurring as a result of irregularities in the drift fillmg, only the three most conspicuous cases of damming are considered; one of these is at Portageville, another at Mount Morris, and the third above Rochester. These have all received the attention of Fairchild,’ whose descriptions are here given: At Portageville the broad, deep valley was completely dammed with drift, and the river found its outlet over the east rock wall of the buried valley. After cutting through perhaps 75 feet of drift the river had to cut through about 125 feet of Portage shales before the lake was drained. This probably required a length of time comparable to the life of one of the stages of glacial waters. The top of the rock cut is about 1,250 feet by estimate, and it seems probable that all the. numerous and strong terraces found in the valley from Portage up to Caneadea and below about 1,275 feet altitude belong to the morainal lake. At Portageville there are good terraces at 1,157 and 1,185 feet, and others by aneroid at 1,220, 1,255, and 1,265 feet. At Rossburg are conspicuous plateaus, the lower ones possibly detrital river plains, but higher ones at about 1,200 feet and over. At Fillmore the terraces are 1,218, 1,233, and 1,252 feet, and.at Houghton is a good terrace, estimated at about 1,250 feet. At Caneadea the terraces are well developed and have altitudes of 1,243 and 1,273 feet. The St. Helena morainal lake, which existed in the postglacial part of the Genesee Valley above Mount Morris, has not been studied. The top of the rock gorge, locally known as the ‘‘high banks,” is not far over 900 feet. The cut, about 300 feet deep, is in dark Hamilton shales and was made during the Warren and Iroquois stages. On account of the narrowness of the valley and the steepness of the slopes, the water planes of the morainal lake are not well preserved, but can undoubtedly be found by searching. A shallow morainal lake probably existed southwest of Rochester, due to the morainic dam which the river has cut through at the ‘‘rapids.” This lake could not have been over 560 feet in altitude, the height of the drumloid barrier on the east, and was probably only, 540 to 550 feet, the present altitude of the moraine. It could, therefore, not have been deep, but it extended up the valley several miles, and had a broad expanse east and west, with very irregular form. For the brief episode of its existence this lake received from the river a large amount of detritus, which was deposited as a smooth floor, with an altitude of 525 feet, making the largest level tract in the region of Rochester. 1 Bull. Geol. Soc. America, Vol. VII, pp. 449-450. GENESEE DRAINAGE BASIN. 207 CHANGES OF DRAINAGE ON THE TRIBUTARIES. The changes of drainage in the southern portion of the basin are of minor importance, and consist chiefly of slight incursions of the present streams into the edges of the old valleys. These deflections are due to a higher drift filling in the middle of these valleys than on the borders. In some cases the lower ends of valleys were filled to a greater height than the middle portions, thus forming morainal lakes in the middle portions. In opening a passage to the Genesee these have in some cases cut down into the old valley slope instead of into the deep part, and thus opened rock ravines near the mouth. One of the most impressive of this class is found on the lower course of Caneadea Creek below the village of Rushford, where the morainal dam rises nearly 200 feet higher than the part of the valley above it. In this headwater portion of the Genesee drainage basin the writer has had opportunity to visit only a few of the passes that connect the Genesee with streams discharging westward, and none of those discharging eastward, and can not speak positively concerning shiftings of the divide. The pass at Cuba appears to have its present divide several miles nearer the Genesee than the old divide, there being a marked constriction in the valley of Oil Creek several miles below Cuba which may mark the old divide. The amount of drift is so great as completely to cover the old col if it stands in this constriction. A stream entering Oil Creek from the south at Cuba seems to have formerly discharged northeastward to the Genesee at Belfast. (See Pl. V.) Fairchild has expressed the opinion that the headwater portions of several of the tributaries of the Susquehanna in western New York formerly discharged northward into the Lake Ontario Basin.’ Possibly the headwater portion of Canesteo River discharged from Arkport northward past the low divide at Burns into the Canaseraga Valley and thence to the Genesee. In the northern portion of the Genesee drainage basin the old lines of discharge for tributaries evidently are not followed by the present lines. The latter not infrequently are cutting trenches in the rocks, and in a few cases have waterfalls. The filling with drift has completely concealed the old drainage lines over much of the area drained by Black Creek and the lower courses of Oatka and Honeoye creeks. 1Bull. Geol. Soc. America, Vol. X, 1899, p. 30. 208 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The headwater portion of Oatka Creek is in the midst of morainic knolls and ridges which conceal the preglacial features as far north as the vicinity of Warsaw. Here is entered an old valley, one-half to three-fourths mile in width, which leads northward through elevated uplands into the lower tract lying between the Corniferous and Niagara escarpments. The stream now turns eastward near Leroy and joins the Genesee, but the preglacial channel probably continued northward. The course of the pre- glacial channel is certainly not coincident with that of the present stream even above the deflection near Leroy, for the latter flows on rock ledges and has an important waterfall, known as “Buttermilk Falls,” just north of that village. Because of the great filling of drift north of Leroy, it will be difficult to determine the course of the preglacial line. It is thought by Fairchild that several of the tributaries of the Genesee held small glacial lakes at higher levels than the lakes in the neighboring portions of the Genesee Valley. One in the valley of Knight Creek had an outlet from its head westward past Bolivar. The evidence of a discharge across the col at the head of this valley is clear. The altitude is so great that it can not have been the discharge for the Genesee glacial lake. There is equally clear evidence of the westward discharge of a small gla- cial lake in Van Campens Creek Valley along a line utilized by the Erie Railroad. There is a well-defined scourway across the present divide at an altitude of 1,692 feet, which is nearly 100 feet higher than the westward outlet of the Genesee Lake into Honeoye Creek, a few miles to the south. This valley carries terraces at different levels, which are thought by Fair- child to harmonize in some cases with the local glacial lake outlet and in others with the outlets for the Genesee waters at 1,600 and 1,496 feet The morainal lake in Caneadea Creek Valley was probably preceded by a glacial lake, though the outlet of the latter was not determined. A glacial lake in Oatka Creek Valley is found by Fairchild to have first discharged southeastward, past the sites of Silver Springs and Castile, to the Genesee Lake, the altitude of the head of the channel being about 1,400 feet. With the retreat of the ice barrier this lake eventually found a line of northwest- ward discharge at an altitude about 100 feet lower, through a valley in which the villages of Dale and Linden stand, and thence across a pass to Tonawanda Valley. With the change of outlet the discharge of the lake passed from the Susquehanna drainage to the Mississippi. These lakesare called by Fairchild MINOR TRIBUTARIES OF LAKE ONTARIO. 209 the First Warsaw and the Second Warsaw glacial lakes. At the seventh stage of the glacial Genesee waters the ice barrier became removed suffi- ciently to lower this lake to the level of the Genesee waters and thus bring its distinct history to a close.’ Fairchild has also found evidence of the existence of small glacial lakes in the headwaters of eastern tributaries of the Genesee that discharged to the Susquehanna at higher levels than the outlet past Burns. These and the glacial lakes held in the valleys of the Finger Lakes to the east of the Genesee have furnished him the material for a very interesting chapter of glacial history, but they lie outside the district covered by the present report. The four papers already published by Fairchild in the Bulletin of the Geological Society of America’ describe in detail much that can be only briefly summarized here. MINOR TRIBUTARIES OF LAKE ONTARIO IN WESTERN NEW YORK. Oak Orchard Creek is the most important southern tributary of Lake Ontario between the Genesee and Niagara rivers. Its headwater portion lies on the plain between the Niagara and Corniterous limestone escarp- ments immediately west of the headwaters of Black Creek and drains portions of Genesee and Orleans counties. In southwestern Orleans County it turns northward through the Niagara escarpment, near Medina, where it has a series of falls, and then takes a northeastward course into Lake Ontario. The falls, three in number, a section of which appears in Hall’s report on the Fourth district, occur in the passage over the Medina sandstone and Clinton limestone, as well as at the Lockport (Niagara) limestone. It is doubtful if the stream in any part of its course follows a preglacial drainage line, for the portions in which it is free from rapids and cascades are in plains heavily covered with drift. The headwater portion is exceedingly sluggish and is bordered by swamps, which have required a large amount of artificial drainage. The remaining tributaries of Lake Ontario in western New York head in the Niagara escarpment and flow usually more or less directly across the plain between that escarpment and the lake. Johnsons Creek, however, 'Bull. Geol. Soc. America, Vol. X, 1899, pp. 33-34. * Glacial lakes of western New York, Vol. VI, 1895, pp. 353-374. Glacial Genesee lakes, Vol. VII, 1896, pp. 423-452. Lake Warren shore lines in western New York and the Geneva beach, Vol. VIII, 1897, pp. 269-286. Glacial waters in the Finger lakes region of New York, Vol. X, 1899, pp. 27-68. MON XLI——14 210 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. takes a northeastward course from eastern Niagara County across north- western Orleans County, thus greatly increasing the distance to the lake. Eighteenmile Creek flows for several miles in a southwestward course before turning northward into the lake, its course bemg governed to some extent by the Iroquois beach. TONAWANDA CREEK. Tonawanda Creek consists of two quite distinct portions: First, a north-flowing portion, leading from Wethersfield Township, Wyoming County, northward in a deep valley through elevated uplands to Batavia, near which it enters the lowlands that lie south of Lake Ontario; second, a west-flowing portion, leading from Batavia to the Niagara River at 'Tona- wanda. Between Batavia and Indian Falls the stream flows on the plain back of the Corniferous escarpment. It descends in a cascade at Indian Falls to the plain lying between the Corniferous and Niagara escarpmenits, and flows in that plain to its mouth. This lower portion of Tonawanda Greek, the headwater portion of Oak Orchard Creek, and the entire basin of Black Creek are thus controlled by the geologic structure. They follow the lowest parts of the plains between the two escarpments and traverse a region coated to considerable depth with drift. Whether the lower course of the Tonawanda follows that of a preglacial line is not fully determined, though it seems probable that a preglacial line had approximately the same position as the present stream. The course from near Batavia to Indian Falls is independent of preglacial lines and is determined apparently by the accidents of drift fillmg. The north-flowing portion above Batavia appears to correspond closely with that of a preglacial line, but the latter, instead of turning westward near Batavia, is thought to have continued in a course east of north into the Lake Ontario Basin, traversing a district now drained in large part by Black Creek. The headwater portion of Tonawanda Creek was occupied by a gla- cial lake, which, as found by Fairchild, discharged at first westward to Buffalo Creek, a tributary of Lake Erie, from a point about 2 miles south of Johnsonburg, and at an estimated altitude of 1,410 feet.’ A study of stream deltas leads Fairchild to think that there are two water levels lower than the one that discharged through the outlet, one being at about 1,300 1 Bull. Geol. Soc. America, Vol. X, 1899, p. 33. TRIBUTARIES OF LAKE ERIE. 211 feet and the other still lower. He has not traced out the lines of discharge for these lower water levels, but supposes them to be on the western border of the valley. As indicated above, the lake in this valley received for a time the outflow from the Second Warsaw Lake in the Oatka Valley. TRIBUTARIES OF LAKE ERIE. The present southern and western tributaries of Lake Erie drain about 12,000 square miles in northern Ohio, about 1,000 square miles in north- eastern Indiana, about 600 square miles in northwestern Pennsylvania, and about 1,500 square miles in southwestern New York. This embraces but a small part of the area that was tributary to the Lake Erie Basin in pre- glacial times. As indicated above (pp. 127-148), the present Allezheny system of drainage is made up of independent preglacial lines which entered the Lake Erie Basin by three or more distinct lines of discharge. Indeed, the entire drainage of the present Ohio in western Pennsylvania and eastern Ohio, with adjacent parts of West Virginia, appears to have dis- charged into the Lake Krie Basin. Possibly the old Kanawha, with much of the Muskingum drainage *basin, was formerly tributary to the Lake Erie Basin, though, as already indicated, the evidence is somewhat in question. In the present discussion the several southern tributaries of Lake Erie are taken up in order, beginning at the east and passing westward to the western end of the lake. BUFFALO CREEK. Buffalo Creek, which enters Lake Erie in the southern part of the city of Buffalo, constitutes a line of discharge for several small streams which head in the elevated uplands of southeastern Erie and western Wyoming counties, N. Y. These small streams lead northward through preglacial valleys into the lowlands that lie south of the Corniferous escarpment, but on the lowlands their courses appear to be largely independent of preglacial lines. Borings in the vicinity of Buffalo have brought to light a preglacial channel occupied for a few miles by Buffalo Creek, whose rock bottom is about 80 feet below the surface of Lake Erie." What proportion of the present drainage basin of Buffalo Creek discharged through this preglacial line has not been determined. It is probable, however, that the eastern 1See Pohlman: Proc. Am. Assoc. Ady. Sci., Vol. XXXII, 1883; also Trans. Am. Inst. Min. Eng., Vol. XVII, 1889. 212 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. portion of the drainage basin had a northward discharge to a valley draining the lower course of Tonawanda Creek The deflections of tributaries of Buffalo Creek in passing the Crittenden or Forest beach are notable, as shown in the discussion of that beach on a subsequent page. EIGHTEENMILE CREEK. This tributary of Lake Erie enters the lake about 18 miles southwest of Buffalo, and this fact is probably responsible for the name applied to the creek. It is formed by the union of two streams which have their headwaters in the elevated uplands of southern Erie County and which flow northwestward through deep preglacial valleys into the plain bordering the lake. Their junction is only about 5 miles from the mouth of the stream. It is probable that the preglacial continuation of the East Fork was northward from near Hamburg into Lake Erie, though the precise line of continuation is not known.’ The West Fork probably entered the Lake Krie Basin along a different line from the present course of the creek, for the stream is now excavating a rock gorge near its mouth but little wider than the stream bed. It is possible that the East and West forks had a common line of discharge farther north than the present mouth of the creek. ‘There is, however, a belt of thick drift immediately south of the mouth of the present stream, as shown by wells in the vicinity of Derby, and this may prove to have been the line of discharge for the West Branch. CATTARAUGUS CREEK. Cattaraugus Creek enters Lake Erie at the village of Irving, about 12 miles east of Dunkirk, N.Y. It drains a large area in Cattaraugus County, N. Y., but has only small tributaries from Erie and Chautauqua counties, while its headwaters drain a small portion of Wyoming County and the extreme northwest corner of Allegany County. Its source, like that of Tonawanda Creek, is in Wethersfield Township, Wyoming County, in the midst of a great interlobate morainic belt. It has a general westerly course from source to mouth. The northern tributaries are very small, but the southern tributaries reach, in several cases, a length of 12 to 15 miles, while the length of South Fork is fully 25 miles. The present limits of the drainage basin are largely determined by drift obstructions. In a paper prepared in 1894 by Chamberlin and the writer, evidence was set forth that the lower course of Cattaraugus Creek constituted the TRIBUTARIES OF LAKE ERIE. 213 line of discharge for the preglacial Upper Allegheny.t| The greater part of the present basin of Cattaraugus Creek appears to have been tributary to the old Upper Allegheny from the east and to have joined that valley near the mouth of Clear Creek, opposite Versailles. The old basin of Cattaraugus Creek included the headwater portions of Ischua Creek and probably of Great Valley Creek, now tributary to the Allegheny. The old divide on Ischua Creek appears to have been just south of the village of Ischua, fully 15 miles from the present divide near Machias. The present drainage departs considerably from the preglacial line near the junction of the South Fork with the main stream. The South Fork appears to have formerly taken a course east of north from the village of Cattaraugus, past Waverly, to join the east or main fork about 5 miles above the present point of junction. The united stream then took a northwestward course, passing just south of Collins Center and Lawton to the lower course of Clear Creek. Between the old junction and the present one Cattaraugus Creek is flowing through a rock gorge no wider in places than the bed of the stream. South Fork also enters a similar gorge about 5 miles northwest of Cattaraugus, which continues to the junction with the main creek. A short distance ~ below the present junction with the main creek the oid valley of the Upper Allegheny is entered. The present creek does not traverse the deepest _ portion of that old valley, but follows its west bluff, and for a few miles in the vicinity of Versailles it is cutting a rock gorge in the face of that bluff. The drainage basin of Cattaraugus Creek is limited on the north and east by moraini¢ belts. It is scarcely probable that these tollow a preglacial divide, though the position of the preglacial divide has not been fully deter- mined. Possibly the headwater portion of Cattaraugus Creek discharged northwestward through valleys now tributary to Buffalo Creek. The old drainage basin of which Cattaraugus Creek formed a part is discussed in connection with the Upper Allegheny River (pp. 129-132). SMALL TRIBUTARIES BETWEEN CATTARAUGUS AND CONNEAUT CREEKS. The tributaries of Lake Erie between Cattaraugus and Conneaut creeks find their sources in the prominent escarpment which borders the lake in southwestern New York and northwestern Pennsylvania. Their sources are seldom more than 15 miles distant from the lake, and the longest streams are 1 Am. Jour. Sci., 3d series, Vol. XLVII, 1894. 214 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. scarcely 25 miles in length. The lower courses of these streams appear to be largely independent of pregla+ial lines. ‘The headwater portions often occupy depressions in the escarpment nearly in line with streams which lead southward from the escarpment. The present divide in these low places on the escarpment is in several cases a morainic ridge, and this apparently lies north of the preglacial divide. CONNEAUT CREEK. Conneaut Creek has its’source in a moraine near Conneaut Lake in western Crawford County, Pa. The headwaters lead down into a broad valley which is continuous with the valley that contains Conneaut Lake and Conneaut outlet, which are tributary to the Allegheny River through French Creek. The course of Conneaut Creek is northward for about 20 miles to a point not more than 10 miles from the border of Lake Erie. It there turns abruptly westward and flows between morainic ridges for a distance of perhaps 15 miles to the village of Kingsville, Ohio, where it breaks through the north morainic ridge and takes a northeastward course to Lake Krie. The valley occupied by the north-flowing portion of Conneaut Creek evidently drained a basin which was very different from that of the present ereek and which discharged directly northward into the Lake Erie Basin across the northwestern part of Erie County, Pa. The probable extent of the old basin is discussed in connection with the Middle Allegheny. It was thought by Carll that Conneaut Creek constituted the former line of discharge for much of the present drainage basin of French Creek and the headwater portion of Oil Creek. It is found, however, that French Creek crosses two cols in passing southward from Cambridge to Meadville, which necessitates an interpretation different from that given by Carll. Instead of turning southward from Cambridge the old line of discharge for the head- water portion of Oil Creek and much of French Creek apparently was north- westward across Erie County to the Lake Erie Basin, as indicated in the discussion of FrencheCreek drainage (pp. 138-143). The west-flowing portion of Conneaut Creek, being determined by morainic ridges, shows little, if any, dependence upon preglacial lines. It is mainly in a rock gorge, though in places the drift extends below the level of the stream bed. After passing through the moraine near Kings- ee TRIBUTARIES OF LAKE ERIE. 215 ville, the stream is given an easterly course for a few miles by a beach line which lies on its north side. Upon breaking through this line it passes directly toward the lake. ASHTABULA CREEK. Ashtabula Creek is a small stream which enters Lake Erie near the city of Ashtabula, in northeastern Ohio. Its source is in a morainic belt or elevated uplands near Andover, Ohio, from which it flows northward through a preglacial valley or drift-filled depression to lowlands bordering Lake Erie. It there is deflected westward a few miles by a morainic ridge, but breaks through this ridge near Ashtabula and takes a direct course into Lake Erie. Its lower course is through a narrow valley cut in shale to a depth of 75 to 100 feet, and is evidently independent of pre- glacial drainage lines. The drift-filled depression which it follows in its upper course was probably occupied by a preglacial stream that headed farther south than the present divide, but the precise position of the old divide has not been determined. GRAND RIVER. Grand River is a small stream draining the basin from which it receives its name (see p. 74). Its northerly course is through the former outlet of the old Monongahela drainage system, and, like Conneaut and Ashtabula creeks, it is diverted westward near the border of Lake Erie by a morainic ridge running parallel with the lake shore. This morainic ridge holds the stream in.a westerly course nearly to its mouth at Painesville The preglacial stream which discharged through the Grand River Basin came to the present shore of Lake Erie a few miles west of Ashtabula, near the village of Geneva. Grand River, like Conneaut Creek, encounters rock strata throughout much of its westward course, and there flows in a narrow gorge, strikingly in contrast with the broad, shallow valley of the Grand River Basin. CHAGRIN RIVER. Chagrin River has two headwater forks, each of which finds its source in marshes among the knolls of an interlobate moraine, on the elevated upland east of the Grand River Basin. The two streams unite near Chagrin Falls, above which point the valleys are inconspicuous. At the falls there is a descent of a few feet over sandstone ledges. The stream then soon 216 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. enters a preglacial channel which has been filled to a depth of about 200 feet with drift. This old valley can scarcely have drained a large area, since the larger systems discharging through the Grand River Basin and the Cuyahoga would have absorbed nearly all the drainage except a narrow strip lying between their trunk streams. CUYAHOGA RIVER. The present Cuyahoga River has its head near the source of the Hast Fork of Chagrin River, on the uplands east of the Grand River Basin, only a few miles from the shore of Lake Erie. It leads southwestward for nearly 50 miles, away from the lake, occupying a shallow valley bordered by marshes throughout much of its course, and having an average fall of but 4.5 feet per mile. At the village of Cuyahoga Falls it makes a fall of 220 feet within a distance of 3 miles and enters a preglacial valley, which it follows northward to Lake Erie at Cleveland. In this preglacial valley there is a heavy drift fillmg, both beneath the stream and on the borders of the valley Wells in Cleveland indicate that the valley floor is about 400 feet below the mouth of the present stream, or less than 200 feet above tide. Silt deposits on the borders of the valley indicate that it was filled to a height of fully 200 feet above the present stream, or to within 100 feet of the level of the bordering uplands. From these data it appears that the preglacial valley. was about 700 feet in depth. Its width is scarcely 2 miles at the level of the present stream, and is probably much narrower at the level of the rock floor. Being bordered at the brow of the bluffs by ledges of resistant sandstone, it has preserved a somewhat narrow channel. The preglacial valley oceupied by the Cuyahoga in its lower course may have constituted the line of discharge for much of the region now tributary to Tuscarawas River, as indicated in the discussion of that drain- age system (pp. 165-168). ROCKY RIVER. Rocky River has two forks, which unite near the town of Berea, Ohio. These tributaries are mainly in drift-filled preglacial valleys, but the united stream northward from Berea is largely in a new course. It crosses the preglacial valley from west to east a short distance north of this city, as pointed out by Dr. D. T. Gould,’ who has traced a preglacial valley 1The Berea Advertiser, April 16, 1886. TRIBUTARIES OF LAKE ERIE. DAT from a point a short distance above Berea northward on the east side of that city to Lake Erie, which it enters a short distance west of the present mouth of the stream. Hach of the forks has falls and rapids in passing over the Berea grit, those on the east fork being at the city of Berea and those on the west fork at the village of Olmsted Falls. The present chan- nels of the streams are shallow above these falls and rapids, being but 25 to 40 feet in depth, but upon passing the outcrop of Berea grit the soft Cuyahoga shale is entered and a narrow canyon-like gorge 100 feet or more in average depth is excavated. BLACK RIVER. Two streams with this name unite at the city of Elyria and pass thence northward to the lake at Loraine. The eastern or main fork has its source on the borders of an extensive marsh near Lodi, in which a boring 210 feet in depth failed to reach rock, and flows thence northward mainly through a drift-filled valley, though not strictly coincident with it. This old valley apparently drained the headwaters of Killbuck Creek, as indi- eated in the discussion of that stream. At the city of Elyria occur falls nearly 40 feet in height, and the power which they furnish has recently been utilized. The west fork heads in a moraine near the village of Nova and takes a course east of north, channeling a passage much of the way through rock, its course not being so nearly in harmony with the preglacial drainage line as that of the east fork. The united stream is mainly in a new course from Elyria to its mouth. VERMILION RIVER. This stream heads in the midst of morainic ridges near Greenwich, and flows east of north, mainly through a rock-bound postglacial valley. It drains a somewhat elevated sandstone district. The valley is narrow throughout its course, being usually but 15 to 20 rods wide. It is scarcely 50 feet in average depth, except for a few miles near the mouth, where it is 100 to 150 feet deep. | HURON RIVER. Huron River has its source in extensive marshes between moraines near New Haven. It drains a low district underlain by shale along the western border of the outcrop of Berea grit. Its valley is shallower than that of the Vermilion, seldom reaching 50 feet in depth. 218 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. SANDUSKY RIVER. Sandusky River is a larger and more widely branching stream than any of the tributaries of Lake Erie thus far discussed. It consists of a westerly and a northerly flowing portion. The westerly flowing portion leads from the escarpment of Eocarboniferous sandstone near Crestline westward down the slope to the axis of the Scioto Basin. Instead of turning southward, as the neighboring streams do, to enter the Scioto River, it turns northward and flows down a gradual slope to Lake Erie. It enters Sandusky Bay at the westérn end. The valley of this river is small, being only 20 to 50 feet in depth and one-fourth mile or less in average width. It is m places cut into rock a few feet, and appears to be largely independent of preglacial drainage lines. MAUMEE RIVER. The Maumee River system has the greater portion of its drainage area within the State of Ohio, but small portions are found in Indiana and Michi- gan. The drainage of the two headwater forks of this system was formerly southwestward from Fort Wayne to the Wabash. At that time Lake Maumee occupied the district through which the Maumee flows, the mouth of the old lake being near the point where the St. Marys and St. Joseph rivers had their discharge. As this mouth stood higher than the portion of the basin toward the east and the portion of the outlet toward the west, there was a natural summit formed upon the withdrawal of the lake, from which the waters of the St. Joseph and St. Marys rivers were free to flow either to the east or to the west. By some accident of deposition or of slope the stream found it easier to turn eastward than to maintain its original course westward, and thus the Lake Erie drainage basin embraces these streams as well as those which have been formed in the old lake bottom or were tributary to the old lake. The Maumee River has a length of about 150 miles and a fall of 164 feet, the source being 735 feet and the mouth 573 feet above tide. It has a shallow channel, perhaps 50 feet in average depth, excavated mainly in the drift. It is not itself a navigable stream, but is followed closely by the Wabash and Erie Canal, which for many years afforded a means of water transportation. The St. Marys River has its source in Shelby County, Ohio, at an TRIBUTARIES OF LAKE ERIE. 219 elevation of about 975 feet above tide, or 238 feet above the level of its mouth. The length of the stream being about 100 miles, the average fall is scarcely 24 feet per mile. The portion within the State of Indiana has a fall of but 18 feet in a distance of 35 or 40 miles, or about 6 inches per mile, and is, therefore, very sluggish. The course of the river, in both Ohio and Indiana, is largely determined by a moraine which lies on its north border. The descent of the river corresponds closely to that of the plain in which it flows, and the stream has formed but a shallow channel, seldom more than 25 feet in depth. The St. Joseph-of-the-Maumee has its source in southern Michigan and flows southwestward across the northwestern corner of Ohio, entering Indiana about 35 miles above its mouth. Its length, like that of the St. Marys River, is about 100 miles. It has a more rapid fall, since its source is in a more elevated district, standing about 1,050 feet above tide. The portion in Indiana has a fall of nearly 2 feet per mile. Throughout much of its course the river flows in a narrow plain lying between two morainic ridges, and its descent is determined by that of the plain. Its valley cuts only 25 to 50 feet into the plain and has a very narrow bottom. The principal southern tributary of the Maumee River in Ohio is Auglaize River, which enters it at Defiance. The relation of the course of this stream and of its principal tributaries to the morainic ridges may be seen by reference to Pl. XI. It will be observed that the main stream and also two of its eastern tributaries, Hog Creek and Blanchard River, have their westerly courses along the outer border of morainic ridges, while their northerly courses and the courses of the smaller tributaries are directly away from the St. Marys moraine. It should be noted also that Tiffin River, a northern tributary entering the Maumee at Defiance, follows the outer border of the Blanchard or Defiance moraine, while, its tributaries, like those of the Auglaize, lead away from the St. Marys moraine. The drainage of the district lying between the Defiance moraine and Lake Erie, in northwestern Ohio, is in lines flowing directly away from the moraine. osSrsssS- 5 0so econ seco ceHroacsene 2 At Mr. Cameron’s, 1 mile south of Cynthiana, a well strikes shale at 20 feet. The drift consists of clay, yellow at top and blue near the bottom. The well is near the north border of Brush Creek Valley. Not more than 100 yards south of this well, on the bank of Brush Creek, is a gravel pit. The gravel is quite fine, few pebbles exceeding an inch in diameter. Many eranite and other Archean pebbles occur. At Cynthiana, just south of the outer Wisconsin moraine, a well on Joseph Wilson’s property was bored to a depth of fully 60 feet without encountering rock. It is described to be mainly in a blue clay ‘free from grit.” In Adams County, a short distance west of Lovett post-office, the following exposure was noted on the borders of a ravine crossed by the pike: Road section near Lovett, Ohio. Feet, 1. Silt, of yellow color ......-------------------------------------------+ + 02-222 222250-2--- 2-3 2. Yellow clay containing a few Archean pebbles - --------------------------------- Pha ok aN 45 3. Reddish-brown clay capping the limestone. --.-.-.....------------------------------------ 2-3 This exposure is of especial interest, since it shows the presence of a well-defined drift sheet above the residuary clay. It also is of importance in geographic position, since it lies fully 5 miles outside the line commonly recognized through Wright’s reports as the glacial boundary. In many other places in Adams and southern Highland counties a bed of reddish- brown residuary clay caps the limestone, while above it is a drift sheet. In a trip from Sugartree Ridge to Sardinia several exposures were observed, showing the following series: Generalized section of exposures near Sardinia, Ohio. a 9 1. Clay or silt nearly free from pebbles ----.----------------- ig oh SL Sees s ee ee ee eee 2-4 2. Brown till, deeply oxidized and streaked in places with brownish-black seams-.- -.--------- 3-4 3. Yellow till, usually very stony and slightly cemented; striated limestone pebbles numerous;- TOE So) Installyy OxachiweGl WS INO), D.. = c2s2e52o55 sdcoss sen scesss soso sess =25255255522555255 6-8 4. Blue till, very stony and partially cemented; striated limestone pebbles numerous; color very deep blue} almost black im places== == 222 22s e sae a aa aa eee 10-15 a GENERAL FEATURES OF ILLINOIAN DRIFT SHEET. 275 At a few places near Sardinia a dark band, apparently a soil, occurs between Nos. 1 and 2, but in the majority of sections observed it is not present. The deep-brown color of No. 2 marks the weathered zone and is strikingly in contrast with the pale color of Nos. 1 and 3. Its color more nearly resembles the residuary clay that rests on the subjacent limestones than that of any members of the drift series. It is fully as significant as a black soil in denoting atmospheric action. At Sardinia wells are 30 feet in depth, but none reach the rock, and rock is not exposed in valleys near there whose depth is 30 to 40 feet. Between Sardinia and Mount Oreb, near Whiteoak Creek, two exposures were observed of a soil or black band between the silt and the underlying till at a depth of 2 or 3 feet. Near Mount Oreb station a gas well, in a depression on slightly lower ground than the station, strikes rock at 49 feet A well at J. F. Jenning’s residence, on ground slightly higher than the station, penetrates 68 feet of drift and unconsolidated beds, of which the following is the section: Section of Pleistocene beds in Jenning’s well at Mount Oreb, Ohio. Feet il, Wellon Geni, WOO Myc saiswd se capaqanenccesaas 4058 bas soap Sos se a eeereesoaeeeeecase sass sage 14 Dh {Siniavol navel Fen AS Ses ees es ice nS ee tea Le Sega Se aan eee eA Protez OD 6 SUSR nents a2 oe. ea aes: SSSR GSS OASIS AEA REIS Wea EI Ste ee a rarer ere a 20 Ame luckanmuckeyclaival (preslacially emer aa eee eA c ene ces tes a teen Ss all ot A es oe 15 RAS AT ese te epee etme eames eee n(n ee ace Sale Ae oe oe eto oe SaserSaitie ss we Seals See RES 3 6. Alternations of bluish clay and black muck extending to the limestone.__......._.....-__.- 10 FT CaP epeeee eee new aR STACY OS nil Yo eo Nin stl, nae ea Se 68 On the uplands in Mount Oreb, near the Christian Union Church, is a gas well which has 106 feet of drive pipe, but the rock was struck at slightly less than 100 feet, there being a few feet of rotten rock below the drift. At the Jennings well the drive pipe is 76 feet in length, but it extends a few feet into the rotten surface of the limestone. The difference in thickness of drift is not due to knolls or ridges, but to inequalities of the underlying rock surface, the uplands in the vicinity of Mount Oreb having now a very flat surface. Between Mount Oreb and Williamsburg there are rock exposures in shallow ravines, the altitude of the rock surface being somewhat higher than at Mount Oreb. A soil was frequently observed between the silt and under- lying till, at about 3 feet below the surface. At Williamsburg the East Fork of Little Miami River has rock bluffs rising on each side of the creek to a height of about 20 feet, above which there is about 50 feet of drift, 276 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. mainly till. A short distance from Williamsburg, on the road toward Bethel, rock outcrops up to a level only 15 or 20 feet below the level of the uplands, or much above the level of the rock surface in East Fork Valley. The peculiar drift structure at Bethel was noted above (p. 273). Granite bowl- ders are found on the surface in the vicinity of Bethel, which are, in some cases, 8 or 10 feet in diameter. Similar bowlders are reported from the vicinity of Russellville, in Brown County. East of Bethel, near Hamersville, on an elevated ridge standing about 975 feet above tide, the drift is thin, bemg only 10 to 20 feet in thickness, and the altitude of the rock surface is 90 to 100 feet higher than at Bethel. The drift is thin on the uplands on either side of White Oak Cr eek, in the vicinity of Georgetown, scarcely exceeding 20 feet. The drift at Winchester has a thickness of only 10 feet in the eastern part of the village, but exceeds 20 feet in the northern and western parts. Drift exposures are numerous between Winchester and Seaman, the first railway station toward the east, but farther east there are only scattering patches of drift or occasional bowlders. The general thickness of the drift along the Baltimore and Ohio Rail- road in Brown and Clermont counties and between that railroad and the outer Wisconsin moraine is 20 feet or less, or an amount scarcely half that found in a trip through a tract 12 to 20 miles to the south. This thickening does not, however, assume the form’of a ridge, but as previously noted, simply serves to fill up preglacial inequalities of surface to a somewhat uniform level. From the Little Miami Valley westward across Hamilton County, Ohio, there is a nearly continuous sheet of till, the thickness of which on the uplands seldom exceeds 20 feet, but in lowlands and ee sometimes reaches 100 feet or more. South of the Ohio River there is not so continuous a sheet of drift. Pebbles and bowlders of Canadian derivation constitute one of the con- spicuous features. There are also deposits of a sandy, or more frequently clayey character, through which Canadian rocks are sparingly distributed. In these deposits many local rock fragments occur. They usually bear but slight resemblance to ordinary till, though the presence of granite or other distantly derived pebbles is evidence that they were acted upon by the ice sheet. They appear to be in the main only the slightly disturbed GENERAL FEATURES OF ILLINOIAN DRIFT SHEET. 217 residuary clays formed by a dissolution of the surface limestones of that region. Aside from the deposits noted there are occasional beds of coarse gravel and cobble. The bowlders, as above noted, are usually a foot or less in diameter, but they occasionally reach a diameter of 3 or 4 feet. In his report on the glacial boundary’ Wright notes the occurrence of till in Campbell County, Ky., on the slopes facing the Ohio River. It extends to an elevation of 350 to 400 feet above the river, but no till or granite pebbles were found on the dividing ridge between the Ohio and Licking rivers, whose general altitude is about 400 feet above the river. He describes a stiff clay deposit containing granite pebbles in western Kenton County at points 7 miles south of the Ohio, and also at a railroad cut at Erlanger, the altitude at Erlanger being 475 feet above the — river. Granitic bowlders were also noted in pebbly clay. The heaviest deposits of glacial material yet observed on the Kentucky side of the river are the Split Rock conglomerate in the Ohio Valley and a similar deposit afew miles southeast of Split Rock, both of which were disczssed above (p. 261). On the north side of the Ohio, in the vicinity of Cincinnati, the Illinoian drift, as previously remarked, forms a nearly continuous sheet both on the uplands and lowlands. So far as observed the only localities in which the drift is patchy or attenuated are along the brow of the Ohio bluffs and on some of the sharp ridges bordering the Great Miami. Here in places there are only scattering pebbles and bowlders. The upland drift, beneath the surface coating of silt, consists almost entirely of ordinary till, there being but little sand or gravel associated with it. The lowland drift is more variable, there being much sand, gravel, and pebbleless clay as well as till. The upland drift ranges from a thin coating up to a deposit about 50 feet in thickness with a general average of about 20 feet. The lowland drift usually exceeds 50 feet, and in the larger valleys a thickness of about 200 feet is attained. The till has a brown or yellow color to a depth of 10 or 15, and occasionally 20 or 25 feet. Below this depth it has a blue or gray color. Where there has been no erosion the bowlders are entirely concealed by the silt, and they are not numerous on the hillsides or in places where erosion has removed the silt covering. The fact that few bowlders and *Bull. U. 8. Geol. Survey No. 58, 1890, p. 63. 278 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. gravel deposits are to be seen in the district south of the outer Wisconsin moraine was noted by Professor Orton in his reports on the counties of southwestern Ohio, though he did not recognize the moraine and conse- quently indicated the boundaries of the extramorainic tract im only a gen- eral way. Thus, in his report on Warren County, he calls attention to the fact that the southeastern townships are covered with white clays, while in the northern townships bank gravel is met with on the highlands as well as in the valleys.’ In his report on Butler County (a county lying mainly within the district covered by the Wisconsin ice invasion) he calls attention to the bowlders that occur plentifully at all altitudes, while in his reports on Hamilton County (a county lying mainly outside the outer Wisconsin moraine) he calls attention to the scarcity of the bowlders. In the report of the Indiana survey on the southeastern counties of Indiana similar state- ments are made concerning the drift in nearly every county lying outside this moraine, it being noted that bowlders are seldom seen except along ravines, and that the uplands contain scarcely any bank gravel; while in reports on counties traversed by the moraine or lying north of it, the pres- ence of bank gravel and surface bowlders receives frequent comment. The contrast between the surface features of these districts is, therefore, so striking that it was remarked long before the moraines were recognized. Some of the exposures of lowland drift in southwestern Ohio merit special mention. One of the most extensive is found along the line of the Cleveland, Cmeimnati, Chicago and St. Louis Railway, between North Bend and Cleves. Here there is a gap in the rocky ridge which lies between the Great Miami and Ohio rivers, in which there has been a drift filling to a height of 150 to 170 feet above these streams. The railway has made a cut 80 feet deep in the summit of the gap without encountering rock; while a well in North Bend near the south end of the cut does not reach rock at a depth of 73 feet, though its bottom is nearly as low as the present river bed. Within 80 rods either side of this cut the limestone ledges rise to a height of 200 feet or more, while on portions of the dividing ridge between the Miami and Ohio rivers the rock surface reaches an altitude of fully 400 feet above these streams. Both the railway cutting and the well are mainly through till. There are, however, assorted beds associated with the till. In one place on the west side of the track a funnel-shaped sand 1Geology of Ohio, Vol. ITI, p. 387. GENERAL FEATURES OF ILLINOIAN DRIFT SHEET. 209 deposit completely displaces the till, extending from the top to the bottom of the cutting. Its beds dip and curve greatly, conditions which seem to suggest that they were deposited beneath the ice sheet and disturbed by its movement. There are also horizontal breaks in the till with thin beds of assorted material between, features indicating an alternation of aqueous with glacial deposition. The upper surface of the till is eroded and a bed of assorted material 6 or 8 feet in thickness rests unconformably upon it. This assorted material is principally coarse sand, but is, in places, of a gravelly character, and it grades upward into a silt or fine sand nearly free from pebbles. Between this assorted material and the underlying till there appears in places a dark-colored band, which is sometimes of a peaty character and contains bits of wood but quite as often consists simply of a stain on the pebbles. In one place there was found a thin bed of very fine sand between the peat and the underlying till, and in this sand minute gasteropod shells were embedded. The evidence is, therefore, decisive that the assorted material is a later deposit than the till, but its precise age is not yet determined. The silt which overlies it and forms the surface of this lowland district does not appear to be of markedly later age than the sand and gravel, there bemg no distinct line of separation or unconformity between them. ‘The preservation of the peat beds and the shell-bearing sands, as well as the sandy character of the assorted beds overlying them, seems to indicate that the depositing waters had not violent movement. Since the assorted beds stand oniy 40 to 50 feet above the terraces which were formed in connection with the Wisconsin ice invasion and at a point where the Great Miami makes an abrupt change in its course, the question arises whether an unusual flood or a temporary ice gorge may not have caused the water to rise to a sufficient height to pass across this low gap into the Ohio and thus produce this deposit. There appears to be nothing in the character of the beds to oppose this interpretation, yet it may not prove an adequate one. In the abandoned valley north of Cincinnati connecting Mill Creek and the Little Miami River (see PI. V) there are several exposures of the upper portion of the drift, from which it appears that the structure presents considerable variation. ‘The structure of the lower portion of the drift, as shown by well sections, is also variable, there being in places heavy beds of blue silt, while in other places there is gravel, and in still others till. 280 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The opinion is expressed by Orton, in the Ohio reports, that this lowland is filled with alluvium, and Wright's reports contain the same opinion, though the latter makes mention of till in this district. The numerous exposures, some sections of which are given below, will make it evadient that the drift here is glacial rather than alluvial. This lowland tract carries a few undulating surface swells 10 to 15 feet and occasionally 20 feet in height, whose forms could scarcely be produced by erosion. A good illustration may be seen in the southwestern part of Madisonville, on the west side of Columbia avenue, the residence of EK. $. Emerson being built upon a swell that stands nearly 15 feet above the bordering tracts. A cistern at Emerson’s shows the swell to be com- posed of till. This lowland tract is drained by a small stream (Dutch Creek) leading eastward into the Little Miami River, and a score or more of exposures along the banks show ordinary till. Beds of silt are associated with the till, but as often as otherwise they underlie it, except in the case of the surface silt, which forms here, as on the uplands, a continuous capping for the till. y In a ditch on the east side of the electric railway, between the Zoologi- eal Gardens and St. Bernard, and near the south border of this lowland tract, is an exposure with a silt deposit 3 to 4 feet, beneath which is fine sand, somewhat contorted and wavy, thickness 3 to 4 feet; then follows a yellow till, very stony, about 20 feet in thickness, beneath which is a pebbly laminated clay of deep-blue color, in which the bedding has contorted or disturbed lines. This blue stratum is exposed to a depth of 25 or 30 feet. On Rose avenue, in St. Bernard, a few rods east of the canal, the following beds are exposed: Section on Rose avenue, St. Bernard. Feet ile | @laly,@ ygSata Cetera yey pete are ei) ea ote tatere le els are =e Sie chara = Lid Spa eiclele Scan te Sle a epee 4-5 2. Pebbly clay of yellow color, doubttully classed|.asstilll 2 25 02 jee Sea Sse eae eee eee eee 3-4 oaekebolyaclayaoindank-bro wm) COLORS ssp ee set e= yer ele cise elt e eee eee ee ae eee eee eer 1-24 4, Fine calcareous clay loam, nearly free from pebbles, porous at top, and of sufficient coarse- ness in places to be called a sand, but grading below into a compact laminated clay, color varying from yellow to blue, but mainly blue near base.....-......--..------------------ 7-8 Hs wOrdimanyayellowaille emcee = 25 stones eee aces Scscis eee de ee ee Sere eae ee ee 3-4 6Ordinaryabluetill exposedé 2 Sil si242 Gls. see Lo Sees Se cae eee Se eee eee eee 2-3 In the vicinity of Bond Hill there are sand deposits which extend east nearly one-half mile from Mill Creek Valley, and lie north of the lowland tract under consideration. ‘They reacha height of 45 to 50 feet above the GENERAL FEATURES OF ILLINOIAN DRIFT SHEET. 281 plain in Mill Creek Valley, immediately west and about 160 feet above the Ohio River. The method of deposition of this sand is not clearly under- stood. Occasional small pebbles, one-eighth inch or more in diameter, contained im the sand seem to indicate that it is not entirely a wind-drifted formation. The till with its capping of silt passes beneath this sand, a fact implying that the sand is more recent than the silt. The sand is probably connected in some way with the floods attending the Wisconsin ice invasion. The features suggest that it may have been deposited during a rise of water occasioned by an ice gorge in the valley of Mill Creek below Carthage, the width of the valley being somewhat reduced in passing Walnut Hills just before it enters the Ohio Valley. In passing through this lowland tract the Panhandle Railway makes numerous cuttings 10 to 20 feet deep, which in nearly every instance expose a silt 4 to 5 feet thick, below which there is ordinary till. In one cut near Pleasant Ridge there is a bed of assorted material (sand and gravel) between the yellow and blue tills, but in the majority of cuttings the yellow till grades downward into the blue. Within the village of Madisonville there is an abrupt change in the substrata, the western portion of the village being underlain by till to a depth of 40 to 50 feet or more, while the eastern is underlain by gravel at slight depth. Above the gravel there is in some places only a silt deposit; in other places there is a deeply oxidized (reddish-brown) clay carrying a few pebbles. The age of the reddish clay is not known, the situation bemg such that it is difficult to determime. It occupies a basin or slightly depressed tract and may, therefore, have received contributions in post- glacial times by the wash from the neighboring highlands. It is also sufficiently low to have been flooded by the Little Miami, at least down to the time of the Wisconsin ice invasion. The bearing of these conditions upon the question of the Madisonville chipped stone, which was found at the base of this red clay, was discussed by the writer some years ago, and the conclusion was reached that the deposit can not be referred with certainty to glacial agencies; in fact it may be much more recent than the last stage of glaciation. 1 Supposed Glacial man in southwestern Ohio, by Frank Leverett: Am. Geologist, Vol. XI, 1893, pp. 186-189. 282 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The following section was obtained in the southwest part of Madison- ville, where a street (Columbia avenue) has been graded down: Section on Columbia avenue in Madisonville, Ohio. Feet 1. Clay or silt, nearly free from pebbles, color light brown_-....-...-.-..----.---------------- 3-4 2. Pebbly clay of dark-brown color, slight traces of bedding, with crumpling and disturbance... 4-6 3}, Ieiconyiam willl syratilon JoMlble) StiMERN MS) = = 8 Se oo eae ease cased spooecaccs aeeesese ees 4 4. Gravel and sand in horizontal beds, exposed.......-..---------------------------=-=---+- 7-8 WNOWM eS - coasacasancseunqsau sc cEssEseao ener noe ade ance aoneess enndecoseséeqsucsusses 20-22 A short distance west the same street grade shows a change in the till (No. 3) to a fine laminated clay, while the underlying bed becomes disturbed. ; Just north of Batavia Junction, where this lowland tract opens into the Little Miami Valley, there is a bluff rising to a height of 80 feet above the station or about 140 feet above the Ohio. The following beds are exposed: Section near Batavia Junction, Ohio. Feet iva Sanciysauriacereposltsates. sj... a8a- cee: seco 2 oo. 2 ee ee ee ee 5-10 2. Yellow clay containing blocks of local limestone. -.-..-.--.--.------------------------.--- 15-20 83. [bos RANG! oo pceedsdson oes sce oe sae seep onsanee coe orenacesechtestetopessecsasspssesse 15 A Greprell, maeihivian {oy COR ea ose eceeoesemee Seb eee ae Spe sceds sooaascedsncoceeenudaceesseene 40 It seems not improbable that the gravel beds here exposed extend north into Madisonville, there being nothing in the topography to oppose this view and the distance being only a mile. A short distance west of Batavia Junction the Wisconsin gravel appears in the form of terraces along the face of the bluff, the upper terrace being about 40 feet below the level of the border of the lowland tract under discussion. Calcareous nodules were observed at many points in this lowland tract in connection with the silts which underlie or replace the till, but they are not common here or elsewhere in connection with the silt that overlies the till and forms the surtace of the uplands and are seldom found in the till itself, An exposure was noted, however, just east of the gate of the Zoological Garden and near the top of the north slope of the Walnut Hills Ridge, where nodules appear in a pebbly clay just below the silt, the section exposed being: Section near Zoological Garden in Cincinnati, Ohio. Feet. il, Stik Or pale Welllony @dlORs 252 5scsc0scosnescssaced ssa sasacsostocsosooseasosbosoessosssesers + 2. Clay containing few pebbles, but thickly set with calcareous nodules. .-.-.........----.-.-- 2 3 HOrdinanyay.ello wail exposed ese ee sees al eee lanier Sane eens ee eee 6-8 \ | : : GENERAL FEATURES OF ILLINOIAN DRIFT SHEET. 283 Sections of several wells along Mill Creek Valley are given in the discussion of the early Wisconsin drift (Chapter X). The greater part of the drift is probably Ilimoian, as appears in that discussion. The portion of the Hlinoian drift sheet covering southeastern Indiana was the subject of only a hasty reconnaissance by the writer, and very few detailed sections can be furnished. Numerous exposures were found in which yellow till extends to the rock, the distance to rock on uplands being generally 20 feet or less. Well sections published in.the Indiana reports, which throw light upon the deeper parts of the drift are here reproduced: Section of Van Osdel well in Ohio County, Ind. (sec. 6, T. 3, R. 2 W.). Feet ils. Soull pial. GENS. 465 4 Se odes Shares eeeate BRASS es Henne ene see Meeenn Ress Renae aa seerseo 22 Zee llovgsanc quite nardsorcemented meena as mas e eas oe seo bce nae eee Heenan eee 9 Se blweyclayapharcenwabnontspeb bles setae seem ee see ase ancae c= aascnoe oaks Sere a erene 13 4. Black soil containing rotten leaves, twigs, and wood, thought to be walnut..:........._.-. 13 i, Coane saindl, ernitalls cull slay Gimme S55 525560 eeeeoe done a peesea see ser encescenaeeaos 9 Gopiardaiblueslimestoneeyaa= ser a= ame ctee sae ne aoe hie ones cm wees gas whe Same ements il ho taller eee ee cime nee nmr ME sip ton h. Seh Sekt does me cles oatienae sen oee 44 Section of Gorden well in northwest Switzerland County (sec. 4, T. 5, R. 12 E.). Feet ie Soilvandaclaypapalenmnulowen pantencecces sae ssa seen sae cine ee ce oe cae eee ee eee 22 2, Alive iminl mesial olor meet AUlllenmIbINN < Se sseeoo cece ses oa sease seeg6 ss se405aceoboassceds 6 3. Black soil containing leaves, cedar wood, and ocherous particles--..-...-..------.--------- 3 AM Srnoallastonestcloselyapacked tore tmeneesmesesee ees aoe esas eisces cece eects See ase ee eee 1 PLO Lalla seperate eee ae eee sae cee mined Soins ema ase olsmcieeles beige S EUs See memes 32 Wells in that vicinity often enter rock at 10 to 14 feet, but a neighboring well struck leaves and poplar bark at 32 feet. It is thought that the bottom bed in the Gordon well is native rock. In the vicinity of Paris Crossing, in the extreme southern part of Jennings County, buried timber is often found in digging wells on land 60 to 70 feet above the bed of Graham Creek. From one well, sunk by Mr. John F. Files, it is estimated that at least a half cord of wood was taken, at a depth of 32 to 40 feet. The wood appeared to be birch, and specimens were sent to the State museum. The wood was much erushed and twisted, but it was found suitable for fuel, and was made use of by Mr. Files. The following is the section of the beds penetrated: Section of Files well, near Paris Crossing, southern Jennings County. Feet 1) hight-colored clay with darker shades below...-------2---=--2--------+----------2------- 10 2.. Ocher-colored clay with flint pebbles, increasing in hardness toward the bottom......--..-- 19 oa VeD banda beduoleclaygam dipravelistn ve aise = selene coo rate ee eee mine ae ereie ee eee cleaerane 2-2 4, Sandy blue clay with water; also limbs, twigs, and roots of trees .....-....-.-------------- 7-10 284 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The ingress of water prevented the deepening of the well, and the wall was commenced on the driftwood at its bottom. A well at South Milan, in eastern Ripley County, 54 feet. in depth, did not enter rock, though quar- ries are opened in that vicinity at about the level of the well mouth. The following is a section of the well made by the railway company: Section of railway well at South Milan, Ind. Feet Inglis ht-coloredk clays san ss sewer seln-< cies ase bcs 12 21a Sara siamese eee lai ee eee eee 10-14 2Zanvellows clays wathuttiontvonarel send etossilli corals! sem sess ae eee eee eee 12 Sa Bluevolacialiclayseeten one ne stot esc Sear eee e kOe aoe See tee Dae eee ee ees 1” 4. Coarse yellow sand with recent shells and water.......-.-...----------------------------- 8 5. Blue clay and muck containing roots and limbs of trees ...--..--...---.---.--------------- 8 M olaleerewe as seme was Sasa e Ses ee es oe aelsase S22 See eee Se econ a Se eee eee 54 Statistics concerning wells were obtained at several villages on the uplands in these southeastern counties of Indiana, as follows: At Versailles, the county seat of Ripley County, wells are obtained at depths of 18 to 25 feet in the upper part of the limestone. At Osgood they are usually obtained near the base of the drift at depths of 9 to 15 feet. Occasionally they are drilled to a depth of 100 feet or more im the northern part of Ripley County. At North Vernon, in Jennings County, wells are obtained usually at depths of 12 to 35 feet, the majority being about 25 feet; they enter the rock a few feet. At Charlestown, formerly the county seat of Clark County, many wells are obtained at a depth of 3u to 35 feet, usually im the Corniferous limestone. A few, however, reach this depth without entering rock. In wells where drift 25 to 30 feet in thickness is penetrated it is common to find a blue mud carrying tree trunks or small pieces of wood near the base of the drift. Rock is ordinarily struck in this village at about 12 feet. There are four very strong springs within the corporate limits of the town, which are used by many of the residents. At Scottsburg, the county seat of Scott County, wells are usually obtained at 25 to 35 feet or less. A gas-well boring near the railway station penetrated 47 feet of drift, as follows: Section of drift in gas-well boring at Scottsburg, Ind. Feet, 1. Yellowish white clay, nearly pebbleless ........................-..------------ 15 Pe SPIE Ck Be Las ese Oe BEEP ACES cee Meee Sete gny SORE Erne pe roel ae eetedi hs Pca Sy 5 _— OUTWASH OF ILLINOIAN AGE. 285 In the Whitewater Valley several borings for gas have been made out- side the limits of the Wisconsin ice invasion. They fall within the limits of a terrace of Wisconsin gravel, but as the Wisconsin gravel probably extends little, if any, below river level a large part of the material is thought to be Ilinoian. A boring at the brickyard in the south part of Brookville shows the rock floor to be about 180 feet below the low-water level of the stream, or but 440 feet above tide. Three other borings in the valley near Brookville enter rock at a level about 125 feet below the river, or 495 feet above tide. A gas boring near Cedargrove, also in this valley, penetrates 154 feet of drift and enters rock at about 450 feet above tide. At the mouth of the river the rock floor is less than 400 feet above tide SECTION III. CHARACTER OF THE OUTWASH. GENERAL STATEMENT. In the western part of the region, from near Louisville, Ky., eastward to near Maysville, the ice sheet at its culmination occupied the Ohio Valley so completely that drainage must have been greatly obstructed. As indicated above, the deposits appear to have been very uneven; parts of the valleys apparently received but little drift, while other parts were filled to a height of 150 to 200 feet above the present stream. The filling is also variable, bemg in places a fine silt, m other places an ordinary till, in other places assorted sand and gravel, and in still other places a conglom- erate with a large number of coarse stones in a matrix of clay or fine sand. In some of the valleys in central Ohio a terrace composed of well-assorted sand and gravel appears, which is probably of Ilinoian age. Reference has already been made (p. 102) to the terrace in the Scioto Valley. This and similar terraces in valleys farther east will now be considered. The discussion begins with a terrace in Sandy Creek Valley, that being the east- ernmost valley in which there appears to be good evidence of an outwash of Ilinoian age. Valleys to the west are then taken up in succession. SANDY CREEK VALLEY. About 1 mile east of Minerva, Ohio, Sandy Creek, a tributary of Tus- carawas River, leaves the Wisconsin drift and enters what appears to be an ungilaciated tract. For several miles below the limits of the Wisconsin drift it seems to have only one terrace above the flood plain, and this is in all probability of Wisconsin age. Near Waynesburg, Ohio, a higher 286 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. terrace appears, which seems to be much older than the Wisconsin terrace. It stands about 70 feet, while the Wisconsin terrace in that part of the valley rises scarcely 40 feet above Sandy Creek. It is preserved only in a recess on the south side of the valley, and there has a much more eroded surface than the Wisconsin terrace. It contains a sandy gravel which shows a greater degree of weathering than the Wisconsin gravel, and it has been opened extensively by the railway company to obtain gravel for ballast. The entire deposit is deeply weathered and many of the stones are very rotten. A few granite and quartzite pebbles, 3 inches or less in diameter, were found after prolonged search, but there is a much smaller percentage of such rocks than in the gravels of Wiscons’n age found on the lower terrace along the creek. The valley was examined below Waynesburg as far as Sandyville, but no other remnants of the old gravel were observed. The occurrence of this old gravel suggests that the border of the Illinoian drift sheet may lie not far back to the north; but, as indicated in the discussion of that drift, no exposures have been noted outside the Wisconsin drift in that part of Ohio. TUSCARAWAS AND TRIBUTARIES. No other remnants of such old gravel have been observed on the Tuscarawas or its tributaries, though the valleys have received only a hasty examination, and some of them have received no attention. The same is true of the valley of Killbuck Creek, a tributary of Walhonding River. The Walhonding emerges from the old or Ilinoian drift a few miles above its mouth, but examinations have not been carried down the valley sufficiently to determine whether there was a notable outwash. Waha- tomaka Creek also emerges from the old drift some distance above its mouth, but the portion outside the drift border has received no attention. We accordingly pass to the next valley to the west, Licking River, and consider its outwash and that of its continuation, Muskingum River. LICKING-MUSKINGUM VALLEY. As noted in the discussion of the drift border, a great dam was built across the old westward line of discharge of the Muskingum, at Hanover, Ohio, which stands about 100 feet above the portions of the valley on each side, and-perhaps 300 feet above the rock floor of the old valley. While OUTWASH OF ILLINOIAN AGE. 287 the dam was accumulating a lake probably occupied the valley to the east. The filling is largely a fine silt of blue color, capped by a few feet of gravel and sand. The amount of filling has been sufficient to cause a new channel to be opened by the Licking for a short distance in the vicinity of the drift border. In the tract lymg between the Licking and the old valley of the Muskingum, east from the drift border as far as the present valley, there has been a general filling up of valleys, not only on the main lines of drainage, but also on the tributary lines. Much of the filling is a fine silt, but the surface, as in the dam at the drift border, is of coarser material. In some of the tributary valleys small drift pebbles have been ‘observed on the slopes up to a level 25 feet or more above the flat valley bottoms, a feature which seems to indicate that the region has been submerged to levels above the valley bottoms. It is suggested that the prevailing west winds may have carried cakes of ice laden with pebbles from the vicinity of the drift border eastward into these valleys, passing, in some cases, over low divides, and thus distributmg them outside the range of the present system of drainage. _ The glacial lake which was held in this portion of the Muskingum Valley discharged southward to the Ohio across the old divide south of Zanesville. The volume of its discharge was probably much greater than that of the present Muskingum, since it appears to have carried nearly all the drainage of the ice field in northeastern Ohio. The high-level gravels below the old divide at McConnelsville, and at points farther down the valley, may prove to have been deposited by the glacial waters crossing this divide. But as yet this is merely a matter of conjecture. The gravel at McConnelsville has an aged appearance quite similar to that of the glacial gravels connected with the Illinoian drift, and decidedly im contrast with the fresh gravels of Wisconsin age, which occur at lower levels in the valley. In this connection it may be remarked that gravel of Wisconsin _ age has been deposited in such large amount along the line of the Licking below Hanover and along the entire length of the Muskingum that the outwash from the earlier ice field has been rendered rather obscure, except at the great dam near Hanover. 288 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. HOCKING VALLEY. The Hocking Valley appears to have been a line of vigorous discharge for glacial waters during the Illinoian ice invasion, there being a large amount of gravel and cobble in its middle and lower courses outside the limits of glaciation, which seems to have been derived from the Illinoian drift. Much of the gravel has been carried beyond the supposed old divide below Sugargrove, there being extensive remnants in the vicinity of Logan and Haydenville; and also north of Athens. The old gravel has been largely removed in the part of the valley above the divide down to ‘a level at least as low as the Wisconsin terraces, but it can be traced up to the Ilinoian drift border. Reference was made in the discussion of the drift border to a terrace on the lower course of Clear Creek that leads down to the Hocking and also to the old gravel in the Hocking Valley at ' Lancaster. These seem to be near the head of the glacial drainage. The altitude of the gravel terrace decreases in passing down the valley at about the rate of fall in the river, and the terrace stands 80 to 100 feet above the stream. At Lancaster the gravel has an altitude of nearly 900 feet, at Logan scarcely 800 feet, and near Athens about 700 feet above tide. The general elevation is about 50 feet above the terraces of Wisconsin age in the valley. ; The gravel varies greatly in coarseness, some portions being rather fine with a liberal admixture of sand, while other portions are a coarser gravel and cobble. On the whole the material is coarser than is usually displayed by terraces connected with the Illinoian drift. It is often firmly cemented mto a conglomerate, the cement being usually calcareous, but in some cases ferruginous. As noted above, this conglomerate is used at Lancaster in stone fences. Near Logan its outcrops on the face of a terrace bear a strong resemblance to rock ledges. Granite, quartzite, and other Canadian rocks, though not so abundant. as in the gravels of Wisconsin age, are well represented all along the terrace. Some of these rocks, in a remnant of the terrace near the school-° house in the north part of Logan, are 5 or 6 inches in diameter. They are nearly as coarse in the terrace north of Athens. In the vicinity of Logan a valley fully one-half mile wide seems to have been filled with this old gravel from a level about 75 feet below the river to a level fully 80 feet above it. For a distance of 3 miles below OUTWASH OF ILLINOIAN AGE. 289 Logan remnants are very extensive, occupying one-third to one-half the width of the old valley. From that point to Chauncey nearly all the gravel has been removed down to a level as low as the Wisconsin gravel; but between Chauncey and Athens a section of the old valley is abandoned, and more than a square mile of the gravel filling is preserved. Below Athens no remnants of the old gravel were noted. Possibly the deposit was not carried in large amount farther down the valley than the abandoned section above Athens. SALT CREEK VALLEY. As indicated in the discussion of the drift border, the North, or main, Fork of Salt Creek appears to have held a small glacial lake during the deposition of the Illioian drift, into which but little material except fine silt was carried. The lake discharged across an old divide near the point where the present stream passes from Hocking into Vinton County, into a valley that opened southward to the Scioto, but it seems not to have carried much material into that valley. The South Fork of Salt Creek, though lymg apparently entirely outside the limits of glaciation, is so situated that the glacial accumulations on the Scioto at the mouth of the creek held a lake in the creek valley into which the glacial waters passed, and at the head of which they opened a passage southward to the Ohio. This lake received a large amount of fine calcareous sediment, the depth at the present divide between Salt Creek and Symmes Creek near Camba being not less than 90 feet. SCIOTO VALLEY. Attention was called in the discussion of the Ilinoian drift border to a prominent gravel terrace on the Scioto, which heads at the glacial boundary east of Chillicothe. ’ This terrace, which at its head stands about 100 feet above the Scioto, has been built up at that point from below river level. Passing southward, down the valley, one finds the glacial gravel covering a series of rock shelves, which show a slight increase in altitude in that direction. It declines in altitude about 50 feet in passing from the glacial boundary to the mouth of the Scioto, where it barely comes to the level of the rock shelves. From more than 100 feet opposite Chillicothe the depth of the gravel becomes reduced to but 15 feet at Coopersville, near the line of MON XLI——19 290 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Pike and Scioto counties, about 30 miles below. The surface in that dis- tance falls from fully 700 feet above tide to 650 feet or less, while the rock shelf, or old valley floor, rises from below 600 feet to fully 625 feet. The material in this terrace varies from a well-assorted gravel of medium coarse- ness to a sandy and clayey gravel very imperfectly assorted. As a rule, the gravel contains a large amount of sand. The current was probably moderate except, perhaps, on the immediate borders of the ice sheet. The gravel, like the drift from which it was derived, contains only a few Cana- dian rocks, yet they have been found as far down as Coopersville. In an old oxbow back of Lucasville, discussed in Chapter III, no glacial deposits were noted, but pebbles were found on the inner slope up to a level above the probable limits of the fillng by glacial gravel. These pebbles, as well as the material in the bottom of that oxbow, may be older than the glacial gravel. The altitude of the bottom of the oxbow is fully as great as the glacial gravel at Coopersville, and no Canadian rocks were found in it after prolonged search. MIDDLE AND LOWER OHIO VALLEY. The portion of the Ohio Valley which was covered by the ice sheet, from near Maysville down to the vicinity of Louisville, Ky., received a large amount of drift, some of which is evidently waterlaid. It is not, however, so distinct an outwash from the ice sheet as that found in valleys to the east, already discussed. Much of it was probably deposited as directly _ by the ice sheet as the till of the bordering uplands. It has accordingly been treated in connection with the drift sheet. By reference to these descriptions, it will be seen that the filling varies greatly im constitution, as is to be expected in a partially obstructed valley. The encroachment of the ice sheet on a part of the Lower Ohio at the Tilinoian stage of glaciation may seem to oppose the view that some of the gravel carried down the Scioto was of Illinoian age. It seems probable, however, that the drainage through the Ohio was obstructed for only a brief time if at all. The glacial boundary at its farthest point extends but 10 or 12 miles beyond the Ohio, and generally but 2 to 5 miles. It is not certain that so slight an extension could cause complete damming. Furthermore, the ice sheet extended beyond the Ohio during only a small part of the Illinoian stage of glaciation, thus leaving the valley open OUTWASH OF ILLINOIAN AGE. 291 most of the time, except for the drift filling, and this was not sufficiently high to greatly impede the flow of water from the upper part of the Ohio and its tributaries. The filling is generally below the 600-foot contour, which is 100 feet lower than the head of the gravel terrace on the Scioto, and perhaps 25 feet lower than the gravel filling near the mouth of the Scioto. Below the limits of glaciation the Ohio Valley has received only a hasty examination, and no deposits have been found that seem to be referable to the Hlnoian outwash. The examination has, however, not been sufficiently complete to make certain that such deposits do not exist, and it is possible that some terraces which have been referred provisionally to the Wisconsin may prove to be older. CO) IEE AU IE MP ID Ta WW IDL. THE SANGAMON SOIL AND WEATHERED ZONE. After the Illinoian stage of glaciation the surface of its drift sheet became weathered, and a black soil was formed on the level or poorly drained portions. This weathering and the forming of a soil continued for a considerable period, as is apparent from the state of decay of the pebbles and the leaching of the till, there having been usually a complete leaching of the lime from the finer part of the till to a depth of several feet, accom- panied by a nearly complete dissolution of limestone pebbles. This weathering has not continued to the present day, for the surface of the Ilinoian has received a coating of silt several feet in depth, which now prevents further weathering. This silt deposition and interruption of the weathering, as indicated below, are thought to have occurred in con- nection with the Iowan stage of glaciation, in which case the soil and weathered zone stand for an interglacial stage between the Illinoian and Iowan glacial stages. The name Sangamon has been suggested for this interglacial stage by the writer because of the excellent development of the soil in the Sangamon River drainage basin, in central Illinois, and because the exposures there were among the earliest recognized in this country." The Sangamon soil and weathered zone may be seen beneath the sur- face silt in thousands of exposures in southeastern Indiana and southwestern Ohio, for the general thickness of the silt is only 4 or 5 feet. Farther north there are, in addition to the silt, the heavy deposits of Wisconsin drift, which have buried the soil and weathered zone to such a depth that it is rarely ~ exposed. However, a few exposures have been found in the deeper valleys, and wells not infrequently penetrate both the silt and the soil under the Wisconsin drift. 1The Sangamon soil and weathered zone, by Frank Leverett: Proc. lowa Acad. Sci., Vol. V, 1898, pp. 71-80; also Jour. Geol., Vol. VI, 1898, pp. 171-181. Numerous instances of occurrence within the limits of the Illinois glacial lobe are cited in Monograph XX XVIII of this Survey. ; 292 SANGAMON INTERGLACIAL STAGE. 293 It is this soil which attracted the attention of Orton in his examination of wells near Marshall, in Highland County, Ohio,’ but the soil there is within the limits of the Wisconsin drift. It is probable that the deposits of peat below the Wisconsin drift near Germantown, in Montgomery County, Ohio, also brought to notice by Orton,” are referable to the Sangamon. In fact, the great majority of buried soils reported in Ohio, Indiana, and Illinois appear to be at this horizon. The soil attracts attention more effectively when found at considerable depth than in places where it is covered by only a few feet of silt. One often passes it in the latter situations without realizing that it is really at a lower horizon than the surface soil, for the surface soil is liable to be washed down the slope below the level of the Sangamon soil. A careful inspection, however, will place beyond question the frequent occurrence of the Sangamon soil. In many cases it can be traced back along ditches until it passes beneath the surface silt, but where this can not be done an examination of the constitution of the Sangamon soil will reveal the presence of pebbles, which distinguish it from the pebbleless surface soil. The Sangamon soil, in the region under discussion, does not commonly show a black color, though exposures of such a color are met with in all parts of the region. he evidence of a land surface is more generally found in the deep-brown color and weathering or soil-producing disintegra- tion of the upper part of the till. The deep brown changes gradually below to the ordinary yellow color of oxidized till, but at top it terminates abruptly at the base of the overlying silt. The color of the silt being much lighter than that of this brown soil, the contrast is very marked. The deep-brown color extends usually to a depth of 2 feet or more, while leaching and discoloration are noticeable to 6 or 8 feet. The amount of discoloration is somewhat greater than is commonly found at the surface of the Wisconsin drift, and numerous comparisons of the Sangamon soil with the post- Wisconsin soil lead to the opinion that the Sangamon involved more time than has elapsed since the culmination of the Wisconsin stage of glaciation. The same opinion is reached upon comparing the amount of leaching. On the Illinoian drift it is rare to get a response with acid within 6 to 8 feet of 1 Rept. Geol. Survey Ohio, 1870, p. 266. 2 Am. Jour. Sci., 2d series, Vol. L, 1870, pp. 54-57, 2938. See also Rept. Geol. Survey Ohio, 1869, pp. 165-169. 294 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the surface, whereas in the Wisconsin drift the leaching has seldom been carried to so great a depth as 6 feet. It seems clear from the »osition and relations of this old land surface that the leaching took place before it was buried under the silt. In view of these facts, this may safely be considered one of the main intervals of deglaciation. The erosion of the Illinoian drift in the Sangamon interglacial stage was not so conspicuous a feature as the weathering. This is true not only in the région under discussion, but also in the region to the west, covered by the Illinois glacial lobe. The channeling seems to have been shallow and broad wherever new lines were opened, while the old lines, being already largely open, suffered but little excavation. These features indicate that drainage conditions were less favorable than now, but they should not be cited against the evidence of a long interval derived from the leaching and weathering of the surface. The conditions for erosion seem to have become worse rather than better toward the close of the Sangamon interglacial stage, and in the stage which followed, as indicated below, erosion was either suspended or became so feeble as to allow silt to accumulate on the surface. CieACP BER Iie THE LOESS AND ASSOCIATED SILTS. GENERAL STATEMENT. On the borders of the Mississippi and its main tributaries there is a very porous silt which overlies the Sangamon soil and weathered surface of the Illinoian drift sheet, and which has long been known as loess. It is commonly calcareous to a marked degree, though its main ingredients are siliceous and argillaceous particles. A series of chemical, mineralogical, and mechanical analyses appear in Monograph XXXYVIII of this Survey. Portions of the loess are highly fossiliferous, with a fauna composed chiefly of terrestrial species of mollusks, but containing also species which inhabit ponds, and occasionally a fluviatile mollusk. Lists of the fossils are also given in Monograph XXXVIII. On the uplands back from the Mississippi and its main tributaries, and also along the minor tributaries, there are silts of more compact texture than those which border the valleys. Mechanical analyses of samples col- lected in Illinois, also appearing in Monograph XX XVIII, show that there is a larger proportion of very fine particles in these compact silts than in the loess bordering the valleys, but that in many respects they are similar. The porous loess does not contain coarser particles than are found in the compact silt. DISTRIBUTION. The compact silt extends eastward in a practically continuous sheet from Illinois over southern Indiana, southern Ohio, and neighboring portions of Kentucky and West Virginia, and is the surface deposit as far north as the border of the Wisconsin drift sheet. It is known to underlie the Wis- consin drift, numerous exposures having been found beneath that drift. This silt has long been recognized in the glaciated districts of south- western Ohio and southeastern Indiana. In the Ohio reports it is referred to as the ‘‘white clay,” and in the Indiana reports as “slash land.” It has 295 296 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. not been known so long that a similar silt extends outside the limits of the Illinoian drift. Wright has called attention to a silt on Beech Flats, in. Pike County, Ohio, which was cited as an extra glacial material, but it now appears to be underlain throughout by glacial deposits." In the writer's examinations in southeastern Ohio and neighboring parts of West Virginia and Kentucky, in 1896, it was found that the silt occurs at least as far east as Parkersburg, W. Va. Examinations in the Beaver Valley, in Pennsyl- vania, in 1898, as indicated on page 252, have raised the suspicion that: it occurs there. It may also occur on the Monongahela and its tributaries, for the terraces there are in many places capped by a compact silt several feet in-depth. This, however, is merely a conjecture. Its limits will not be easy to determine, for it is so thin that it is likely to be preserved only on comparatively flat areas where erosion has been very slight. Wherever flat uplands appear in southeastern Ohio from the glacial boundary east- ward to Parkersburg, W. Va., the silt capping is clearly recognized. It is especially noticeable in parts of Morgan County, near McConnelsville, which are underlain by limestone, for the silt contrasts more strikingly in color with the residuary products of the limestone than with those of sandstone. The extent of this silt northward beneath the Wisconsin drift is unde- termined. It has been found at some distance back from the border, both in southeastern Indiana and in southwestern Ohio. THICKNESS OF THE SILT. The thickness of the silt on the uplands of southeastern Indiana, northern Kentucky, and southern Ohio, where it overlies the Ilinoian drift, averages scarcely 5 feet, and seldom reaches 10 feet. As the exposures are mainly on slopes where more or less removal has occurred, the thickness seems to be only 2 or 3 feet, but the wells or excavations on flat uplands correct this interpretation and show it to be about 5 feet. The thickness varies but little from place to place, though it seems to be less on uplands near the Ohio Valley than farther north near the limits of the Wisconsin drift. This difference may be due to greater erosion on the borders of the Ohio, where the surface is more completely dissected than at points some distance back. But there is also a strong probability that some silt has been deposited as an outwash along portions of the Wisconsin border. 1Bull. U. S. Geol. Survey No. 58, 1890, pp. 92-96. THICKNESS AND CHARACTER OF THE SILT. 297 The thickness of the silt on uplands outside the limits of the drift is even less than on the drift, though it probably falls short but a foot or two. The estimates are mainly from exposures on slopes, there being few oppor- tunities to learn its thickness on the level upland. It should be borne in mind, also, that the country outside the limits of glaciation is generally much more uneven than in the glaciated tracts, and that flat areas such as would hold the silt in its full thickness are comparatively rare. The silt is seldom preserved in the Ohio Valley, the exposure at Parkersburg being the most conspicuous instance noted. In the northern part of the city it covers an island-like hill which stands about 175 feet above the river, and it there has _a thickness of 12 to 15 feet and a porous texture similar to the loess along the valleys farther west. In the abandoned valley of the Kanawha, leading from St. Albans, W. Va., to Huntington, known as Teays Valley, there is apparently a thin bed of the silt under discussion, capping a thick deposit of silt of different color. he thickness is only 5 or 6 feet, or but little greater than on the bordering uplands. The deposits in the Beaver and Monongahela valleys which are con- jectured to be of this age are only a few feet in depth, those on the Beaver being 5 or 6 feet and those on the Monongahela but little thicker. CHARACTERISTICS. coto.— The color of the silt is a distinguishing characteristic, for it is in striking contrast with both the underlying till and with the residuary clay, and is remarkably uniform throughout its extent in this region. It is generally of a pale yellow or ashy color from top to bottom, the soil as well as the subsoil bemg pale and light colored. For this reason it is widely known as ‘‘white clay.” In parts of southern Ohio and southeastern Indiana this deposit has given rise toa black soil. This is found mainly in exceptionally flat portions of the uplands, and does not prevail very exten- sively there, the level tracts being usually characterized by a very light- colored soil. Texture——The name silt indicates that this deposit is of fine texture. Ordinarily it contains no grains or rock fragments sufficiently coarse to be detected by the naked eye, but in a few places occasional small pebbles have been noted in it, usually near the bottom of the deposit. The rarity of these pebbles raises the suspicion that they may not be normal to the 298 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. deposit. In some cases they may have been brought up from the underlying till by burrowing animals long after the silt was laid down; but im other cases they seem to have been brought in during the process of deposition. A few were found in the unglaciated parts of southeastern Ohio, where their presence seems difficult to explain unless they were laid down with the silt. The pebbles are generally of quartz, though a few other very resistant rocks are represented; this is true of pebbles in both the glaciated and the unglaciated tracts. Chemical constitution—But one analysis of this silt has been reported. This first appeared in the Geology of Ohio,‘ and was made by T. G. Wormley, State chemist. The specimen was obtained on the level upland in western Highland County. Analysis of white clay from western Highland County, Ohio. Per cent. Wiatericomibinedip terse. eee ks ds Se oa oN Se pS ee Se Oa en 5.54 Siltcictacideeeeseaseeseses Pine else seen sae ee dels Se Cauts oe aoe Ste CEe NES ee eee eee eee 62.60 Hip es ale eee Ss Ie RA RS a ae ae ee ee Me eee reese nee ae ee otmoobok 18.90 Sesquioxidevofmaronee’ ss ssa 2 ek ee Se oe oe GE See eS eye pace te Cee rn a ee 6.30 IVAN PANCSE Mame eer eae ees eis els Se esc a ete mo Slee Wis Slade sete sso Slap ae eee yee ees 0.20 Phosphateyotulime: 36256 bee cesses ok hole. Se teie ies Se ea i ye See a eee ere 0.63 Carhbonaterotdimeyeaekeeen = een smaance case coe Sek cmisicia eras Slee eC Soe ee eee eee 1.89 @arbonateyoimapnesiase: Gases seo2 SOL ov diss Beco sdiece cee ace eee ae ee eRe eee eee 1.82 Potashtandt Sod aie see eee ee a ee ae Sie Se late mye ela ee Bm ee pe ec R 2.32 Ro tallest parte Cerne eel Le ao Eke oan 2 Se eek a XO anak aie my ee Nee re ane eee 100.10 Mineralogical constitution—"'wo samples collected by the writer have been examined microscopically by R. D. Salisbury. One is from Beech Flats, in northwestern Pike County, Ohio; the other is from western Highland County, not far from the locality from which the sample subjected to chemical analysis was obtained. One is very near the glacial boundary, the other 15 or 20 miles back from the boundary. No essential difference was found in the samples. Both consist mainly of quartz grains, among which are feldspar fragments, hornblende, and possibly epidote and augite; there are also coarse grains of chert and minute concretions of iron oxide. The material is largely angular, even when the grains are of sufficient coarseness to have been liable to become rounded under favorable conditions. PROBABLE IOWAN AGE. Standing, as it does, above the Sangamon weathered zone and below the Wisconsin drift, the position of the silt is similar to that of the Iowan drift. ‘Vol. I, p. 445. Geet es AGE AND MODE OF DEPOSITION OF THE LOESS. 299 It is certain that the loess on the south border of the Iowan drift in eastern Towa and western Illinois is of the same age as that drift, for the two deposits connect completely at their borders. The loess sets in abruptly at the south border of the Iowan drift like an outwash from the Iowan ice sheet. The silt appears to hold the same stratigraphic position throughout its entire extent, and no reason has been found for excluding any part of it from the Iowan stage. It is not certain, and perhaps it is scarcely probable, that the deposit is everywhere an outwash from the Iowan ice sheet. But it seems to have been deposited at a single epoch of general lew altitude and slack drainage. Its wide distribution on the uplands may, however, be due immediately to the agency of winds. MODE OF DEPOSITION. The mode of deposition of the loess and associated silts has beer. and still remains one of the most puzzling problems of Pleistocene geology. At present little more can be done than to state the several hypotheses and discuss the difficulties of interpretation. This has been attempted by the writer in Monograph XX XVIII of this Survey, and but little can be added to that discussion. The leading hypotheses are known as the aqueous and the eolian. But as a portion of the deposit in southeastern Ohio has been attributed to organic agencies, that interpretation also should be considered. It is generally recognized that difficulties attend the application of any one hypothesis to the entire deposit. Probably no one questions the view that the influence of the wind has been important, and nearly all will concede that water, or at least imperfect drainage, has been influential. The division of opinion, therefore, is concerned with the relative importance of wind and water in the distribution of the loess. The question of the influence of the atmosphere as an agent of erosion, transportation, and sedimentation has been carefully examined and ably discussed by Udden, with the result of showing that it is competent to per- form as much work as is required in producing this deposit.2 Chamberlin has recently discussed the peculiarities of distribution and considered the 1See Edward Orton: Geology of Ohio, Vol. I, 1873, p. 445; also G. F. Wright: Bull. U.S. Geol. Sur- vey No. 58, 1890, p. 104. ?The main results of Udden’s investigations are presented in the following papers: Erosion, transportation, and sedimentation performed by the atmosphere: Jour. Geol., Vol. II, 1894, pp. 318-331; Loess as a land deposit: Bull. Geol. Soc. America, Vol. IX, 1897, pp. 6-9; The mechanical composition of wind deposits: Augustana Library Publications, No. 1, 1898, Lutheran Augustana Book Concern, Rock Island, Ill. 300 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. difficulties attending the application of either hypothesis to the entire deposit.? The adherents of the eolian hypothesis generally assume that drainage conditions were such that the dust accumulation exceeded the erosion of the land, but they object to the view that much of the surface was under water. The restriction of the deposit to a certain stage in the Glacial epoch is thought to affect in no way the applicability of this hypothesis so long as it is granted that there were exceptionally poor drainage conditions, it being thought that erosion is ordinarily more than a match for dust accu- mulations. They cite the presence of shells of land mollusks and the wide vertical distribution of the loess as fatal to the aqueous hypothesis. The adherents of the aqueous hypothesis, while recognizing the diffi- culties of accounting for the land mollusks and the wide vertical distribu- tion of loess, have emphasized the important fact that the thickest and most porous loess is distributed along the main valleys, and they maintain that its distribution was largely dependent upon the great streams of the region. They also have emphasized the occurrence of coarse material in places in the basal portion of the loess, and the occasional development of distinct beds of silt and also of sand that seem to be water laid. The close connection between the Iowan drift sheet and the loess deposits of eastern Iowa and western Illinois is recognized by the advocates of each hypothesis, and there seems to be unanimity of opinion that water was an important distributer there, though some difference of opinion exists as to the extent of its influence. In the region under discussion the variations in level are such as to put the aqueous hypothesis to severe test, for the silt deposits occur from an altitude 500 ‘feet or less above tide up to more than 1,000 feet. In southeastern Indiana this wide range is found within a space of but a few miles. The uplands ordinarily stand 200 feet or more above the surface of the drift accumulations in the main valleys, and nearly 400 feet above the main streams. To submerge this region it would seem necessary to assume a depression that would bring the uplands about to sea level and carry the valleys to a level far below tide, there being no apparent basis for the hypothesis of land barriers or other obstructions which could have held a wide body of water much above sea level. 1Supplementary hypothesis respecting the origin of the loess of the Mississippi Valley: Jour. Geol., Vol. V, 1897, pp. 795-802. ee MODE OF DEPOSITION OF THE LOESS. 301 That this region had an unfavorable altitude for drainage in the pre- ceding Sangamon interglacial stage, and probably stood much lower than at present, seems evident from the shallowness of the valleys which were opened on the surface of the Hlinoian drift. The drainage conditions seem to have become still more unfavorable during the silt deposition, so that erosion was either suspended or became so weak that it could not keep pace with deposition. This increased imperfection of drainage conditions seems best explained by a depression of the land. This being granted, there may be found but little occasion for dispute between the advocates of the eolian and the aqueous hypotheses, it being only necessary to decide whether or not depression stopped short of submergence. The pebbles and occasional sandy beds found in parts of this silt may help in deciding this question. The source of the material is a question of prime importance, but so far as the region under discussion is concerned it is largely undetermined. The part which covers the glacial drift seems from the examinations made by Salisbury to have been derived to some extent from glacial deposits, there being minerals present which abound in these deposits and are not present in neighboring rock formations; but the quartz which forms the ereat body of the silt may easily have been derived from various rock formations, near or remote, east, south, or west from the glaciated districts, and also from the drift. It remains to consider the influence of organic agencies, the view having been presented by Orton that the white clay of southwestern Ohio is merely the fine material brought up by burrowing animals, earthworms, etc., from the underlying till. This view was suggested before the relationship to the loess had been determined and before the underlying Sangamon weathered zone had been clearly recognized. While therefore the effectiveness of such agencies to produce deposits of considerable bulk is not questioned, the reference of this silt deposit to such agencies can scarcely be sustained. The disturbance produced by these organic agencies has not been suffi- ciently deep to greatly affect the buried Sangamon soil and weathered zone, there being, as indicated above, a clearly marked line separating the weath- ered surface of the Llinoian till sheet from the overlying silt. The inad- equacy of organic agencies to account for the surface silt becomes still more apparent when the great bulk of the silt farther west is considered, the thickness of the loess in parts of the Mississippi Valley being over 100 feet. CHAE Ee exe THE PEORIAN OR POST-LOESSIAL SOIL AND WEATHERED ZONE (TORONTO FORMATION?). The soil and weathered zone formed on the lowan till aud the loess and associated silts before the culmination of the Wisconsin stage of glaci- ation have been called the Peorian,* because of good exposures in the vicinity of Peoria, Ill, beneath the Shelbyville or earliest sheet of the Wisconsin series. The interval between the lowan and Wisconsin stages had previously been provisionally named Toronto by Chamberlin,’ because of excellent exposures of interglacial fossiliferous beds along the Don Valley in Toronto, Ontario, which were at first thought to be of this age. Chamberlin remarks, in connection with the introduction of this name, that the grounds for the correlation are not very strong, and that further investi- gation may show them to be erroneous. In view of the uncertainty attached to this correlation it has seemed advisable to employ for the present a sub- stitutional name which is known to be applicable to the interval between the Iowan and the early Wisconsin. In case the correlation suggested by. Chamberlin is demonstrated to be correct the name Toronto has precedence. The evidence of this interglacial interval is found not only in the formation of a soil and leached horizon at the top of the loess, but also im a great change in the outline of the ice sheet in the succeeding or Wisconsin glaciation from that displayed in the preceding or Iowan glaciation. There was also a marked change in the attitude of the land, the conditions for drainage being decidedly better in the Wisconsin than in the Iowan stage of glaciation. These several lines of evidence are well shown in the region covered by the Illinois glacial lobe, and are discussed in Monograph XXXVIII. ‘The Peorian soil and weathered zone (Toronto formation?), by Frank Leverett: Jour. Geol., Vol. VI, 1898, pp. 244-249; see also Mon. U. 8. Geol. Survey, Vol. XX XVIII, 1899, pp. 185-190. * Classification of American glacial deposits, by T. C. Chamberlin: Jour. Geoi., Vol. ITI, 1895, pp. 270-277. 302 PEORIAN INTERGLACIAL EPOCH. 303 In the region under discussion the Iowan drift has not been found outside _ the Wisconsin, and nothing is known concerning the outline of the Iowan drift border. The other lines of evidence are, however, about as clearly shown in this region as im that covered by the Illinois glacial lobe. A comparison of the weathering and erosion on the silt with that on the earliest moraine and drift sheet of the Wisconsin series shows a perceptibly greater change in the silt than has been effected in the surface of the Wisconsin drift; but here, as in the Illinois lobe, the interval appears less prolonged than the Sangamon interglacial stage. It was remarked in Monograph XXXVIII, in the discussion of this interval, that the weathering appears to indicate that it is comparatively brief, but that the change in the outline of the ice sheet and in the attitude of the land may call for more time between the Iowan and Wisconsin stages of glaciation than the weathering seems to require. It should also be remembered that the Toronto formation has furnished decisive evidence of a prolonged interglacial interval.’ Should it be proved to represent the interval between the Iowan and Wisconsin deposits its testimony should outweigh any inferences of a brief interval drawn from a comparison of the weathering of the two deposits. 1See descriptions by Dr. A. P. Coleman and Prof. D. P. Penhallow: Am. Geologist, Vol. XIII, 1894, pp. 85-95; see also additional interpretation by Dr. Coleman: Jour. Geol., Vol. III, pp. 274, 622-645. CHAPTER X. THE EARLY WISCONSIN DRIFT. © GENERAL STATEMENT. In the Wisconsin stage of glaciation there were several glacial lobes occupying the basins now covered by the Great Lakes and extending beyond them into the lowlands that are connected with the southern borders of the lake basins. These lobes were brought to notice and named by Chamberlin.1 Those included in the region under discussion are the Miami, Scioto, and Grand River lobes, named from the drainage basins in which they were situated, and their successor, the Maumee-Erie lobe, which occupied the Maumee and Lake Erie basins. The East White lobe is not included, since it falls naturally into a report, now in preparation, which covers the Wisconsin drift of central and northern Indiana and the southern peninsula of Michigan. Although the several glacial lobes form somewhat distinct areas they are discussed together, each morainic belt being traced so far as possible through the several lobes. The lake history, although closely interwoven with the withdrawal of the Maumee-Erie lobe, is taken up after the discus- sion of the moraines of that lobe. SECTION I. EARLY WISCONSIN DRIFT OF THE MIAMI LOBE. THE OUTER OR HARTWELL MORAINE. DISTRIBUTION. The Hartwell moraine receives its name from the village of Hartwell, Ohio, which stands at the extreme end of the morainic loop, in Mill Creek Valley, a few miles north of Cincinnati. The general course of the moraine may be seen by reference to Pl. XI. From Hartwell it leads northeast- ward, leaving Mill Creek Valley at Sharonville, and rising to elevated land 1 Preliminary report on the terminal moraine of the second Glacial epoch, by T. C. Chamberlin: Third Ann. Rept. U. 8. Geol. Survey, 1883, pp. 291-402. 304 MONOGRAPHXLI PL.X!I LEGEND RQ Tilinoian drift Orrin SMEET SHORE, > —— Maun rS) Plane surface drift x Bowling (ren ] Ren snote ! RAEN SN ec. ‘ gl: Heston: Old lake bottom ER ENC 26 BARTHOLOMEW 27 DECATUR 28 FRANKLIN 29 DEARBORN 30 RIPLEY 31 JENNINGS OHIO Sh JUUUS BIEN & CO. LITH NY. MAP OF THE MAUMEE-MIAMI GLACIAL I OBE BY FRANK LEVERETT ee ee ee re . OUTER MORAINE OF THE MIAMI LOBE. 305 near Pisgah. From Pisgah it passes down into Turtle Creek Valley just above its junction with the Little Miami Valley near Kings Mills. It then crosses a high tract south of Lebanon and comes to the Little Miami Valley below Waynesville. Near this village it connects with the outer or Cuba moraine of the Scioto lobe. From the junction of the Hartwell with the Cuba moraine there extends northward along the borders of the Little Miami Valley, across Greene County, a system of morainic ridges which may constitute an interlobate belt of the same age as the moraine. Farther north, in Champaign and Clark counties (see Pl. II), there are drift ridges which are perhaps of more recent date than this moraine, yet. older than the outer moraine of the late Wis- consin series. They accordingly seem referable to the early Wisconsin drift, and are discussed in connection with the Hartwell moraine. They lie mainly east of Mad River, and occupy a belt extending from that river eastward several miles. At the north, near the border of Champaign and Logan counties, they are overridden by a moraine of late Wisconsin age. The moraine curves abruptly northwestward from Hartwell, and follows the southwest border of the Mill Creek lowland tract to the Great Miami River below Hamilton, there being a series of low knolls and ridges of drift along this route, while the uplands to the south have a plane-surfaced drift, probably Hlinoian, and a coating of loess-like silt. In the Great Miami Valley fresh-looking drift and sharply morainiec features appear near New Baltimore (Sater post-office), and a belt of morainie type leads westward from there to New Haven (Preston post-office). There are feeble morainic features between New Haven and Philanthropy, but the prominent hills and large valleys of preglacial age are so much larger that the morainic swells are rendered inconspicuous by the contrast. The drift in eastern Hamilton and ‘southwestern Butler counties failed to fill the valleys or even to modify greatly the preglacial drainage, though there is much more drift and the knolls are sharper in the valleys than on the uplands. The moraine enters Indiana near Philanthropy (Scipio post-office), having conspicuous features just south of the village. Its course in Franklin County, Ind., is northwestward through Mount Carmel to Kast Whitewater River, which it crosses north of Brookville just above its mouth. The moraine here swings toward the north, following the west side of the river into Fayette County and widening near the latitude of Connersville to cover 20 MON XLI 306 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. nearly the whole tract between the two Whitewater rivers. From Conners- ville northward it is closely associated with the outer moraine of the East White River lobe, and the combined moraines occupy the western half of Wayne County. In northern Wayne County these moraines are overridden by a later one and their northward continuation is completely concealed. It is scarcely probable, however, that they extended farther north than — the summit of the highland tract in Wayne and Randolph counties, for it seems natural that the Miami and Hast White River lobes would have completely coalesced in the low country to the north of these highlands. Wayne County presents features to which it is necessary to direct especial attention, otherwise there may be a misunderstanding of the inter- pretation concerning the course of the moraine. The western part of the county is traversed by a series of large ridges and broad valleys, trending north-northeast to south-southwest, the height of the ridges being 75 to 125 feet and their breadth several miles, while the valleys present a usual breadth of about one mile. The drift, as a rule, has considerable depth, both on the ridges and in the valleys. On the ridges or uplands the wells indicate that the rock surface is generally as low as in the valleys, and so far as collected, the evidence all favors the view that the relief of the ridges is due rather to drift accumulation than to rock substrata. But it is scarcely probable that it was the last ice invasion which deter- mined the main outlines. The course of the moraine under discussion is such as to carry it into the valleys as well as over the ridges of the western part of Wayne County, yet it scarcely touches either a large ridge in the east-central part that lies between East Fork and Nolands Fork, or the uplands west of the West Fork of Whitewater River. There seems little doubt, therefore, that these reliefs are referable to pre-Wisconsin agencies. This determination raises the double. question, whether the earlier ice invasion produced the succession of ridges and valleys here displayed or whether it produced a plane-surfaced deposit which was carved into ridges and valleys by the streams which drained this district in the Sangamon or the Peorian or both of these interglacial stages preceding the Wisconsin glaciation. The contours of these ridges and valleys apparently support the view that the drift surface as left by the ice was nearly plane, and that a large amount of sculpturing was accomplished in the merelaeial stages just mentioned. OUTER MORAINE OF THE MIAMI LOBE. 307 RELIEF. The highest points along the crest attain an altitude of perhaps 50 feet, while the sags and lower parts of the moraine stand but 10 to 20 feet above the outer border district. The average relief is estimated to be about 30 feet. On the inner border it is even less, there being a sheet of drift con- nected with the moraine which reduces its relief on that border to but 10 to 20 feet. RANGE IN ALTITUDE. The range in altitude depends largely upon the differences in the level of the underlying surface. The effect of the drift accumulation has been to reduce rather than to increase the inequalities of surface, many of the pre- glacial valleys being deeply filled with drift while the neighboring ridges are thinly coated by it. For example: In Mill Creek Valley, at Lockland, where the moraine has almost its lowest altitude, the entire drift, older and newer, has a depth of about 180 feet below the level of the creek; but on the upland ridges its depth is seldom over 50 feet and often is so slight that shallow wells and cisterns reach the rock. However, in Fayette, Wayne, and Randolph counties, Indiana, there is (including the earlier or Ilinoian drift) 100 feet or more of drift on the uplands. The following table indicates approximately the range in altitude, though possibly portions of the uplands contain higher points than appear in the table. It includes altitudes along ridges in the reentrants between the lobes: Altitudes along the outer moraine of the Miami lobe. Feet above tide. lebeinevacls iim bese Ctopmniny, loo 4-506 552 5o- seed sas ae one esse osessscesosesusces 1, 200-1, 500 INearaWestilaberbysrommuplandsiaas22- ac secinisicine = Cociine seine = Sepese nce gees se ee sere 1, 200-1, 300 Near WiestelabertyinMadmhiver Valley S222 252222 ce uae is oie nee SE eee 1, 100 DEsGOr mom, Cm walk. sso s- sass seeaSa aes ee eo Bee aE Soe eeHaS sae ese Soe se soos. 1, 050-1, 100 Springfield, on moraine, near Standpipe, about -...--.---.---------------------------- 1, 075 Wiestrolavellowspnrinosaen eee ctysat se seat swaths ONS chy eeu at Sac eterna ele tepals 1, 000-1, 025 WYGSE- Ol Gila 6 Soe Seisc So oes e ed eso ss oe ee ae AOE ne Cane ae orem ee meee se oS aeee 940-975 lin sjoninee Wallis odes Soc cea aokbose SoBe ses soe cre aa ee ree Sonoma se beeaee stances esssne se 760-825 Eg or WaymeswilllOs. .24- cossbaueuesee saaenso see ane bp apodsoosuaaeemborseesbeSes soso" 875-900 SON CLA MING = od sod ccaodebeae oben s Suess a Sean sees ee eseer ose Se obeAmece SSaaee 875-900 Northwest of Deerfield, in Turtle Creek Valley.........-..---------------------------- 675-725 Multomponiandayicinlitvapeerreseecesise o/s seacee see kee ae- nee see e eee esas 900-925 Pisgah (highest point in village) about.............-..-..----.----------------------- 960 Mill Creek Valley, between Sharonville and Hartwell ......-.---.---.----------------- 570-600 Between Mill Creek and Great Miami River, about....-...---------------------------- 750 owlandetract soubmwest olVenice, abouties--sss--52- sess cceeeeee seas ce seeesceem ese. 600 308 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Feet above tide. Wikororatt: Chrmaavell, UinGl,, Mow -so2ce Hsonse bse n soos ease bosaSescusseeaesss=sczosecssosoeed 1, 020 Summit on Brookville and Connersyille Pike, near tollgate, 4 miles from Brookville (ammo) Sok oceeeoteSeaoesossss25555e 35 see o eee Eman oem seSseessonaa] Sosnacscac4 1, 050 Alguina, about.........-..----------------------------------------+ 2-2-2522 -22-22--- 1, 025 Whitewater Valley at Connersville. -..-.-....---------------------------------------- 850 Haryeys station (in valley of Martindale Fork) ---..-.--------------------------------- 958 Moraine) bill Sfeastrot ble yey sess ee eee eee 1, 065 Highlands of northern Wayne and southern Randolph counties. ------------- Mes Leone 1, 200-1, 250 The range in altitude between Mill Creek Valley and the highlands of Logan County is, therefore, nearly 1,000 feet. The range in the altitude of the rock surface slightly exceeds 1,000 feet, the altitude being less than 400 feet in Miil Creek Valley, and fully 1,400 feet m Logan County, near Bellefontaine. TOPOGRAPHY. The moraine has, as a rule, a gently undulating surface, but as its features vary from place to place a detailed description will be given, beginning in southern Logan County, Ohio, where moraines of early Wisconsin age first come into view outside the later ones, the moraine is carried thence south and west Sharp ridges with north-south trend, separated by narrow gravel plains, appear in southern Logan and northern Champaign counties. ‘There are two of these ridges in southern Logan County, and a third one sets in in northern Champaign County, which at its northern end lies west of the others, but which, owing to the disappearance of the other ridges, becomes within 2 to 3 miles to the south the outermost and main ridge. These ridges are of variable height and stand 20 to 100 feet above the bordering gravel plains. Farther south, in the vicinity of Kings Creek, the ridging becomes less sharp and the moraine consists mainly of low knolls 10 to 25 feet high, though it includes occasional larger ones 50 to 75 feet in height. From Kings Creek southward to Springfield it is spread out over a breadth of about 3 miles, while north from that creek the united breadth of the ridges would scarcely amount to 2 miles. With increase of breadth there comes a softening of contour, and much of this portion of the moraine consists of swells only 10 to 20 feet high, among which are numerous shallow basins. Near the eastern border of the moraine, and apparently connected with a gravel plain lying outside (east) of it, there are irregular sags and depressions, formed perhaps by the escape of water from beneath the ice sheet. In the midst of the gravel plain there are occasional drift OUTER MORAINE OF THE MIAMI LOBE. 309 knolls rising, in some instances, 40 to 50 feet above the surface. Whether they are the product of this lobe or of the Scioto lobe was not determined. Within the city of Springfield morainic features are developed, a well- defined ridge passing the standpipe and thence southwestward through the southeastern part of the city. There is a distinct ridging in a northeast- southwest direction, and along the crests and slopes are knolls 15 to 30 feet in height. The moraine loses much of its ‘strength in the southern part of Springfield Township, though numerous gravel knolls extend toward Selma. From Springfield Township southwestward to the Little Miami River there is a gently undulating till tract, dotted with occasional gravelly knolls, but not a well-defined moraine. A conspicuous group of knolls occurs near the county line about 2 miles northwest of Yellow Springs, the most promi- nent knoll (Polhemus Hill) standing nearly 75 feet above the bordering country. This knoll is elliptical, with a northwest-southeast direction, having a length of about one-fourth and a width of one-eighth mile. Other knoils in its vicinity are 15 to 25 feet in height and of sharp contour. Just west of Yellow Springs is an elliptical knoll with north-south trend which rises about 30 feet above the bordering country. It is 40 to 50 rods in leneth and 20 to 25 rods in width. On the north bluff of Little Miami River, near the line of Beaver Creek and Xenia townships, there is a prom- inent knoll at least 75 feet in height. Toward the west, between this hill and Beaver Creek Valley, the undulations are sharper than to the north and the topography again appears morainic. Sharp gravelly knolls and ridges 15 to 30 feet high are common, and occasionally an esker-like linear gravel ridge is found among the knolls; till swells with gentle slopes also occur. North of Xenia, between Wilberforce and the Little Miami River, there are several other sharp gravelly knolls 20 to 50 feet high. East and south from Xenia for several miles there is only a gently undulating till tract. West of Xenia, at the west side of a gravel plain known locally as “Cherry Bottoms,” several prominent knolls form a group about one-half mile long from north to south and one-fourth mile from east to west. The highest points are 50 to 60 feet above the plain. Knolls are numerous south and west from this group, but they are only 10 te 20 feet high. East, south, and north from Spring Valley the drift on the uplands consists of gravelly or sandy knolls and ridges 20 to 25 feet in height which wind and interlock in morainic fashion. This seems to be an interlobate tract of the same age 310 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. as the Hartwell moraine. It is probable that for 5 or 6 miles south from Spring Valley the Miami portion of the interlobate moraine lies between Czesars Creek and the Little Miami River, while the Scioto portion les east of the creek, the position of the creek being determined to some degree by this relation to the ice lobes. East and south of Lebanon low swells occur on the slopes of the pre- glacial ridges and in valleys or lowland tracts, but the moraine is rather inconspicuous. It is strikingly in contrast with the neighbormg portion in Turtle Creek Valley, which for about 3 miles above the mouth of the creek has so many sharp swells and gravel knolls that the valley is nearly filled. The highest are but 40 to 50 feet, and many are only 15 to 20 feet in height, but they are closely aggregated and constitute a noticeable feature. They have forms independent of the drainage, present or past, and connect here and there in the irregular and peculiar manner common to moraines. About 3 miles above the mouth of Turtle Creek the valley becomes free from knolls and contains a broad, swampy lowland plain about a mile in width. This plain passes northwest into the Great Miami drainage basin, the lower course of Dicks Creek, a tributary of the Great Miami, lying in it. The freedom from knolls gives this portion of the valley or lowland strong contrast with the portion occupied by the moraine. This lowland tract, which was first discussed by Orton in a report of the Ohio geological survey,! appears to be a line of preglacial drainage, as noted in Chapter HI. On the upland tract between the Little Miami River and Mill Creek, in southwestern Warren, southeastern Butler, and northern Hamilton coun- ties, no very prominent knolls were observed, but the surface has many swells with gentle slope, and the drift is sufficiently heavy to greatly mask the preglacial valleys and ridges. In the vicinity of Pisgah the drift has unusual thickness as well as altitude, and there are knolls of morainie type 10 to 20 feet in height. They cover but an acre or two each. Such drift knolls continue down the slope into Mill Creek Valley at Sharonville. West of Pisgah, in the vicinity of Westchester, there are some larger drift knolls. One just west of the Cleveland, Columbus, Cincinnati and St. Louis Railway and north of the Westchester and Pisgah wagon road is 60 feet or more in height. It is in a lowland tract, as are nearly all the other prominent knolls near Westchester. 1 Geology of Ohio, Vol. III, 1878, pp. 381-382. OUTER MORAINE OF THE MIAMI LOBE. 311 Mill Creek Valley between Sharonville and Hartwell contains many morainic swells, the highest of which stand probably 30 feet above the general level of the valley, but the majority only 10 to 15 feet, perhaps less. At Reading the drift surface consists of winding ridges of gravel, 20 feet or more high, but directly west, in Wyoming and Lockland, it consists in the main of conical swells of till 10 to 30 feet high, but few of which are abrupt or sufficiently prominent to be worthy of notice. Notwith- standing their inconspicuousness when contrasted with the bluffs and hills bordering Mill Creek Valley, these knolls constitute a marked feature when Mill Creek Valley alone is taken into account. South of Hartwell and also north of Sharonville the valley has a smooth plain from bluff to bluff, aside from some low hills southeast of Glendale, which have a rock nucleus. Much of it above Sharonville is a marshy tract so level that it has been difficult to drain, and a portion of it has been converted into ice ponds. South of Sharonville, where the moraine appears, the valley bottom is undulatory, affording beautiful sites for the Cincinnati suburbs from Wyo- ming to Hartwell. South of Hartwell the valley is again free from drift knolls, and continues so to its mouth at Cincinnati. The knolls between Hartwell and Sharonville, like those in Turtle Creek Valley, appear to be in no way dependent upon the present drainage for their form, but, like morainic swells on the uplands, they present a topography readily distin- ouishable from the drainage erosion type. The drift west of the Great Miami, between New Baltimore and Venice Gn the lowland tract mapped by Orton as an old valley),* has a swell-and-sag till topography. The undulations are slight, seldom reaching a height of 20 feet. The surface is bowlder strewn, and is not coated by a sheet of silt such as occurs farther south and west. A short distance southwest of New Haven (Preston post-office) the hills set in, and again it is difficult to dis- tinguish a morainic belt, though knolls occur on the lowlands. It may be remarked in passing that drift knolls are not often seen in the lowlands south of this moraine, either in Ohio or in Indiana. South of Philanthropy, near the State line of Ohio and Indiana and on the west side of Dry Fork, is the most prominent drift aggregation in this part of the morainic belt. It consists of a ridge of gravel, 500 yards or more in length and about 200 yards in width, trending northeast to southwest and standing 30 to 50 feet 1 Geology of Ohio, Vol. I, 1871, p.419. Map of Hamilton County. 312 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. above the surrounding country. Several small knolls, also gravelly, are connected with it at the sides. Between this prominent knoll and the East Whitewater River there are on the uplands low till swells 5 to 10 feet high, while knolls of gravel 10 to 20 feet high characterize the drift in the valleys and on their slopes. West of East Whitewater, on the uplands immediately north of Brookville and about 3 miles from the city, there are both till and gravel knolls, the largest having a height of about 20 feet. The knolls are in several instances elliptical, but there appears to -be no uniformity of trend. On the inner border plain north from these knolls, in Franklin County, few knolls occur that are as much as 10 feet in height. In southeastern Fayette County the surface is very uneven, there being ridges and dry valleys which are apparently partially masked interglacial drainage features. In various positions in these valleys and on the ridges and slopes, swells 10 to 20 feet high occur, many of which are gravelly. In north- eastern Fayette County and im Wayne County there are few knolls that rise to a height of more than 10 to 15 feet, the only prominent exception noted being a group in the vicinity of Doddridges Chapel, Washington Township, Wayne County, whose highest members have a height of 40 to 50 feet. In northern Wayne County abrupt knolls 30 to 40 feet in height are common, but it is probable that these belong to a later morainic belt which crosses northern Wayne and northeastern Henry County in an east- west direction. STRUCTURE AND THICKNESS OF DRIFT. The soil of this moraine is strikingly in contrast with that of the tract south of it. It is usually dark colored and loamy, with an admixture of pebbles and sand, while that outside is a light-colored clay or silt with scarcely a trace of sand and pebbles. In the morainic tract there are also bowlders on the surface on upland tracts as well as along streams, but in the outer border district none occur at the surface except along valleys or on slopes where drainage erosion has carried away the silt or surface deposits that had covered them. Throughout its entire course this moraine consists mainly of till, but is characterized by occasional gravelly knolls among the till swells. The gravel knolls are especially frequent where the moraine crosses valleys, beg present in nearly every good-sized valley within the morainic belt, OUTER MORAINE OF THE MIAMI LOBE. 313 but they occur also on the uplands. A good illustration of such knolls in the latter situation may be found on the elevated tract north of Brookville, Ind., at an altitude 400 feet above the Whitewater Valley. Here two gravel knolls were observed, each about 20 feet in height, standing in the midst of the till swells of the moraine and in no way connected with drain- age lines. Having considered the question whether those which occur in the valleys may not have been sculptured into their present forms by post- glacial drainage erosion, the writer is convinced that their origin is inde- pendent of the present streams. They were neither deposited by them nor are they remnants left by erosion. They usually present the hummocky irregular surface characteristic of morainic deposits. Only the knolls, how- ever, are composed largely of assorted material, the low-lying tracts among them, as shown by well borings, being frequently underlain by till. We may now pass to a more detailed description of the noteworthy illustrations of drift structure and thickness. The discussion begins with the tract in the Scioto-Miami reentrant angle. At West Liberty, Ohio, in the valley of Mad River, a gas well pene- trated 216 feet of drift, largely sand and gravel, while in the same valley 13 miles east there are exposures of limestone along Mackocheek Creek at about the altitude of West Liberty, and ledges still farther east rise to a height of 100 feet above the village, or 1,200 feet above tide. Wells are often obtained at 25 to 50 feet on the morainic ridges, after penetrating a stony till. Several deep wells have been made in the vicinity of Urbana, of which the following tabulated records were furnished by T. F. Moses, formerly of that city: Table of wells near Urbana. Naame, Altitude Depth of above tide. drift. Feet. | Feet. plan enyawelleeter sats ia Sank yce ie ese noe eee case eenke selec sce emeee se | 1, 044 | 150 ROGIER WG kes SP Bee S8 Secs SSG ERR net ca ae te ctes aeeey eeyer Cee | 1, 001 | 133 Giluetiactonyswellipe me exet seerse sae ke ewe cee ae MUU es ee ea sues 1, 020 | 102 SVCAM OLE We ll assesses aes Sais SoS alad Skies Selene sac Seeisa a see Serieeisee 1,000 | 150 Citizens te Nom Rememem men ee tate inn ah TE DRT TE ee is ees Ce aoe Ca i aln(ail | 150 314 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Dr. Moses furnished the following section of the drift in the tannery well, but of the others no record of drift structure was kept: Section of drift in the tannery well at Urbana. Feet, SOUVSulbsoll ete eee eens ates cae ieee a a Neh See Ay Ce ae a ee Re 10 Gravelland? sain dtiaet syanted tkoe eae OS hes Hoe ere aoe oe a ce ee ees See dl Sees e ser 35 Biueyclaya (pebble eee e See we as Soseeee JAN, Feet fStolligumval selllonyjorelo oh Glenyi(uill))| So soso saccee sees aee ose paee eee sees Gh ek Kees al 10-15 Bliektillnotwenveharememersne mene Tem Anse aa eae mes Tre eee In etree mee Arner eunael 20-30 Sand bed containing water. On the east bluff of Mill Creek, east of Sharonville, J. P. T. Miller’s well penetrated about 40 feet of cemented gravel, and there are outcrops of cemented gravel in the ravines in that vicinity. It is not improbable that this may belong to the earlier drift sheet, though located in the moraine, since in that vicinity the moraine appears to consist of but a thin sheet of drift. Records of several deep borings along Mill Creek Valley—that is, the old valley of the Ohio River—are introduced here. Some of these belong to the tract lying north of this moraine. They serve to show how greatly 318 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the glacial drift has softened the outlines of this still rather broken region by filling up its valleys. The list of borings begins at the northern end of Mill Creek Valley, where it joins the Great Miami Valley, and includes a few wells in the latter valley. At Hamilton a prospect boring for gas penetrated, 210 feet of drift, which was nearly all gravel and sand, striking rock at an altitude of about 390 feet above tide, or 42 feet below low water in the Ohio at Cincinnati. A well at Snyder’s paper mill, in the eastern part of Hamilton, penetrated a bed of bowlder clay beneath the gravel, as follows: Section of well at Snyder's paper mill, Hamilton, Ohio. Feet GWEN ss Secscc cogs eacnel Gee eeokps cose ee nee Saou see saree aber sesnsnUse acme csScccsercoueess 80 Tellin loowwieler Clay... --. 2522255422 sa sseosecessssccnesess sees sseseS sess ss0ossosscssasesess 20 Gimnyell Wess decesossos clauses Hees he eae owes ue aero res men oeceensesceqersg.cseccdi causes 20 Wolo oes eased awe anoe esas eceqosobeaedpEeroane cescncocscndeeracnossSos cues 120 A well at the Franklin paper mill in the southern part of Hamilton penetrated a blue, pebbleless clay near the bottom, as shown by the following section: Section of well at Franklin paper mill, Hamilton, Ohio. Feet (Clojoisile aiantl atmn@l.. 2 2 sce esas scones esesosas ss oS SscesSs e225 58025es55ccesaeeseresscsesce: 25-30 ine wamyell wattle S@MNe SHG. -2ossesces sags sese52 258s 5 5520255552525 so ses ssescsasaecesses 50 Ble clay witlmowtt joel oles... .- 22 sscossessecssonsassssossessseossessseee Pee SSR Aah A ae, 25 Sand at bottom. Dejade of welll... 2.0222 22eossseeseosere ssee2ee22 2252255522522 5se2esaceeescecscerer¢ 102 Wells in the Great Miami Valley 5 to 6 miles below Hamilton, near the mouth of Indian Creek, strike a black muck under the gravels of the glacial terrace at a depth of 60 to 65 feet, the altitude at the well mouths being about 40 feet above the river. This black muck probably separates gravel of Wisconsin age from earlier deposits. The exposures in Mill Creek Valley, from the border of the gravel plain on the Miami River near Hamiiton to the border of the moraine near Read- ing, are quite uniformly till, or deposits such as would be produced by glacial action, and differ markedly from the gravel deposits that follow the Great Miami and Ohio rivers. Three miles southeast from Hamilton, in the lowland tract near the canal, a gardener, Joseph Federlee, made a well 110 feet deep which did not strike rock. The drift consists mainly of a blue, OUTER MORAINE OF THE MIAMI LOBE. 319 pebbly clay. This well is scarcely one-fourth mile south of the bluff or upland north of the valley, in which rock rises 100 feet or more above the level of the well mouth. A small gravel knoll directly across the highway from Federlee’s residence has been opened and shows caleareous sand and gravel containing many limestone pebbles in arching beds. A mile or more east of this place the Panhandle Railway makes a slight cutting, in which are exposed— Railway cutting in Mill Creek Valley. Feet WAS o Ny os a eS ae Oi aes een et RS a Ray DR Eee eee 6-8 Eonizontallysbeddediny ellowasan diese ae aes eae Seo MS Se los Ie a IE ace peyne bea 5-6 Blue sandy till at base. Such knolls are rare and much of the valley is very level, but these few knolls, taken in connection with the well sections, indicate that there is very little true alluvium in the valley, and that here, as well as farther south in the moraine, the filling is of glacial origin. The deposits are cer- tainly not fluvial. At a blacksmith shop in Port Union a well 36 feet deep gave the following section: Section of well at a blacksmith shop in Port Union, Ohio. Feet sViellowmpebbly clay mastine ea eames Se Sethe ee Ok Oe bee oe ae Sage Se Ste 12 IG GEN RRs So GuEIR Aan G5 ae Satan SMEAR eAOS AE ree ore ee ae ae Ae ee ys ai Ora eto ee ee 15 Blue Pprayacand ecaving bad yee ses whet cence kes sae Mato ee ou eS ee Ses Genoese See eee eenS ardabluempeb bliviclayeassecy free ance ciet e Ael cine (Ss sea See Nace ac an sete aes Soames cece aeeie 7-8 Sand and water at bottom. In Rialto, at a paper mill beside the canal, only a few rods from the west bluff of Mill Creek Valley, a well over 100 feet deep and several others 90 feet deep did not reach the bottom of the drift. In all of these wells the greater part of the drift is reported to be blue clay, the sand and gravel being interstratified in thin beds. Stones were frequently encoun- tered, making it difficult to drive the wells. In one well they were so numerous at a depth of 90 feet that the boring was abandoned. North of the Rialto station, a few rods east of this paper mill and farther from the bluff, is a cutting 10 feet in depth, which exposes yellow till with blue till at the base. The upper portion of the till, to a depth of 25 to 3 feet,. contains fewer pebbles than that in the lower portion of the exposure. In the till are many small blocks of limestone, such as find outcrop on the borders of the valley, and these are but little waterworn, while many are striated. 320 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. A mile or more east of Rialto, near the east side of the valley, is a well about 35 feet deep located on a knoll perhaps 15 feet in height. It passed through assorted material in its upper part, but the lower part penetrated blue pebbly clay. In Sharonville wells penetrate about 20 feet of till, and at that depth obtain water from gravel. On Mr. Ferris’s farm, 13 miles west of Sharon- ville, on the west side of the canal, a well penetrated the following beds: Section of Ferris well near Sharonville, Ohio. Feet, Yellow and blue clay, thought by the well diggers to have contained pebbles (dug)---.---.---- 61 Snel ovorxstal, yahilon SionGilll Ayyev~eNO)) Bo Sasa ocanos soos Soule SSE esaecosse0DesocU sss soasassesesoososs 16 ANoiGl lhe Soe ee eRe eC ae ae Memes br eee Saree ora uc ad copa SaDaeoSeakesfouKS 77 On J. Brown’s farm, 1 mile southeast of Sharonville, wood was encountered in blue till at a depth of 20 to 40 feet. At the gas-well boring in Lockland, in the valley of West Mill Creek, the surface being fully 30 feet lower than the upper lock in Lockland, or about 546 feet above tide, drift was penetrated to a depth of 190 feet, showing the rock floor of the valley to be but 356 feet above tide. ‘This, so far as known to the writer, is the lowest altitude of rock floor yet found in the valley. The exact section was not recorded, but Mr. Latty, of Lockland, who was inter- ested in sinking the well, made the following statement from memory: Section of drift in a gas boring at Lockland, Ohio. Feet. /Sillinyiltien sc eae s Oe eG r One ee eae aes en ene Masher ot tanaGh acinbraoopa lh oaaaod 8 GranGlascactssdodbue Csesadse sae ee SEE ene Soe Eee ae eer Ses eae okocaecsesetce sa scassaguses 12 Bina: pelo ohy Clay. socbadaec sco okoeseousssceseaodoscousonebasasneks jasednodscaarsubcespcodes 22 Alternations of sand, gravel, and blue clay, in beds each but a few feet thicket pte pees ee were 148 Potalidmnititiss eer eeeiss cece Die 22 pepe Sa teeth Ace ne eee eee eee es 190 At Stearns and Foster’s cotton mill in Lockland, near the upper lock, a well whose surface is 565 feet above tide is 147 feet in depth, and did not reach rock, but terminated m sand beneath a thick bed of blue clay. At Wyoming the city well (whose mouth stands 600 feet above tide) pene- trated 155 feet of drift without reaching rock, there beg yellow and blue clay, gravel, and bowlders in the upper 84 feet, and sand in the remaining 71 feet. A short distance south of Wyoming and Lockland, on the west side of Mill Creek Valley, the Cincinnati, Hamilton and Dayton Railway was, at the time of a visit in October, 1889, making a cutting for a switch between OUTER MORAINE OF THE MIAMI LOBE. o21 its main line and a starch factory east of the railway. The cutting passes through a till knoll about 30 feet high. Yellow till covers the knoll like a blanket to a depth of about 12 feet. The till is soft and has no silty covering. Below it is a dark-blue till, also soft, having pebbles very irreg- ularly distributed, bemg thickly set im places, but in other places nearly free from them. Where pebbles are wanting the material has the appear- ance of a very fine, laminated, sandy clay. In the deeper part of the cutting some coarser sand of yellowish color is exposed. Large pieces of wood were embedded in the blue till at a depth of 30 feet beneath the highest part of the knoll. The largest piece observed was about a foot in diameter and 3 to 4 feet long. It was very soft and so spongy that a spade could be pushed into it readily. One large piece, several inches in diameter, had a curled grain and an irregular surface and appeared to be a root. John Bonsall Porter, formerly engineer of the Glendale waterworks, informed the writer that several of the suburbs of Cincinnati have obtained a public water supply by sinking tubular wells in Mill Creek Valley. These wells ordinarily penetrate 75 to 150 feet of blue clay, largely glacial, beneath which is sand and fine gravel, which has been penetrated in some cases 100 feet without entering rock. From this sand, which Porter regards as the deposit of an old river, an unlimited supply of good water is obtained. The wells at the Glendale plant, in the center of Mill Creek Valley, 2 miles from the village, pass through 97 feet of “drift and alluvium,” then strike coarse sand of dark color, which in one case was penetrated 78 feet without reaching rock. The altitude at the bottom of the deepest well is only 395 feet above tide, or about 40 feet below the low- water level of the Ohio at Cincinnati. The water stands in the wells at about 560 feet above tide, or practically at the surface. Other villages using wells of this class at the time this communication was received (June, 1895) are Wyoming, Hartwell, Reading, Carthage, St. Bernard, Norwood, Linwood, and Madisonville. The last five lie outside the limits of this moraine. The wells at Norwood reach a depth of 235 feet, but those at other villages fall below 200 feet. Whether the sand found in the lower part of these wells is strictly alluvial and earlier than the glacial deposits, or whether its deposition resulted in some way from the ice invasion, can not perhaps be decided at present. It may perhaps be difficult to determine how much of the drift in Mill 21 MON XLI 322 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Creek Valley should be referred to the Wisconsin stage of glaciation. It seems probable, however, that it should be only a small part. It may include only the fresh-looking surface till, such as is exposed in the railway cutting, and may extend but little below the level of the flat part of the valley. Along the Great Miami River there is a gravel-filled valley three- fourths to 14 miles in width, of which the upper 60 feet of filling, as noted above, seems referable to the Wisconsin outwash. West of this valley the uplands in Hamilton and Butler counties, Ohio, carry a thin sheet of drift, but the lowlands and larger valleys carry a very thick deposit. The low- land tract connecting the Great Miami with Whitewater River, in northwest- ern Hamilton County, though utilized probably as a preglacial and possibly an interglacial drainage line, seems not to have been thus used since the Wisconsin ice invasion Like the valley of Mill Creek, it has been filled chiefly with till. A well in this lowland, at Mr. Guest’s, about a mile east of Preston post-office, passed through 90 feet of till and, at bottom, 10 feet of sand before obtaining water. The well surface is about 70 feet above the bed of Dry Fork at Preston. Ordinarily wells in this till tract find water at 40 feet or less, there being deposits of water-bearing sand inter- bedded with the till. The till tract presents a variable surface structure, such as is displayed in the majority of moraines whose main component is till, there bemg many places where sand and gravel immediately underlie the soil, but these are apparently in local and isolated tracts. North and northwest from this lowland till tract are uplands standing 200 to 300 feet above it. On these uplands the prominent ridges and hills have a very thin coating of drift, but the lower parts of the uplands are covered with a sheet of till of moderate thickness. The valleys have con- siderable gravel either flanking their slopes or aggregated in low knolls in their bottoms, but the maim bulk of the drift in the valleys is till, the gravel seeming to be mostly superficial. These hills are not silt covered in Butler County, Ohio, but in Franklin County, Ind., there is a narrow belt along the north side of the Whitewater which resembles the tract south of that stream in having a silt 3 to 4 feet or more in thickness covering an old drift, the Wisconsin drift beg absent. With the exception of this nar- row belt, which seldom reaches back 5 miles from the Whitewater Valley, the surface portion of the drift of northeastern Franklin County is a fresh, OUTER MORAINE OF THE MIAMI LOBE. 323 pebbly till dotted with occasional gravel knolls. The drift is about as thin there as in portions of the county outside the limits of the Wisconsin drift. Many wells have struck rock at less than 20 feet. In a trip along the watershed north from Mount Carmel the thickness of the drift was noted at several wells, as follows: Thickness of drift ir wells near Mount Carmel, Ind. Feet Upp AteAtp plecate shelley eaae onsets sat jee os eee cee e saber nose Sal Sen emaciee Sue ase ee eee 8 Witte IMiGraa PS ULE SE SOR SSS Se, Serene ies asi ANE a ae a Se re ele ne emg ee Rea RIE eee aby 4 (GeOrser Dione shwellNE At eens a =e Nes ee a Ao ro take She cae ns anntote Sse Meals ioe eee 20 Johme Schulltizisiwellieee sete sae seer oa iela fs) Senne ce we Se Seine See ote scien Seis mice cis pees 13 Ceaqge Saauilliz’s Walle sodssbesacoussss san cr edad snetese SeSedanlcdnAsesees Sceseuoteosedcedsbose 18 Mrmclowe:shwelll (SH pantisecs ail bathwihpy)) ase 62) eee ee Soe eee eles ee ee 22 No thE pantrolsecs 21a (Owmennotascertalned))|seee— esse serene sens ose) ene ee eye 16 In Howe’s well there was— Section of drift in Howe well. Feet Pi ey aden atest = = UR EM SCARS SH REAR Marana a eae HERR retUe en tieaeine aet yen 15 Samdlibed assay. weqcanipmraarle teeta sae ea LG Gey io ube adll dy ae iae wa selected adem eeetae RE eee Clarence et slats eeee Sts crenata is siainsi a saicics eae esate elsintiswde acces sie hee ome com area 34 PRO tallest aati ieee Ie a nei se twice Ses Smiles ness Sette dese thats ade ki sje 22 At Dixon’s a cistern 12 feet deep penetrated several feet of till, then passed through a black soil about 2 feet thick, and entered a whitish clay. No other instance of a buried soil came to the writer's notice in this neigh- borhood. Although the drift is mainly till, several gravel knolls have been opened in the valleys northwest of Mount Carmel. Southeast of Mount Carmel also, near Philanthropy, there is a large gravel knoll, which is described on a previous page. On the uplands west of the East White- water, 2 or 3 miles north of Brookville, there are two gravel knolls, one of which, near the center of sec. 7, T. 9, R. 2 W., contains a gravel pit 20 feet or more in depth. The gravel beds are in arching or oblique positions. The well at a schoolhouse nearby, in the same section, 30 feet deep, was mainly through tili and did not strike rock. Several other wells in the neigh- borhood, 20 to 25 feet deep, do not strike rock; but rock outcrops appear in a ravine east of the gravel pit at a level scarcely 30 feet below its base. The variability of the drift is shown by wells, some of which are mainly through till, while others are in gravel much of their depth. Bowlders are usually abundant im the vicinity of these gravel knolls. The valley of Whitewater River does not contain gravel knolls at the place where the ice sheet overhung it when the moraine was forming. The valley at this point 324 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. is now about 400 feet deep, and was perhaps 100 feet deeper previous to the deposition of glacial gravels by streams from the Wisconsin ice margin. ' In southern Fayette County, near Everton, morainic features are well displayed and the structure of the drift is variable. Several gravel knolls occur between Everton and Aleuina, and also northwest of Everton, but the greater part of the drift is till, both at the surface and in well sections. In northeastern Fayette and southwestern Wayne counties there is but little gravel on the uplands. ‘The soil is not so loose and loamy as is usually the case in morainic belts, and is called by the residents ‘‘cold clay.” The thickness of drift here is variable. One well near the county line, a mile or more east of Waterloo, is about 80 feet deep, and does not strike rock. About 4 miles southeast of Waterloo and east of the West Whitewater there are rock quarries. Along the West Whitewater in Fayette and Wayne counties there is a gravel plain one-half mile to a mile wide, which has a deep deposit of glacial gravel. The bottom has been reached only in the few gas-well borings that have been made along it. Several borings along this valley, both within the moraine and south of it, that reach rock are discussed below, beginning near the head of the stream at Dalton, Wayne County, on Nettle Creek, one of the main tributaries. At Dalton the thick- ness of drift in the gas well is 240 feet and the altitude of the well mouth is about 1,100 feet. There was a slight amount of gravel at the surface, but the greater part of the drift was found to be till, mainly of a blue color. Dr. E. H. Thurston, of Hagerstown, gave the following information con- cerning wells in that village, the altitude of which is about 1,000 feet: Hight gas wells have an average of about 100 feet of drift, the least amount being 78 feet. The upper 50 feet is largely gravel, the remainder till. At Cambridge (whose altitude is about 940 feet) two wells show about 100 feet of drift. One has 10 to 15 feet of gravel at top, the remainder of the drift being blue till. A reliable record of the second well was not obtained. There are outcrops of rock in Whitewater Valley in that vicinity at about the level of the wells. A mile west of Cambridge, and at 70 feet higher altitude, a well penetrated 160 feet of drift; the upper and lower portions of this were sand and gravel, a considerable amount of till intervening. At Dublin, 2 miles west of Cambridge, and at an altitude 115 feet higher, a gas well penetrated 300 feet of drift. At Connersville several deep wells OUTER MORAINE OF THE MIAMI LOBE. 325 have been made in prospecting for gas. The first boring, the altitude of which is about 850 feet, penetrated 75 feet of drift, nearly all sand and gravel. No record of the other wells could be obtained. Between the West and the Kast Whitewater rivers, in Wayne County, the record of but one well in which the rock is reached was obtained. 'This well is at Centerville, where a natural-gas boring penetrated 176 feet of drift, mainly till. A little gravel was passed through near the surface. The altitude is about the same as the Centerville station, 995 feet above tide. Water wells in this district often go down about to the level of the bordering valleys without entering rock. E. R. Quick, of Brookville, has collected the following information concerning the drift in the gas wells in the vicinity of that city. A well at a warehouse east of the river, near the forks of the Whitewater, altitude 630 feet above tide, penetrated 135 feet of drift, all sand and gravel. A well at the Franklin County Infirmary, west of the river, penetrated about 140 feet of sand and gravel and struck rock at about 2 feet higher altitude than at the warehouse. At Mr. Brocker’s, in Brookville, west of East Fork, at an altitude also about 630 feet above tide, a well has 135 feet of sand and gravel. Mr. Kimball’s well, near the station in Brookville, altitude 666 feet above tide, penetrated 160 feet of drift, thought to be mainly gravel. About 4 miles below Brookville a gas boring at an altitude of 600 feet penetrated 154 feet of sand and gravel before striking rock. BOWLDERS. There are not many surface bowlders associated with this 1aoraine or the inner border tract, but their occasional occurrence on the surface in places where there has been scarcely any erosion distinguishes this moraine and the district north of it from the older drift tract toward the south, on whose uplands the bowlders are concealed by silt. One very large gneiss bowlder on Mr. Perrine’s land, near the “Rock schoolhouse,” about 3 miles southeast from Lebanon, was mentioned by Orton.t It measured 17 by 13 by 8 feet, and slopes outward at the base as though still larger under ground. Near the road between Waynesville and Harveysburg, on the elevated uplands, the writer observed a bowlder about 8 feet in diameter and 3 to 4 feet high. By far the largest transported rock mass ever reported from Ohio is that which Orton mentions in his report 1Geology of Ohio, Vol. III, p. 339. 326 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. on Warren County.’ It is a large mass of Clinton limestone, covering about three-fourths of an acre and having a thickness of 16 feet. It is found east of Little Miami River near Freeport, and is 2 to 3 miles out- side the limits of the Wisconsin drift. It overlies Ilinoian till and other drift material. It was thought by Orton to have been derived from the outcrops west of the river, but in the writer’s opinion it was more probably derived from the northeast. This opinion is based on the fact that the strize at Wilmington, a few miles to the east, that underlie the Ilnoian drift, and are therefore connected with an ice movement as early as this bowlder transportation, have a southwestward bearing. STRIZ. Observations of striz: are not rare in the district covered by the Miami lobe, there being thirty-three recorded within this district south of the Wabash moraine. None have been observed outside the moraine under discussion, but between this moraine and the next succeeding one there are seventeen observations. Of these four are in Wayne County, Ind., and bear west of south toward the western limb of the moraine; three are in’ Butler County, Ohio, and bear southward toward the point of the morainic loop; the remainder are in the district between the Great and Little Miami rivers, and bear southeastward toward the eastern limb of the moraine. The glaciation, therefore, harmonizes well with the distribution of this moraine, the striz in nearly every instance being directed toward the moraine. Plummer, many years ago, discussed strize discovered by him near Richmond.” They are of interest, not only because of their value in indicating the direction of ice movement, but also because they are apparently the first striz ever reported from that State. They are found in a quarry of blue limestone on the west side of a small stream tributary to the East Whitewater, 2 miles north of Richmond. A very hard clay rested on the striated surface, and above this deposit were gravel, sand, clay, and soil, the whole occupying 15 feet. The bearing of the striz is 5. 20° W. Plummer gives the following description : The grooves vary from a mere scratch to furrows an inch or more wide, and with one or two exceptions running exactly parallel with each other. The average depth of these grooves is perhaps one-eighth of an inch, and their breadth and shallowness give to the surface of the rock a vittated appearance. 1Geology of Ohio, Vol. III, p. 285. 2 Suburban Geology of Richmond, Indiana, by John T. Plummer: Am. Jour. Sci., 1st series, Vol. XLIV, 1843, pp. 281-313. STRILZ OF THE MIAMI LOBE. 327 Other interesting observations on the drift formations are reported by Plummer in equally graphic manner. They relate to the occurrence of silts contaming blue spots thought to be “tanno-gallate of iron,” from which he made an ink; also to organic remains in the drift, and to the number and kinds of bowlders on the surface. The following observations of striz in Indiana are recorded in the State geological reports for 1859 and 1878: On page 43 of the earlier report, striz near Cambridge in a quarry in NE. } of sec. 33, T. 16 N., R. 12 E., about a mile west of Whitewater River, are said to have a bearing from north of northeast to south of southwest. In the later report (pp. 184-185), strive at the falls of the west fork of East Whitewater, near the locality noted by Plummer, north of Richmond, have a bearing of S. 40° W. Strize in the bed of Nolands Fork, near Centerville (p. 215 of same report), bear slightly west of south. In Butler County, Ohio, strize, whose bearing is nearly north to south,? were observed by G. F. Wright about 4 miles east of Hamilton on the southeast bluff of the Great Miami. Concerning these strie Wright remarks: These are of additional interest as showing the degree to which the ice move- ment at this point was independent of the local topography. The striz here observed were upon the south side of the Miami River (whose general course is here northeast and southwest), and 75 feet above low-water mark. The direction of the striz is diagonal to that of the valley, which is here a mile or more in width, but nearly at right angles to the general course of the glacial boundary, about 20 miles to the south. Orton personally mentioned to the writer that he had observed strize on the uplands northeast of Oxford which have a bearing nearly south. About 3 miles southwest of Middletown, on the west bluff of the Great Miami, is a glaciated exposure in which the striz bear 8. 8° E. (magnetic). In Warren County, Ohio, about 3 miles northeast of Springport, on elevated uplands at Brown’s quarry, striz bear 8. 48° E. (magnetic). Three miles west of Waynesville the bearing is 8. 48° E., while 3 tiles northwest, near the village of Lytle, the bearing is 8. 70° E. Orton’s map, opposite page 413, Vol. I, Geology of Ohio, indicates striz in the vicinity of Lytle bearing S. 66° E. and 8. 54° E., while near Centerville the map shows striz bearing 8. 80° E. In the vicinity of Yellow Springs and Springfield, and below Springfield, along Mad River 1See Bull. U. S. Geol. Survey No. 58, 1890, pp. 41-42. 328 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. bluffs, observations made by Orton, and later ones by Chamberlin, give the strie a bearing 8. 8°-12° E. About 4 miles east-northeast of Urbana, in a quarry south of Long’s station, there are exposures of strize which bear about E.10° N. The east- ward movement is clearly indicated on the rock surface, whose prominences show plainly that their west side is the stoss side. his bearing is nearly at aright angle to a moraine in which this quarry is situated, whose trend in that vicinity is from slightly west of north to east of south (see Pls. II and XI). INNER BORDER DISTRICT. The district which lies between the Hartwell moraine and the next later one (the outer moraine of the late Wisconsin series) comprises only a few counties in southwestern Ohio and southeastern Indiana. Its extent may be seen by reference to the map of the Maumee-Miami lobe (Pl. XI). TOPOGRAPHY. The features are somewhat diversified. The Ohio portion is hilly, except near the border of Indiana in Preble and Butler counties. The hills have rock within a few feet of the surface; the main drainage lines remain essentially the same as in preglacial times. The valleys of this region, especially those of streams like Fourmile, Sevenmile, and Indian creeks, are characterized by a peculiar filling with till) The till is several times as deep as on the uplands, and is level topped or nearly so, giving the appearance of a terrace when viewed from the uplands. In the lower portions of these streams the till has been channeled to a depth of 75 to 100 feet, and forms an inner and lower bluff. Above these lower bluffs of till stand the rocky upland tracts 200 to 300 feet or more higher than the streams. The plane surface which the till presents in these valleys is perhaps no more remarka- ble than that of upland plains. Had the amount of drift been sufficient to have nearly filled the valleys the plane surface would scarcely suggest a terrace. Two valleys in this inner border district, Mill Creek Valley and a val- ley leading from the Little Miami at Kings Mills to the Great Miami at Middletown, resemble the valleys above mentioned in having level-topped plains in them, but a view of these plains from bordermg uplands does not suggest a terrace, since the small streams now occupying them have scarcely INNER BORDER OF THE MIAMI LOBE. a29 begun the excavation of a valley, and the size of the plain is much more out of proportion to that of the present streams than the plains along Four- mile, Sevenmile, and Indian creeks. In northeastern Franklin, in Union, and southeastern Wayne counties, Indiana, and in a narrow belt in southwestern Preble and northwestern Butler counties, Ohio, the uplands are strikingly in contrast with those just described. Instead of being hilly the surface is level and poorly drained, and the valleys do not have the depth and size of those draining the adjoin- ing tracts in southwestern Ohio. The valleys are nearly all of postglacial age, the preglacial drainage being obscured except in the main lines, such as the Whitewater River and lower portions of the tributaries of that stream in northeastern Franklin County, Ind. : There is but little surface undulation in this level tract, the till swells, as a rule, being scarcely 5 feet in height. There is, however, a ridge-like accumulation in Union County that merits notice, though its significance was not determined. The writer’s attention was directed to it because of its prominence on the profile of the Cincinnati, Hamilton and Indianapolis Railway, which had been examined by him before he visited that district. The profile led to the suspicion that the ridge is a moraine, but upon reaching the ground it proved so inconspicuous a feature that the suspicion was scarcely confirmed. It has as smooth a surface as the bordering” plains, and might be crossed by the traveler without appreciation of its real height. The profile gives the following data: Profile over ridge in eastern Onion County, Ind. ¢ Yy Location. \ansattones Altitude. | Miles. Feet. Hist aSc tee enema eer a em eae nee eh ch ax 2 ae et eae ae 23. 00 475.0 (GRATE ca beaeSSg aS RSE SS oe NSS OA STE a en EI Se ieee BL 23. 875 509. 9 ANVGSTY OBIS AB cle al fA athe en te ad CS aia ei Be Se ete eo Ee gen Dy 24, 60 470.5 The slope on the east continues to College Corners and on the west to the creek west of Lotus, but is less rapid than on the ridge. The trend of the ridge is nearly north-south, but it dies away in either direction within a mile or two from the railway. It has been penetrated about 30 feet by wells and no rock strata have been struck. 330 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. STRUCTURE OF THE DRIFT. The drift of this inner border district, like that forming the moraine, consists largely of typical till, which has a clayey matrix with liberal admixture of pebbles. There are a few gravel knolls and ridges on uplands and also along valleys. Portions of the valley filling present a horizontal bedding in which sandy partings separate till beds or beds of stony clay; but the greater part of the filling, like that on the upland, appears to be typical till without distinct horizontal bedding. Wright has given views of two exposures of the till in the valley plain of Fourmile Creek, in Bulletin No. 58, which are here reproduced in PI. XIU, A and 2. The till represented in the first view is a typical deposit, which is nearly level topped and is banked against the base of a high, rocky bluff that within a mile toward the south rises to 300 feet or more above the creek. The exposure in the second view presents lamination, and in places there is clear evidence of water bedding. The large stones appear to have been dropped by ice into a stream which had only a sluggish cur- rent. ‘The eastern part of Oxford is on a flat-surfaced till plain, along the same creek, whose surface stands fully 100 feet below the high rocky bluff on which the rest of the town is situated and nearly 100 feet above the creek bed. There is scarcely an exposure of rock along the postglacial valley of Fourmile Creek from the junction of the three forks above Oxford to its mouth. The record of but one well was obtained along this valley. This well is at Brazil Inman’s, about 1 mile above the mouth ot the creek. It is 104 feet deep, and penetrates 90 feet of till, below which it is in sand and gravel. It is reported that “snail shells” and small twigs were pumped out from the sand near the bottom of the well. What percentage of drift in the valleys is of the age of the moraine under discussion, and what of the earlier or Illinoian age, can scarcely be determined from the facts at command. The freshness of the exposed por- tion of the drift along Fourmile, Sevenmile, and Indian creeks leads the writer to consider it of the same age as the moraine. The shells and twigs reported above, which were pumped from sands beneath the till near the mouth of Fourmile Creek, may be of interglacial age, and mark the line between the Wisconsin and the earlier drift sheet. The oceupancy of Mill U. S. GEOLOGICAL SURVEY MONOGRAPH XLI PL. Xll A, SECTION OF TILL AT LANE’S MILL NEAR DARRTOWN, OHIO. RB. EXPOSURE OF TILL SOME MILES EAST OF LANE'S MILL SECTION, INNER BORDER OF THE MIAMI LOBE. ool Creek Valley, in Hamilton County, and also the abandoned valley connect- ing the Little and Great Miami valleys, in Warren County, by this moraine, and the freshness of the drift there exposed, indicate that the upper portion at least was deposited contemporaneously with the moraine. However, the well sections in Mill Creek Valley south of the moraine seem to suggest that much of the filling may have taken place in the earlier advance. As above noted, there is some uncertainty whether the lowland tract connecting the Little and Great Miamis through western Warren County contains a deep buried channel or waterway capable of carrying a stream from one valley to the other, for the reason that rock is struck at slight depth in wells in the western part of the swampy tract connecting these streams. A well at Mrs. Stewart’s, on the east side of the county line road (between Warren and Butler counties), struck rock at 13 feet, and one at Mr. Schwab’s, about one-half mile farther north, at 20 feet. These are both in the valley, the latter being near its center, the former near the south side. Such meager evidence does not, however, preclude the possibility of a deep channel existing in this low belt, though it throws doubt on its occurrence. A few records of wells were obtained in'the Indiana portion. Mr. Burt, a well driller residing at Liberty Ind. who has made wells on the drift ridge near Liberty, noted above, reports that they penetrated yellow and blue till to a depth of about 30 feet, and then entered a black earth into which they were carried for a foot or two, the deepest well being 33 feet. In a well on the east slope at Mr. Bamon’s, one-half mile north of Cottage Grove, Mr. Burt found many bowlders about 30 feet below the | surface. Possibly an old land surface or stream bed was reached at this well. Two other wells were reported by Mr. Burt which may have passed into a drift older than Wisconsin in their lower portion. At Beechy Mire post-oftice Mr. Lybrook’s well entered a yellow clay below the blue till at adepth of 33 feet. At Salem, about 3 miles southeast of Liberty, Mr. Burt made a well which passed through the following beds: Section of a well southeast of Liberty, Ind. Feet Welllogy ill ss os SU sh Sei eee re tg es BAR eel on Ee Te Ma ore ee 8-10 IB ne atl leer ease ene eee yy Men a eee, halen Cem Oe a ace hc cee ee ce spar eb esee eee ters 25 Yellow clay, not noticeably pebbly, at bottom of well. aoe GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. At Weibels Corners, 4 miles northeast of Liberty, Mr. Burt made a well in which the blue clay below the surface yellow till was peculiarly soft, sticky, and free from pebbles, so that it could be unrolled from the auger like putty. In Liberty, at the Pyle House, a bed of muck and leaves was struck by the same well driller about 35 feet from the surface, below a blue till. Between the muck and the underlying rock was a sand bed 15 feet in thickness. In Liberty two gas wells have been made, of which one, on high ground in the east part of town, penetrated about 90 feet of drift; the other, on low ground in the west part of town (29 feet below the level of the railroad station, or 940 feet above tide), penetrated 70 feet of drift, mainly till. The drift in these wells is much thicker than the average on uplands in Union County. In the southeastern part of the county the thickness averages scarcely 10 feet over a tract comprising several square miles; and the large creeks in the county, which have cut channels 30 to 50 feet below the level of the uplands, usually reach the rock. It is probable that the average thickness is not more than 50 feet. In southeastern Wayne County, also, the deeper ravines reach the rock at 50 to 60 feet below the upland plain, which in the vicinity of the village of Boston is very level. Two short gravel ridges, which should perhaps be classed as eskers, were observed in the north part of Warren County, Ohio, east of Springboro. The longer one has a length of about a mile and trends west-northwest to east-southeast, while the shorter one has a length of about one-half mile and trends north to south. The shorter one has its southern terminus in Clear Creek Valley about a mile east of the eastern terminus of the longer one, the latter being situated entirely in Clear Creek Valley. The bearing of strie in that vicinity, as shown above, ranges from about southeast to S. 70° KE. The longer ridge, therefore, approaches more nearly the direction of the striz than does the, shorter one, but neither is strictly in harmony with them. At the southern end of the shorter ridge a spur leads off abruptly to the east for a few rods and there dies away. This turn of the southern end of the shorter ridge and the bedding in the longer ridge indicate that the direction taken by the water which formed the ridges was eastward, or the reverse of the present course of drainage along Clear Creek. No delta deposit nor eastward continuation of gravel deposits was found beyond the Derr Oe GED tind DP se ee INNER BORDER OF THE MIAMI LOBE. 333 shorter ridge. There are gravel knolls along the Little Miami Valley, near Waynesville, about 5 miles to the east, but the distance from the gravel ridges is so great that it is doubtful if the same stream that formed either of of them also formed the gravel knolls. The longer ridge is interrupted near its eastern end by a slight gap (a feature not unusual in eskers). Its greatest height is 30 to 40 feet, while portions are 20 feet or less. Its width, including slopes, is 100 to 200 yards. Its surface is somewhat irregular, as if there had been uneven deposits of englacial drift upon it after the body of the ridge had been formed. This view finds support in the fact that in Bennett’s gravel pit, which opens the ridge to view near its eastern end, there is a change from gravel to till in passing from the center to the north slope of the ridge, the till here being confined to the lower portion of the slope. The exposures are not suffi- cient to show whether or not the till in places reaches the crest of the ridge. Bennett’s pit shows great variations in the bedding of the gravel, in dip and thickness, as well as in coarseness of material. The lower part of the pit is more largely gravel than the upper, there being beds of nearly clear sand near the top of the ridge. The shorter ridge has a height of 10 to 12 feet and breadth of 50 to 100 yards, including slopes. It is opened at Blackford’s pit, its cross section being well shown. The surface beds arch over, but the deeper beds are horizontal beneath the center of the ridge. This arching of the surface beds may have been produced in the manner suggested by Russell," in his article on the glaciers of the Mount St. Elias region. The view is there expressed that gravel ridges of this class are built up in horizontal beds in tunnels in or beneath the ice sheet, and that upon the disappearance of the ice walls the material next the borders is left unsustained, and therefore settles down, giving the arched appearance to the surface beds. This short ridge has a much smoother surface than the larger one and apparently has no capping of till. At Blackford’s pit it is composed mainly of gravel of medium coarseness, there being but little sand and but few cobblestones intermixed. In both ridges the pebbles are composed largely of limestone rocks, not a small percentage being the local rocks. Near the mouth of Clear Creek, in Franklin, and for a mile or more southeast from that village, drift knolls are numerous. They range in 1J. C. Russell: Am. Jour. Sci., March, 1892. 334 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. height from 10 feet up to fully 60 feet and are sharp and nearly conical. They are all in a lowland tract on the south side of the valley, their bases being but 40 to 50 feet above Clear Creek, while the uplands on the south rise to a height of fully 200 feet above the creek. Occasional gravel knolls oceur along Clear Creek Valley between this group and the western end of the large gravel ridge. They appear to contain much gravel and may owe their presence in this lowland tract to the same stream which formed the ridge, though the method of deposition is even more problematical than, that of the ridge. CHARACTER OF THE OUTWASH. In the district outside the Hartwell moraine three quite distinct classes of deposits appear above the consolidated rocks: First, the earlier or Ilinoian drift which, covering the uplands, extends south to the glacial boundary; second, the silt deposits which cover the Illinoian drift and extend into the unglaciated districts; third, the morainic outwash, including the gravel aprons and such valley drift as seems to be connected with the moraine. The first and second having been considered, it remains only to discuss the third class. In connection with this the gravel aprons and valley drift in the reentrants are also considered. In the reentrant between the Scioto and Miami lobes there is a com- plex series of gravel plains. Probably all are of somewhat later date than the Hartwell moraine, and the latest are of late Wisconsin age. The broad gravel plain leading down Mad River is evidently of late Wisconsin age, the source of the gravel being in: the late Wisconsin moraine, which encir- cles the head of the river. East from the valley of Mad River there are other gravel plains, which are somewhat older than the one along the stream. One which leads from West Liberty southward past King’s Creek Station to Urbana, connecting both at the north and south with Mad River, stands but little above the Mad River gravel plain and may also belong to the late Wisconsin series. It appears to be an outwash from a weak moraine lying between it and Mad River Valley. Easi from this gravel plain there is a prominent moraine, noted above, which extends from southern Logan County, southward past Urbana, to Springfield, as indicated on the glacial maps, Pl. Il and XI. On the east side of this moraine a gravel plain appears which leads southward near the east border of the Mad River drainage basin to the headwaters of the Little gt haps ee pee eT ea fr. OUTWASH FROM THE MIAMI LOBE. 335 Miami, m a course singularly out of harmony with the present system of drainage, its course being directly across Mackocheek, Long, Buck, and Beaver creeks. It connects with the Little Miami Valley east of Spring- field near Thorpe station and, swinging to the southwest, follows down that valley. The width ranges from a half mile or less up to nearly 2 miles. There is a marked southward descent along this gravel belt, the alti- tude above tide being near Kennard 1,185 feet, east of Urbana about 1,150 feet, at Catawba station 1,090 feet, at New Moorefield 1,060 feet, and at the pomt of connection with the Little Miami drainage near Thorpe about 1,030 feet. The general elevation of this gravel belt is about 100 feet above the gravel plain along the neighboring portion of Mad River Valley, and, as it is distant from that valley only 3 to 6 miles, through much of its course within the present Mad River drainage basin, the descent toward Mad River is more rapid than along the line which the old stream followed. It is for this reason that the eastern tributaries of Mad River now pass directly across this old line of drainage. The course selected by the old stream appears to have been just out- side the Miami ice lobe at a time when Mad River Valley was buried beneath the ice. The moraine which lies west of the gravel plain bears out this interpretation, for it seems to be of the same age as the gravel plain, and knolls in places come down to the level of and merge into the plain. The eastward-bearing striz near Urbana also show that the Miami ice lobe extended about to this gravel plain. On the east side of this plain there is a blufflike border which indicates that the drift on that side was exposed for erosion and hence is probably somewhat older than that on the west. Its freshness, however, is such as to place it within the early Wisconsin glacial stage. The gravel plain has been eroded to a markedly greater degree by the streams that cross it than the late Wisconsin terraces on the same streams. It has been cut down from a level 20 or 30 feet and occasionally 50 feet above the late Wisconsin terraces, while those terraces are seldom 50 feet above the present stream. There is also a broader excavation above the level of the late Wisconsin terraces than below, which makes the contrast still more striking. As erosion in gravel is a comparatively slow process under ordmary conditions, these features seem to indicate that an interval of considerable length separates this gravel deposit from the late Wisconsin gravels along Mad River and its tributaries. 336 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. It seems probable that the ice sheet had melted away from the portion of the Little Miami Valley below the point where this belt of gravel con- nects with the river before the gravel deposition occurred, for latitude and the heat radiated from an extensive land surface would favor melting there, while the ice sheet still held its ground in the part of the reentrant to the _ north. z There are gravel aprons associated with morainic knolls and ridges along this part of the Little Miami which are probably somewhat older than the long belt of gravel just discussed. The most conspicuous is the plain immediately west of Xenia, known as ‘‘Cherry Bottoms.” There is also a small gravel plain east of Spring Valley. The Cherry Bottoms plain rises toward the moraine which borders it on the north and west, and fits about its knolls and ridges. It also contains numerous basins along the border next the moraine. This gravel plain is now drained southward to the Little Miami, through a valley utilized by the Little Miami Railway in rising from the river valley to Xenia. It is not certain whether the glacial waters followed this route or passed southward to Ceesars Creek along the ice margin; perhaps both routes were used in the course of the formation of the moraine. The small gravel plain east of Spring Valley stands at its western border more than 100 feet above the Little Miami River. There is a bed of gravelly knolls along this border which overlook Spring Valley and serve as a water parting between the Little Miami and Ceesars Creek; and south from there a till ridge causes the water to run from within one-half mile of the bluff of the Little Miami eastward to Cesars Creek. It is probable that the glacial waters which formed this gravel plain, like those of the present system of drainage, escaped through Ceesars Creek. On the west side of the Little Miami, 1 to 2 miles below Spring Valley, there is a small gravel plain which, though it lies near the inner border of the moraine, was probably formed by waters of glacial age. It stands fully 100 feet above the river, extends back about one-half mile from the bluff, and is a mile or more in length. There seems to be no terrace of corresponding height along the Little Miami below this plain. Its origin is therefore not clearly understood. Near the mouth of Ceesars Creek there are, on the east side of the river, gravel beds at levels about 150 feet above the stream but they are awe TRY Jao CME * i tr Rar OUTWASH FROM THE MIAMI LOBE. dal not clearly outwash deposits, being disposed in arching and oblique beds. One gravel pit exhibits beds which dip sharply eastward toward the bluffs. Gravel terraces apparently of glacial age are well defined along the Little Miami, below the point where the moraine crosses, but they are surprisingly low down, the general altitude of the upper terrace being but 50 feet above the river. In the vicinity of Kings Mills the moraine comes down to the borders of this terrace at the low altitude just named, thus indicating that no higher glacial terrace exists which can be correlated with this moraine. Upon approaching the Ohio the river descends more rapidly than the terrace; as a consequence the same terrace that stands 50 feet at Kings Mills stands about 100 feet above the river at its mouth. The altitude of the terrace at the point where the river leaves the moraine (near the mouth of Czesars Creek) is about 730 feet above tide, while at the mouth of the stream it is but 580 feet, a fall of 200 feet in 40 miles The present bed of the river falls 250 feet in this distance. The material embraced in the terraces varies greatly within short distances, showing a range from fine pebbles, well rounded, up to coarse subangular blocks, but the variations may, in many instances, be readily accounted for. For example, at Love- land the terrace is loaded with local limestone slabs which are thought to have been brought in, in part at least, by the freshets on a tributary which enters the river there from the east. Instances were noted where blocks: of local limestone were derived from projecting points a short distance upstream, and it is possible that the blocks at Loveland were in part derived from such sources. In many instances the coarseness of the material varies in accordance with the curve of the stream, bemg much coarser on the outer than on the inner curve. Where unaffected by these local influences the material in the terrace consists of well-rounded gravel with but a slight intermixture of sand or earthy material. The pebbles, like those in the moraine, consist largely of local rocks, the Canadian rocks forming less than 5 per cent of the material. The gravels present a remarkably fresh appearance, the surface of limestone pebbles slightly embedded, as well as those at some depth, bemg scarcely at all oxidized, while pebbles of crystalline rocks seldom show signs of disintegration. In these respects the pebbles are decidedly in contrast with those of gravels in the earlier drift whose lime- stones, when slightly embedded, are deeply oxidized and whose crystalline MON XLI 29, 338 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. pebbles are to a large extent disintegrated. The calcareous material with which the waters that percolate this terrace are charged forms a slight cementation of portions of the terrace from which the water is removed by evaporation. The terraces of the Little Miami were probably built up in part by glacial streams from the vicinity of Kings Mills, where the ice sheet came down to the borders of the valley, as well as from the point where the moraine crosses the stream near the month of Caesars Creek, and from the Scioto lobe along Todds Fork. It is not known whether glacial terraces lead in from the East Fork, that stream not having been examined. On account of these numerous lines of discharge, the lower portion of the Little Miami Valley and the portion of the Ohio Valley immediately below the mouth of the Little Miami were greatly filled by gravel, there being in the city of Cincinnati a filling from a level somewhat below the present stream to a level about 110 feet above it, the greater part of which is gravel with but a slight admixture of sand and earthy material. . As above noted, statements that the rock floor of the Ohio Valley at Cincinnati stands 120 to 200 feet below the present bed’ are probably due— to confounding the terrace with the river bed, which would make a differ- ence of about 110 feet. After careful inquiry the writer could learn of no wells within the city limits which show the rock floor to be lower than 75 feet below low-water mark. Records of wells were obtained at various parts of the city showing the distance to rock in the midst of the valley as well as on its borders, as follows: East End Gas Works, near north bluff, penetrated 130 to 135 feet of drift, striking rock at 70 to 75 feet below low-water mark. West End Gas Works, in midst of valley, penetrated 118 feet of drift, striking rock at 58 feet below low-water mark. Storr’s distillery (formerly Gaft’s), west of Mill Creek, near mouth, has one well that struck rock at 40 feet below low-water mark, while thirteen others failed to strike rock, though terminating at levels 40 to 50 feet below low-water mark. The pier on the Ohio side of the suspension bridge rests on rock at about 40 feet below low-water mark, while the middle pier of the Chesa- peake and Ohio Railway bridge was reported by Joseph F. James to rest 1See Geology of Ohio, Vol. I, 1873, p. 433; also Bull. U. 8. Geol. Survey No. 58, 1890, pp. 79-80. ‘ | i an OUTWASH FROM THE MIAMI LOBE. 339 on rock at a level about 60 feet below the river bed. The well at the Hotel Emory penetrated 150 feet of drift and is thought to be on rock at the bottom 40 to 50 feet below low-water mark. be, x : = : ' MAP OF THE SCIOTO GLACLAL LOBE a be. = BY PRANK LEVERETT 0 ee ee OUTER MORAINE OF THE SCIOTO LOBE. d41 found to support the view that it was markedly greater in the basins than on the elevated hilly tracts that border them. On the contrary, evidence against great excavation is found in the district south of the glacial boundary near the southern extremity of this glacial lobe where the two types of topography are nearly as much in contrast as within the glaciated district, there being east of the meridian of Hillsboro, Ohio, and Maysville, Ky., a more elevated and more hilly district than there is west of that meridian. For further discussion of topographic features see Chapter II. THE OUTER OR CUBA MORAINE. An earlier moraine than the outer one described by Chamberlin! was discovered by the writer in the southwestern part of the district covered by the Scioto lobe. It is apparently to be classed with the early Wisconsin series, while the one described by Chamberlin seems to belong to the late Wisconsin series. So far as recognized, it lies outside the later ones only in the southwestern part of the district, though it may possibly have cor- relatives in portions of the tangled systems of moraines formed on the eastern side of the lobe. The name Cuba is taken from a village that stands on the crest of the moraine near the middle of the morainie loop. DISTRIBUTION. On the north side of “Beech Flats,” in Pike County, and near the | eastern line of Highland County, Ohio, this moraine becomes clearly sepa- rated from, and distinctly developed outside of, the later ones. It is readily traced westward along the south side of Rocky Fork, from the mouth to the source of that stream, the villages of Cynthiana, Carmel, and Marshall being situated near its southern margin and Hillsboro just north of it. Its ‘breadth is 1 to 2 miles. In the vicinity of Hillsboro the creek winds among sharp gravelly knolls, which have a contour strikingly different from the remainder of the belt, and which may prove to belong to the earlier drift sheet. Northwest of Hillsboro the moraine for several miles is not well developed, but a mile or two southeast of New Vienna it reappears in con- siderable strength. From that point it takes a westward course, its outer margin being in surveys 2357, 753, 4656, 4233, and 4234, Highland County. Continuing westward into Clinton County its margin at the East Fork of 1Third Ann. Rept. U. 8. Geol. Survey, 1883, pp. 339-341. 342 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Little Miami River is at the crossing of the Martinsville and Hillsboro pike. From this stream westward to Martinsville the pike runs near the south margin of the moraine, keeping the outer border plain constantly m view. Martinsville is itself on the south slope. West from that village the moraine leads through Cuba, its southern edge being followed by the East Fork of Cowans Creek to its junction with Todds Fork, near Clarksville. From this point it swings rapidly northward and, assuming a course slightly west of north, comes to Czesar Creek, near Harveysburg, where it connects with the eastern limb of the outer, or Hartwell, moraine of the Miami lobe. The interlobate moraine, as above noted (p. 305), extends up the Little Miami Valley across Greene County. This belt exhibits its greatest breadth near Cuba, where for a few miles it has a width of 4 or 5 miles; usually its width is but 1 or 2 miles. RELIEF. North of Beech Flats, in Pike County, and m southeastern Highland County, the moraine is of a subdued type, and stands only 10 to 25 feet higher than the north border of these flats. Toward the west sharp gravel hills, 80 to 100 feet in height, set in, among which are low tracts no higher than the tracts outside (south) of the moraine and but little higher than the valley of Rocky Fork, which lies on the north. As already stated, these gravel hills may belong to the earlier drift sheet instead of this moraine. Both north and south of this portion of the moraine there are rocky hills bearing scarcely any drift, which stand much higher than the moraine. The moraine is, therefore, not so conspicuous a feature as it would be on plane tracts, such as are found in northwestern Ohio or even on those in the adjoining counties, Clinton and Fayette, where there are few rocky hills. In the northwestern part of Highland and in eastern Clinton counties it rises quite abruptly above the flats that border it on the south, in many places a rise of 20 feet being made in as many rods, while the crest of the moraine is 30 to 60 feet above the outer border plain. The Baltimore and Ohio Railroad profile shows at Martinsville a rise of 15 feet in 5 chains and a rise of 62 feet in 52 chains in its passage from the plain to the crest of the moraine. West of Martinsville there is a more gradual rise to the moraine from the outer border plain than that noted east of the village, about 50 feet in a mile being the usual rise in the vicinity of Cuba. North of Clarksville it stands 30 to 50 feet above a plane tract along its outer OUTER MORAINE OF THE SCIOTO LOBE. 343 border, drained by a small stream known as Flat Fork, and presents an abrupt relief. North from the point where it touches Caesars Creek, near Harveysburg, it is, as noted above, so closely associated with the correla- tive Miami moraine as to be distinct only at intervals. Near Xenia the eastern part of the interlobate belt rises boldly above the country west of it, but its altitude there is due, im large part, to the underlying rock, since it lies upon the western edge of the Niagara escarpment. On the Xenia and New Jasper pike, leading eastward from the court-house in Xenia, there is an ascent of about 100 feet in 2 miles, where a summit is reached. A mile or more farther east, and only 40 to 50 feet lower, are outcrops of rock. The inner border relief of the interlobate belt in this vicinity is 30 to 40 feet. In Clinton County the inner border relief is scarcely noticeable except in rare instances; it seldom exceeds 25 feet, and rises for a mile or more to attain this height. RANGE IN ALTITUDE. The altitude ranges between 900 and 1,200 feet above tide, being ereatest in the vicinity of New Vienna, as shown by the table below: Altitudes along the Cuba moraine. Feet above tide. Mierngll (Olm@ Ceolosiceall Sieve) -aasccgsco sence soSaaueucsonegssvocesssbendscenseoeseasces 1, 031 Near New Vienna (Baltimore and Ohio Southwestern Railroad) .....-.-.-.------------------ 1, 180 Near Martinsville (Baltimore and Ohio Southwestern Railroad)..........-.------------------ 1, 106 Ogden, in valley (Cincinnati and Muskingum Valley Railroad) -...-.---.-.------------------ 901 BASLO texte Mian (AN ELOIG) Me ee eee cies tee eieise ee ear ee bers SACLE tis ee see See ote me em eR 1, 100 TOPOGRAPHY. The topography of the moraine is of a gently undulatory type, swells exceeding 10 feet in height not being numerous, while those with a height of 15 to 20 feet are rare. It is undulatory, however, in this sheht degree, and thus differs from the plains toward the south, which have extensive tracts so level that the water which falls in the spring often stands on the surface until evaporated by summer drought. The distinctive characters of this moraine are its relief above the flat land which borders it, as was noted above, and its general freedom from silt such as covers the flat land. Were it not for these its classification as a moraine might be doubtful, for in the matter of drift swells it certainly has not a pronouncedly morainic expres- sion; but a consideration of these features and of its connections makes 344 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. it evident that it marks a part of the margin of a glacial lobe. The sharp gravel knolls which appear near the line of the moraine in the vicinity of Hillsboro apparently belong to the [linoian or earlier ice invasion, as already indicated. In eastern and central Highland County the moraine presents in its . outer portion gentle swells of till, 5 to 15 feet in height, each covering areas of 1 to 10 acres or more. Northwest from the Maysville Railway, in sur- vey 2480, small gravelly knolls 10 to 20 feet or more in height abound, several of which are in view from the Cincinnati pike west of Hillsboro. From survey 2480 northward to survey 2351, a distance of about’ 4 miles, there are no well-defined morainic features. In northwestern Highland, in Clinton, and in Greene counties there is, aside from the main ridge, which stands 20 to 40 feet above the outer plain, a moderate number of small knolls and gentle swells 10 to 20 feet in height. The majority of these swells are conical, or but slightly elliptical. When elliptical, the trend of the longer axis is usually in line with the moraine, whose trend there is from east of north to west of south. STRUCTURE AND THICKNESS OF DRIFT. In the main the drift consists of till, but, like most other moraines and also the intermorainic drift sheets, considerable variation is frequently-found within short distances, owing to the presence of local beds of assorted material which occur at various depths. It is from these beds that the wells of the region usually derive their water supply. But in Highland County, in the vicinity of Hillsboro and thence down Rocky Fork, as has been noted, large gravel knolls occur. 'The gravel in these knolls is largely composed of limestone pebbles, and much of it near Hillsboro is cemented, and in general it has the aged appearance of the earlier drift. It shows strata in various attitudes, but where opened extensively horizontal stratifi- cation predominates. The lower limit of this sheet of drift is in places shown by a buried land surface, having a soil and peaty deposits. The buried soil is found at Marshall, as has been noted by Orton, and many wells reported to the writer in Martinsville and some at Wilmington strike it. It is well exposed along a ravine in the south part of Wilmington, as described below. The buried soil, wherever noted in Highland and Clinton counties, is OUTER MORAINE OF THE MIAMI LOBE. 345 usually but 20 to 25 feet, rarely 40 feet, from the surface, and it is thought to constitute, as a rule, the surface of the older or Illinoian drift sheet. Apparently this slight depth represents the usual thickness of the early Wisconsin drift in this region, for it is not over 25 feet on the moraine at Martinsville and Marshall, and may be even less on the inner plain. At Martinsville many wells strike considerable vegetal material, wood, soil, ete., at about 20 feet, but occasionally as low as 40 feet. Wells in this village 40 to 45 feet deep do not reach rock. In some wells inflammable gas issues at a depth of from 30 to 40 feet, and is perhaps derived from the vegetal deposits of the drift. The drift there is mainly till, both above and below the buried soil. Orton has reported that at Marshall 11 out of 20 wells struck a buried soil or vegetal material at slight depth. The drift at this place extends deeper than the horizon of the soil, smce wells 25 to 30 feet deep on low ground, as well as those on knolls, fail to reach rock. Near Wilmington the distance to rock on surfaces having no marked difference in altitude ranges from a mere trace up to 80 feet or more, there being an outcrop of rock just east of the city, while on ground equally low within the city limits 60 feet of drift is not uncommon, and the gas-well boring north of the city, on ground but little higher, penetrates about 80 feet of drift. The late L. B. Welch, of Wilmington, has ascertained that wells in Wilmington, where drift is 60 feet deep, penetrate about equal amounts of older drift and newer, and the older, i. e., that below the buried soil, is drier and much more difficult to penetrate than the newer, probably because of a partial cementation. Excellent exposures of the buried soil are found along Lytles Creek in the south part of Wilmington. The soil is 2 to 6 feet in thickness and of very dark color. It is overlain by 15 or 20 feet of Wisconsin till and underlain by about the same amount of IIl- noian till. There is a small amount of white clay resting on the soil, but in most of the exposures the clay was removed before the Wisconsin till was laid down, so that the till commonly rests directly on the soil. The till below the black soil is oxidized to a depth of 10 or 12 feet, below which it is of a blue color. It is on Lytles Creek, a few rods below the place where the buried soil is exposed, that strize were found beneath the Illinoian drift. They bear 8. 32° W., or in about the same direction as the Wisconsin ice movement. As above noted (p. 326), they bear strongly upon the inter- 346 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. pretation of the direction in which the Clinton limestone of the “ Betty Heidy ” quarry was transported. Welch has found many Devonian fossils in the drift near Wilmington, which accord with the strie and the Wisconsin moraines in indicating a southwestward movement of the ice sheet, for the principal outcrops of Deyonian strata are to the northeast. Wells in Wilmington also strike a bed containing molluscan shells beneath about 25 feet of till and above the hard till of the Ilinoian drift. They were probably in the white clay referred to the Iowan stage. Welch collected a considerable number of these shells, which await identification, | though they seem to be largely Succinea avara. He also examined expo- sures of the buried soils and found seeds of Sagittarius and the bulrush of northern ponds; also pieces of wood, one ot which shows beaver cuttings; and another was thought by him to show evidence of charring by fire. Of these specimens the writer has seen the first-named piece of wood and the collection of shells from below the till. The wood appears to be cedar. The shells are all minute, being scarcely one-eighth inch in diameter, and were in their original matrix of fine silt. In Greene County there are few deep wells along the moraine, water being usually found at 20 feet or less. The following records of deep wells are the only ones obtained. At C. W. McDonald’s, on the Xenia and Wilmington pike, about 2 miles south of Xenia, a well 52 feet in depth does not reach rock. It was thought by Mr. MeDonald to be mainly through till. At a school- house about 14 miles southwest of Paintersville, on the plain east of the moraine, a well was dug which has the following section, as reported by D. H. Oglesbee, who assisted in digging it: Section of schoolhouse well near Paintersville, Ohio. Feet. Ales AYGOl low Antllll Sales yneenim rcs tN ee oe SU Se oa 2ST cid Seu S) et ee ORION ye ee 8-10 Dien SNivi=y(nllll es Nee Sean ere Re Ao Ser Pe Nn ere Mean Kee At. Sc. Wot Soe 40 By DAY REIL oo debe seceded nace bose ate bee ere ebenooseesodse dseadositedmaadoscsseasssee5s 10-12 A, Teleml, clay Gein, oit lollivusin Collong, joemeinmeGl. ~-- 62552 S526 5252s 522s ctec cessed en eacessccess=: 20 The well was abandoned at about 80 feet. Another well made subse- quently at the same schoolhouse obtained water at 125 feet, which over- flows, but the writer was unable to obtain a detailed section. Oglesbee is of the opinion that it did not reach the bottom of the drift. INNER BORDER OF THE SCIOTO LOBE. 347 BOWLDERS. There are few bowlders either on the moraine or on the inner border plain, but what is lacking in number is partly made good in size. A gneiss bowlder on the farm of the Clinton County infirmary, about 200 yards south of the Wilmington and New Vienna pike, measures 47 feet in cireum- ference 1§ feet above its base. Its highest point stands { feet 8 inches above ground, and it is evidently sunk into the ground to some depth. It has a diameter from north to south of neaily 20 feet, but from east to west it is scarcely 10 feet. It contains a few very coarse crystals of feldspar several inches in diameter, and coarse masses of quartz, but the crystals are generally fine. A short distance south of the crossing of the Midland Rail- way by the Wilmington and Cuba pike, there is a limestone bowlder 11 or 12 feet long and 6 or 7 feet wide standing about 1 foot above ground. It contains Favosites and cyathophylloid corals (species and geological horizon not determined). A number of small bowlders 1 to 2 feet in diameter, mainly granite, were observed between Cowans Creek and Cuba. They are more numerous there than elsewhere on this moraine, but they consti- tute no serious hindrance to the cultivation of the soil. Nearly all the bowlders observed are well rounded; this is especially true of the smaller ones. Pebbles are generally quite rare on this moraine to a depth of a foot or more, but the moraine has not such a continuous deposit of silt as occurs on the outer border plain. INNER BORDER PHENOMENA. In Greene County there is a plane tract between the Cuba moraine and a neighboring later moraine. In Clinton County there is a generally plane surface between these moraines, but just east of Wilmington there is a small drift ridge trending from northwest to southeast. It has a more or less distinct continuation in both directions, but joins the Cuba moraine at the northwest im northwestern Clinton County, and at the southeast a short distance southeast of Wilmington. Its surface is about 30 feet above the tracts east and west of it, where the Washington and Wilmington pike crosses, but as a rule it is scarcely so prominent. Its width where most prominent is less than a mile. The surface of the crest is gently undu- latory, with oscillations of 10 to 15 feet, more or less. These undulations, though slight, are in contrast with those of the smoother till tract on 348 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. either side, which scarcely exceed 5 feet. In Highland County the inner border district is hilly, but the drift has usually a plane surface; occasional knolls and ridges of small size and limited extent appear. STRIZ. The bearings of the striz are on the whole in harmony with the distribution of the moraine, since they form a diverging series bearing southward, southwestward, and westward to meet the moraine nearly at right angles. While the majority may have been formed at the Wisconsin invasion, one exposure is certainly of Ilinoian age, as indicated above, Observations were made as follows: 1. On the south bluff of Lees Creek, near the top of the hill, 140 to 150 feet above the creek valley. Exposed in a ditch on the west side of the East Monroe and Hillsboro pike, bearing 8. 12° W. (magnetic). The rock surface rises rapidly toward the south, affording an excellent surface for the glacier to work upon. The strie take the form of numerous fine lines. 2. On Bull Run, a tributary of Hardins Creek, in survey 2518, about one-fourth mile east of the Leesburg and New Petersburg pike, bearing S.9° W. (magnetic). The rock is a hard brown limestone, perhaps siliceous in part. ‘The exposure is in the bed of the stream, and the glaciation con- sists of shallow grooves one-half inch or more in width, and of fine lines, all having, so far as determined, the same bearing. 3. In the second railway cutting west of Leesburg in a ditch at the side of the track, on brown limestone, bearing S. 18° W. (magnetic). The strize consist of fine lines, parallel so far as observed. In a cutting between this place and Leesburg the railway has removed layers of rock to a depth of several feet. Mr. Hilliard, of Leesburg, states that he has observed strize in this cutting bearing west of south. Orton has reported striz on a hill to the south, the altitude being 75 feet or more above the level of the exposure in the railway cutting.’ 4. In Clinton County two striated exposures were noted. One is on the Clinton limestone, in the bed of Lytles Creek in the southwest part of Wil- mington, bearing 8. 32° W. Gnagnetic). 5. The other is just below the railroad bridge west of Ogden on a low ‘Rept. Ohio Geol. Survey, 1870, p. 265. STRILA OF THE SCIOTO LOBE. 349 bench of rock at the west side of the creek bed, bearing 8. 37° W. It consists of a multitude of fine lines on a blue fossiliferous limestone of Lower Silurian age. 6. Chamberlin has reported striz on Andersons Fork southwest of Reesville, bearing $. 45°-56° W.' 7. On the east side of the Wilmington and Xenia pike near the top of the north bluff of Czesars Creek, in Greene County, are several glaciated exposures, bearing 8. 40° W. (magnetic). 8. Near New Jasper, Greene County, in Bickett’s quarry, south of the Xenia and New Jasper pike, the rock surface is planed to glassy smoothness and covered with strize, the majority of which bear W. 5° N., but they range from W. 2° N. to W. 20° N. (magnetic). The westward movement was determined by the examination of a cherty prominence in the stone, the east side being the stoss side. | 9. At Conklin’s quarry, near New Jasper, a short distance east of Bickett’s quarry, on the bank of Czesars Creek, bearing of nearly all the strie about W.17° N. This rock, because of its hardness, is not planed down like that in Bickett’s quarry. ‘There are many depressions and furrows so striated as to indicate a westward movement, the strongest striation and heaviest planing being on the west side of such furrows as were too deep for the ice to striate to the bottom. OUTER BORDER PHENOMENA. The earlier drift and its silt capping having been discussed, it remains only to discuss the fluvial plains. There are two streams, Todds Fork and the East Fork of Little Miami, which lead from the moraine under discussion into the outer border district, and whose valleys were available for the escape of glacial waters at the time the moraine was forming. The East Fork was not examined for evidences of glacial streams, but Todds Fork was found to carry remnants of a gravel terrace which is apparently of the same age as the moraine. At the outer border of the moraine just above Clarksville the terrace is well exhibited, occupying nearly the whole width of a broad valley. Its connection with the moraine is not so close as in certain other streams which the writer has examined within the glaciated district, but this may be due to the fact that the moraine does not fill the valley, but simply dots the slope with scattering knolls. 'Third Ann. Rept. U. 8. Geol. Survey, 1883, p. 340. d00 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. This much is certain, however, that gravel deposits are rare above the moraine and very abundant below it. The height of the terrace at the border of the moraine is about 30 feet above Todds Fork, and it is about the same at Clarksville. At a railway switch about midway between Clarksville and Hicks station it rises 40 feet or more above the creek. In the vicinity of Hicks station it is 40 to 50 feet, while along the north- flowing portion of the creek, 1 to 14 miles above its mouth, the terrace stands about 60 feet above the creek. it continues down Little Miami River, being well exposed in the south bluff for 2 miles below Morrow. The descent of the terrace near its head is about the same as that of the creek, 18 to 20 feet per mile, but farther down it is less rapid. From Clarksville to the exposure a mile above the mouth of the creek, its descent is about 130 feet in 10 miles. The fall of the present stream in the same distance is 160 feet. The Cincinnati and Muskingum Valley Railway has opened a gravel pit in the terrace near its head, about a mile above Clarksville. It exposes 3 or 4 feet of sandy gravel at top, beneath which is gravel with but little sand intermingled, exposed to a depth of about 20 feet. It is horizontally bedded and contains many pebbles 3 to 4 inches in diameter. Much of the gravel is well-rounded local limestone, but Canadian rocks are not rare. At Clarksville a well on the terrace at the Hadley House, 20 feet in depth, did not reach the bottom of the gravel. It was described by Mr. Hadley as containing coarse gravel with pebbles 3 to 4 mmches in diameter, thin beds of fine gravel being interbedded with the coarse. Mr. A. W. Thomas has a well on the lot adjoming the Hadley House which reached the bottom of the gravel and entered a blue shale at 20 feet. At the exposure near the mouth of Todds Fork the upper 20 feet consists of well-rounded gravel containing Canadian as well as local pebbles. Few pebbles exceed 3 inches in diameter, and there is much fine gravel and sand intermixed with the larger pebbles. There is no silty capping here such as occurs near Clarksville. Below the gravel for about 20 feet there is a poorly assorted material in which many slabs of local limestone occur, and beneath this is about 20 feet of blue till. The till apparently fills a narrow gorge in the rock strata, for a few rods up stream from the deposit of blue till limestone strata are exposed which rise to the level of the top of the deposit. i i ea DRIFT OF THE GRAND RIVER LOBE. B51 SECTION III. PROBABLE EARLY WISCONSIN DRIFT OF THE GRAND RIVER LOBE. As indicated m the discussion of the drift border, a portion of the extramorainic drift in eastern Ohio and western Pennsylvania, notably that in Columbiana County, Ohio, and Beaver County, Pa., appears to be as recent as the early Wisconsin, while that in counties to the east seems to be much older, Kansan or pre-Kansan in age. The portion thought to be of early Wisconsin age extends only a short distance, nowhere more than 10 miles, beyond the strong outer moraine of late Wisconsin age. It is rarely aggregated in knolls or ridges, thus ditfermg markedly from the hummocky surtace of that moraine. It fills the valleys and lowlands to considerable depth, but on ridges and hills it is represented only by seatter- ing pebbles and occasional thin deposits of till. The till is often present in considerable amount on the north side of ridges nearly to the crest, while the south side at similar altitudes is almost destitute of drift. The till is of a clayey constitution, like that of the early Wisconsin farther west. The chief reason for assigning this part of the extramorainic drift to a later stage than the old drift farther east is found in its comparative fresh- ness. It is but little more weathered than the late Wisconsin drift of the neighboring moraine. A response with acid can usually be obtained at a depth of but 5 or 6 feet The bowlders also are but little more weathered than those on the surface of the late Wisconsin moraine. hey are strik- ingly in contrast with the rotten and deeply weathered bowlders and pebbles which characterize the old drift. of northwestern Pennsylvania. The grounds for separating this extramorainic drift from the late Was- consin are perhaps open to question. It has impressed the writer, and also Professor Chamberlin, as somewhat more weathered than that of the neigh- boring late Wisconsin moraines. The fact that it is so strikingly different in topography has also been considered a matter of some consequence. It also seems natural that this lobe, as well as the Scioto and Miami lobes, should have extended farther in the early Wisconsin than in the iate Wisconsin stage. But the reference to the early Wisconsin is only provisional. This drift may yet prove to be the product of an advance but little earlier than that which formed the bulky late Wisconsin moraine. CEA wi Gs SXele THE INTERVAL BETWEEN THE EARLY AND LATE WISCONSIN DRIFT. The Hartwell-Cuba moraine and its associated sheet of drift, and the morainic tracts in the reentrant between the Scioto and Miami lobes, appear to be the only outlying representatives of the early Wisconsin drift in this region, the remainder of the series being concealed beneath the moraines and drift sheets which are here referred to the late Wisconsin series. The evidence of an interval between the deposition of the early Wisconsin drift and the formation of the outer moraine of the late Wisconsin series is well shown in the elevated land lying between the Miami and Scioto lobes, where, as above noted, the outer moraine of the Miami lobe and the outwash eravel associated with it had been trenched by streams prior to the formation of the neighboring late Wisconsin moraines of the Miami and Scioto lobes. Professor Chamberlin noted this channeling and interpreted it as evidence of an interval while making a reconnaissance of western Ohio in 1883, -and the writer gave it further attention a few years later. The cutting of the broad valley of Mad River, about 2 miles in average width and 25 to 50 feet in depth, was referred by Chamberlin to this interval, as were also similar channels of its tributaries. In the late Wisconsin stage the ice came down about to the valley of Mad River on the west and covered the upper portion of the western tributaries. The sheet of drift deposited at this later advance only partially fills some of the tributaries, but its knolls dot the slopes and bottoms of the interglacial channels, thus repeating the phenomena of the early Wisconsin moraine in valleys of the Whitewater system noted above (p. 306). On the east side of the Mad River drainage basin there are similar phenomena associated with the outer late Wisconsin moraine of the Scioto lobe. This moraine descends into valleys cut in the early Wisconsin drif of that region. The details are given in connection with the discussion of that moraine (pp. 382 et seq.). 302 TIME BETWEEN EARLY AND LATE WISCONSIN. aoe) It should perhaps be stated that Mad River and its tributaries do not follow to any great degree preglacial lines, the concealed rock surface, if we may judge from well data, being nearly as elevated along the valleys as beneath bordering uplands. The evidence appears decisive that the valleys are interglacial and not preglacial. The evidence of an interval is less striking on the south and west border of the Miami lobe than that on the east, just noted. On the Great Miami, the valley gravels leading away from the later sheet of drift have filled its channels about to the level of the early Wisconsin terraces. On some of the western tributaries of the Great Miami the gravels of the later invasion lie in trenches cut into the drift of the early Wisconsin, but the trenching is not conspicuous, probably because of the small size of the interglacial streams and their moderate rate of fall. In Whitewater Valley the gravel of the late Wisconsin has been built up about to the level of the early Wisconsin gravel, rendering it difficult to separate the two. On the whole, the interval between the early and late Wisconsin appears much briefer than the Sangamon interglacial stage, and somewhat briefer than the Peorian. The difference in the erosion features of the early Wisconsin sheet and those of the outer moraine of the late Wisconsin appear no more striking than between the Shelbyville and the Valparaiso moraines of the Illinois glacial lobe; indeed, the difference in the outwash seems scarcely so strik- ing. Itis, however, such a difference as would naturally be found im passing from the outer part of the early Wisconsin to the outer part of the late Wisconsin in Illmois, and is greater than is found in that State in passing from the northern or later part of the early Wisconsin to the southern or outer part of the late Wisconsin. From this it is inferred that the Hartwell- Cuba moraine is a correlative of either the Bloomington or the Shelbyville moraine of the Illinois lobe, rather than the Marseilles. However, the precise correlation of this moraine with a moraine of the Illinois lobe has not been attempted. MON XLI——23 Chet AIP ME aes SC ICIE, THE MAIN MORAINIC SYSTEM OF THE LATE WISCONSIN STAGE. SECTION I. IN THE MIAMI LOBE. THE MORAINES. GENERAL STATEMENT. Under this name is discussed a series of moraines whose members in part coalesce and therefore are more easily described together than sepa- rately. This system where best differentiated comprises three moraines. Of these the outer two were examined by Chamberlin, and are briefly described in his paper in the Third Annual Report.* The third or inner one lies but a few miles north from the second, and is distinct from it only in the midst of the terminal loop. The entire system, including the narrow plains lying between the moraines, has nowhere a width exceeding 18 miles, and where the members are closely associated the width is reduced to 10 miles or less. DISTRIBUTION. At the head of the reentrant angle near Bellefontaine, Ohio, this morainic system connects with the correlative system of the Scioto glacial lobe. The eastern limb follows and constitutes the western bluff of Mad River from the source of the stream east of Bellefontaine, southward nearly to the latitude of Urbana, the several members being united into a single great belt. It then leaves the river to the east for a few miles and passes southwestward through New Carlisle, near which it begins to separate into distinct members. The outer member crosses Mad River near its mouth and follows nearly the east bluff of the Great Miami from Dayton about to Frank- lin. Here it swings westward, crossing the Great Miami Valley near Carlisle, and passing south of Germantown and north of West Elkton, enters the valley of Sevenmile Creek at Camden. Jt then swings abruptly northward, passing near Sugar Valley, West Florence, and Westville, striking the State line between New Paris, Ohio, and Richmond, Ind. Near the State line it 1Terminal moraine of the second Glacial epoch, by T. C. Chamberlin: Third Ann. Rept. U. 8. Geol. Survey, pp. 334-830. 304 MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 300 is jomed by the other members of the system. In Indiana the united belt passes north of west across northern Wayne and southern Randolph coun- ties into northeastern Henry County, where it connects with the correlative moraine of the East White lobe. The outer member is quite distinct around the southern end of the loop from near Dayton to the State line and has a width of 2 to 3 miles. Throughout the remainder of its course it is more closely associated with the later members, but it does not appear to be overridden by the later ones except in the extreme northern portion of the eastern limb, and possibly in the reentrant angle between the Miami and Kast White lobes, in Henry County, Ind. The middle member is clearly recognized throughout its entire length by the remarkably large number of bowlders which it carries. It lies in the midst of the morainic system, passing from the head of Mad River (east of Bellefontame) southwestward near Spring Hills, Mosquito Lake, St. Paris, Christiansburg, and West Charlestown, and crossing the Miami River just above Dayton. It then makes a gentle curve around the southern end of the loop, passing about 3 miles north of Germantown, and touching the villages of Farmersville, Enterprise, and West Alexandria, and the northern part of the city of Haton. From Eaton it follows the northeast side of Sevenmile Creek northward to its source near Ebenezer, and continues northwest past Brinley and Braffettsville, coming to the State line just north of the village of Whitewater, Ind. In Indiana it passes through Bethel and touches Arba, lying mainly south of the village. It crosses the Grand Rapids and Indiana Railway 2 to 4 miles south of Lynn, and comes to the Big Four Railway near Bloomingsport and continues near the line of that railway to Losantville, then passes north into Henry County, connecting near Blountsville with the correlative moraine of the East White lobe. The usual width of this member where distinct is 2 miles or less. The inner member is not so strong as the others and forms a distinct belt for only a few miles in the point of the terminal loop. Its inner border is usually sufficiently in contrast with the plains north of it to admit of mapping, but in places it passes into them by insensible gradations. The position of this inner border may be indicated approximately by lines connecting the following towns: Degraff, Quincy, Palestine, Fletcher, Troy, Harrisburg, Pyrmont, Sonora, Ithaca, and Fort Jefferson, Ohio; and 356 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Spartanburg, Snowhill, Huntsville, and Windsor, Ind. The width of the inner member, where distinct, is 2 to 3 miles, being greater than that of the middle member. RELIEF. Throughout the terminal loop the outer member of the system has a general relief of 20 to 30 feet, while its highest points rise to a height of 50 feet or more above the outer border district. It can scarcely be entered at any point from the outer border district without making a perceptible, and throughout much of the border an abrupt, rise. the relief is less easily determined, since the moraine breaks up into sharp knolls more than in the terminal loop. On the inner border the rise into the In the reentrant portions moraine is somewhat less and is also more gradual than on the outer border. The middle and inner members of this system have a relief above bordering districts nearly as great as that of the outer member, but the rise is less abrupt; they are consequently less conspicuous topographic features. RANGE IN ALTITUDE. The eastern limb of this morainic system has a range in altitude of about 850 feet, and the western limb nearly 400 feet. The rock surface has equally great range, as may be seen by the following table of altitudes: Table of altitudes along the moraine. Station. (above tide). | (above de), Feet. Feet. Wplandsieastofibelllefombtaimensaes senses eee see eae e eee eee eee 1, 350-1, 540 ; 1,150-1,400+ - igo uelSummitas sees eee secs se scree sees see ocinniciss cee meee eee 1, 540 1, 150 Westitiberty wmavalleves sss -2e ss los. Seon. eee see eae see meee 1, 100 883 Syomiaysy JBL, Gal Wylie Es. keke ee pan see abesaseEasdacabescoces a1, 150 760-1, 000 = Mosquito piake aimivalleyeace aes tes oessh sect saceee Seeeses a1, 100 ? Stabariswommiplamd siete asco. scneinsee yoace eye scene oes een 1, 238 700-870 ittlew fountain, meanst-weaniss = seso-22se a= cee ceeisseeeeeeeeeeae ee 1, 326 ? News Carlislesinuvalle ye: * 226 cast 8 Sh see Se eRe ee ee eens 883-915 ? Oshorne pinivalleyges ses Wasito- cians sees te mielayci news se eee see eeee 830 625 UplandstinieastmpantotsDay tones sass ss sees seis ee eee eee 1, 000-1, 100 | 1, 000 = IDEN, Ma WEEN? oonscaoonscace sooo nasodassescsonssssasoceucnssss- 750 525 Ganlislesinavallleyserer ee acre See sees ee ae isom esses eee see 696 500 += (Uplands southtoreGermantowms se eee =) ee eee eee a1, 000 950 + Caniden mintyalll eye cetera eral aioe Sens ey omelet eae Sern yore ate ee 839 658 Uplands in northwest Preble County, Ohio, and in Wayne and Randolph counties, Ind!--~--------- =~ - 222-222-2222 1, 175-1, 225 | 1, 050-1, 100 a Barometric. MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 307 TOPOGRAPHY. The outer member of this morainic system has, on the whole, stronger expression than the middle and inner members, but it is less plentifully supplied with bowlders. The knolls and ridges in each of the members are of characteristic morainic types. Since the eastern limb is not clearly differentiated into distinct members it may be discussed as a unit. At its northern end it is strongly morainic throughout its entire width, consisting of sharp knolls and winding ridges 10 to 59 feet in height, thickly strewn with bowlders and enclosing basins 5 to 20 feet in depth. The Hogue Summit, 2 miles east of Bellefontaine, which is reported to be the highest point in Ohio (1,540 feet above tide),* is a morainic knoll having a height of about 40 feet and covering 8 or 10 acres. Other knolls in that vicinity rise to within 20 or 25 feet of the same altitude. In southern Logan County and in Champaign, Clark, and Miami counties the features of the moraine are extremely variable. In its eastern or outer part are occasional clusters of very sharp and prominent knolls 30 to 75 feet in height, illustrations of which may be seen 3 to 4 miles northwest of West Liberty and in the vicinity of Spring Hills, also west of St. Paris and in Honey Creek Valley west of New Carlisle; but much of this eastern part is characterized by a subdued morainic topography, with knolls and ridges only 10 or 15 feet in height, among which shallow basins are inclosed, nearly the entire surface being undulatory. In the western or inner part of the eastern limb a somewhat different topography appears, knolls 10 to 25 feet in height dotting the surface of an otherwise nearly plane tract, and occupying but a small fraction of it. Basins are rare compared with the outer part of the moraine. Bowlders are very abundant both on the knolls and the plane-surfaced tracts. Where the moraine-headed terraces or gravel plains connect with the moraine, as in Mad River Valley near West Liberty, and again east of New Carlisle, on Glade and Muddy creeks near Northville, and on Nettle Creek near Millerstown, the morainic knolis come down to the gravel plains and occasionally occur like islands on them. The latter statement is especially true of the district east of New Carlisle, where morainic knolls and ridges 1See Geology of Ohio, Vol. III, p. 482. 358 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. 20 to 40 feet high occur out to distances of a mile or more in the gravel plain. They appear to have been built up at the time the gravel plain was occupied by glacial waters, having been no evidence found that they were cut into by glacial streams. However, the materials comprising the knolls are such as are subject to landslides, creeping, and rapid erosion, and it has been so long since the gravel plains were occupied by streams that erosion marks may have been obliterated. : The several members of the morainic system are sufficiently distinct. around the southern end of the loop to make it advisable to discuss them separately. The portion of the outer member lying south of Mad River, along the east bluff of the Great Miami, has greater strength than is displayed elsewhere by this member. There is im places a well-defined ridging in a north-northeast to south-southwest direction, i. e., in line with the trend of the moraine, the ridges succeeding each other at intervals of one-half mile or more and standing 15 to 30 feet above the intervening tracts. One ridge was noted, however, in which the trend was nearly east to west. It lies 24 miles north of Centerville, is about a mile in length and one-fourth mile in width. Its highest points reach an altitude of 50 to 60 feet above the bordering district. From this ridge northward to Mad River Valley the moraine has sharper knolls than it has toward the south, there being many whose height is 40 to 50 feet and whose slopes are but 20 to 30 rods in length. The outer border of the moraine in this portion of the belt is somewhat irregular, and patchy developments of morainic topography occur for a mile or more east of the main ridges. In the Great Miami Valley this moraine is very feebly developed, but in the vicinity of Carlisle low ridges occur, among which are basins and irregular depressions. On the uplands between the Great Miami and Sevenmile Creek the moraine consists of a broad basement ridge standing 20 to 40 feet above the — outer border tract and having a width of 1$ to.3 miles. On its crest and slopes are minor ridges and knolls 10 or 15 feet in height, among which sags and irregular depressious are inclosed. In Sevenmile Creek Valley the moraine is only feebly developed, but where the moraine crosses the valley a decided change in structure occurs, there being a well-defined gravel plain south of the moraine, while north of it there is scarcely any gravel, the valley of the creek being cut in till depos- MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 09 its. From Sevenmile Creek northwestward into Indiana the moraine presents a main ridge standing 15 to 30 feet above the outer border plain, on whose crest and slopes there are small knolls and ridges. The outer portion of the moraine has a uniformly undulatory surface, while the inner slope has clusters of knolls around which the surface is nearly plane. Tn northern Wayne and northeastern Henry counties, Indiana, groups of knolls occur, but at least half the surface is very gently undulating. The highest knolls are only about 25 feet in height, but some of them appear prominent because of very abrupt slopes. Returning to the Great Miami Valley and taking up the middle mem- ber, we find it crossing the stream just above Dayton; indeed, its outer border extends into the northwest portion of the city, known as Dayton View. It is well developed near the mouth of Stillwater River, where it consists of gravelly knolls rising to a height of 25 to 40 feet above the river bottoms. The moraine is feebly developed on the uplands between the Stillwater and Miami south of Chambersburg, consisting of low swells 10 feet or less in height, on which bowlders are numerous. On the highlands west of Dayton, in the vicinity of the Soldiers’ Home, the moraine has very feeble development, but southwest of these highlands, in the lowland tract south of Liberty, it is well defined, with knolls closely aggregated and thickly strewn with bowlders. The height of the knolls is slight, being but 10 or 15 feet. From this lowland tract northwestward to Ebenezer (near the State line) the moraine has scarcely any knolls exceeding 15 feet in height, and but few have sharp contour. The largest and sharpest knolls observed is a group 3 miles northwest of Eaton, which contain knolls 20 feet in height. Along the outer border are many bowlders, but the topography there is often less sharply morainic than it is a mile or so north of the bowlder belt. For several miles east of the State line and throughout much of its course in Indiana this member has a strong expression, containing knolls 25 to 30 feet in height, among which are basins and irregular depres- sions, the surface being thickly strewn with bowlders. Its expression is stronger than the portion of the outer member adjacent to it on the south The inner member of this morainic system is represented in eastern Indiana and western Ohio by irregularly grouped drift knolls of sharp con- tour, separated by wide stretches of nearly plane-surfaced drift, all liberally strewn with bowlders, though not in such numbers as the middle member. 360 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. It is very strongly developed along the valleys also, and since these valleys trend nearly at right angles with the general course of the moraine they present the appearance of spurs leading northward from the moraine. The most conspicuous of these valley belts noted leads from New Madison northward past Fort Jefferson nearly to Greenville. It includes gravel ridges which have the outline of eskers, but they are interrupted at frequent intervals and replaced by sharp morainic knolls; consequently it seems legitimate to consider them as part of the moraine. The highest knolls and ridges rise 50 to 60 feet above the bordering low ground, but the majority are but 15 to 25 feet in height. The topography from this valley-morainic belt eastward is markedly smoother than it is to the west- ward, much of it being nearly level. In this eastern district basins are usually numerous. They are small, being but 3 to 6 feet m depth, and occupy only an acre or so each. A short distance east of Fort Jefferson the inner border of the moraine turns abruptly southward and follows Millers Fork of Twin Creek, passing through Ithaca and just east of West Sonora and Euphemia. This portion of the moraine contains only low swells 10 feet or less in height, but its surface is all more or less undulatory. Near Euphemia the moraine leaves Twin Creek and bears eastward past Pyrmont and Air Hill, having in this portion of its course numerous swells 8 to 10 feet in height, which, though low as compared with those in some portions of the moraine, present a sufficiently strong contrast to the flat tracts on the north to make it easily traceable. From Air Hill the moraine passes northeastward, crossing Stillwater River near Little York. It con- sists mainly of low swells 8 to 10 feet in height, but on the west bluff of Stillwater River, about a mile northeast of Taylorsburg, a chain of sharp gravelly knolls and ridges occurs, whose highest points stand 30 to 40 feet above the bordering portions of the moraine. The chain trends with the moraine in a northeast-southwest course. In Stillwater Valley there is, near Little York, an undulatory lowland standing about 70 feet above the river, on which a slight capping of till and numerous bowlders occur, with heavy beds of gravel beneath. On the uplands between Stillwater and the Great Miami the moraine has feeble expression, with swells only 5 to 10 feet high, but is very liberally strewn with bowlders, and the bowlders also abound northward over the bordering plains. In the Great Miami Valley, just below Tippe- ————— MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 361 canoe, there are sharp, gravelly knolls and ridges varying from 10 feet up to 40 or 50 feet in height. From the Miami River northward this inner member has been described as a portion of the eastern limb of the morainic system. THICKNESS OF THE DRIFT. In the eastern limb of this morainic system the thickness of the drift has a known range from a mere trace up to 530 feet, with an average of probably 200 feet. The thickness on the uplands is greater in Cham- paign and Logan counties than farther south. The rock surface is much more uneven than the drift surface, the effect of the drift being to fill up the valleys and lowlands to about the level of the preglacial ridges. The greatest amount of drift yet penetrated in Ohio is found in an attempted gas-well boring at St. Paris, where, after penetrating to a depth of 530 feet, the well was abandoned without reaching the rock. Within 3 miles south of this well, and at about the same altitude as its mouth, a limestone quarry has been opened. The thickness of drift in the gas-well borings at De Graff ranges from 33 to 300 feet, and at Bellefontaine from a thin coating up to 150 feet. In the Great Miami Valley there may be a continuous deep channel, _ though it must be narrow, since the river in places has a rock bed, and rock is near the surface throughout much of the valley bottom. The drift in this valley has the following ascertained thickness: Near Piqua, 170 feet; at Troy, 133 feet; at Dayton, 247 feet; at Miamisburg, 181 feet; and at Hamilton, 210 feet There may be points in the valley where it is even - thicker than at Dayton. On the uplands, between the Great Miami and Sevenmile Creek, the thickness is usually between 25 and 50 feet, but in the valley of Sevenmile Creek a boring at Camden shows 180 feet, and borings near Eaton show 75 to 80 feet of drift. Between Sevenmile Creek and the State line the thickness on the uplands ranges from 30 or 40 feet up to 100 feet or more. In eastern Indiana the thickness ranges from 50 feet or less up to fully 250 feet, with an average thickness of 100 feet or more. What proportion of this drift was deposited previous to the formation of the morainic system under discussion is difficult to estimate, there being, so far as known, no widespread, well-defined soil or weathered zone separ- ating the late Wisconsin drift from the early Wisconsin. Indeed, very few 362 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. instances of buried soils have come to notice in this region. A comparison of the thickness of the drift in the district lying outside (south) of the moraines with that covered by them, leads to the conclusion that at least one-half the drift was previously deposited. This constitutes probably the | most reliable method of making an estimate. It must, however, be con- sidered a rude approximation, for it is probable that the ice sheet gathered up and redeposited a portion of the drift that it overrode. STRUCTURE OF THE DRIFT. The portions of the moraine characterized by a gently ridged or a swell-and-sag topography contain much more till than assorted material, while the sharply ridged tracts and the prominent knolls, so far as opportu- nity for examination has been afforded, contain a preponderance of assorted. material. However, there are, on the gently undulating till tracts, numer- ous places where gravel appears at the surface both in the knolls and the intervening depressions, while wells indicate that beds of assorted material are interstratified with or deposited in pockets within the till. In the sharp gravelly ridges and knolls the presence of till is not uncommon and it sometimes constitutes a considerable part of the material. While, therefore, the structure admits of division into two classes, there appear numerous abrupt changes in structure such as are characteristic of morainic deposits. An interesting section of a sharp gravel knoll on an elevated portion of the moraine may be seen 14 miles southwest of St. Paris. The knoll is elongated in an east-northeast to west-southwest direction and was originally very abrupt at its eastern end, rising within 10 to 15 rods to a height of 75 feet, while toward the west it had a gradual slope. The excavation began in the eastern end and has been carried past the highest part of the knoll, leaving only the western slope. The portion removed contained considerable well assorted sand, gravel, and cobble, but the portion remaining presents an interesting combination of beds, there being deposits of cobble, gravel, and till, intergrading with each other, which are curiously disturbed and contorted in their bedding. The gradual slope on the west side of the knoll forbids the supposition that the beds owe their disturbance and contortions to recent landslides, and leaves it probable that their form and position are due to the molding and pressure exerted by the ice sheet. Sections of lowland gravel knolls may be seen in the vicinity of New a MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. BOK) Carlisle, where an old valley, probably interglacial, is partially filled by the moraime. Near the railway station in New Carlisle there is a gravel pit in which no till appears. The gravel is in various positions—oblique, arching, and horizontal—and varies greatly in coarseness within short distances. Southeast of the station there is a cutting in which gravel and cobble appear near the top, beneath which is a yellow till 10 or 12 feet in depth, and beneath this blue till. The gravel and cobble increase in thick- ness in passing northwestward, owing to the dropping off of the till. It seems probable that the till belongs to an earlier ice advance than that which produced the gravelly hillocks that cap it, presumably the early Wisconsin. West of New Carlisle there are extensive excavations showing a large preponderance of assorted material in oblique and arching as well as horizontal attitudes. In one instance the knoll is capped by till and bowlders, while the nucleus is of assorted material. A good exposure of the structure of nearly plane-surfaced upland drift appears at the Beavertown quarries 3 to 4 miles southeast of Dayton. There is being removed here ‘about 20 feet of drift, consisting of an almost continuous capping of yellow till 5 to 10 feet in thickness, beneath which are deposits of poorly assorted gravel and sand horizontally bedded. In places these gravelly deposits reach to the limestone, but fully as often a thin bed of till mtervenes. The surface of this lower till is uneven, and the gravel rests unconformably upon it. The lower beds of gravel being horizontal, are shut off where the till rises above their level. ‘This break between the lower till and the overlying deposits may indicate a lapse of considerable time between their depositions, though it is not known but that the erosion of the surface of the lower till was rapidly accomplished by the same streams which deposited the overlying gravel and sand. A series of interesting sections of plane-surfaced lowland till appear along Twin Creek in the vicinity of Germantown, in a district lying between the outer and middle members of this morainic system. These are of especial interest, since in one locality a peat bed outcrops beneath the till. Attention was first called to the exposures just below (east of) Germantown in 1870, by Orton, who gave at that time an account of the deposits of peat beneath the till? More recently Wright” has called attention to the same deposits and added some interesting observations on the occurrence of sheets of till that perhaps mark successive advances and retreats of the 1 Am. Jour. Sci., 2d series, Vol. L, 1870, pp. 54-57. Bull. U.S. Geol. Survey No. 58, 1890, pp. 96-98. 364 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. ice sheet, and has published a photograph showing the section of drift over- lying the peat, which is here reproduced (Pl. XIV, A). In this section the peat is greatly concealed by talus from the till, but is exposed in one place up to a level several feet above the stream. Among other interesting facts, Orton called attention to the occurrence of cedar berries and fragments of coniferous wood in the peat and of undecomposed sphagnous mosses, grasses, and sedges in its uppermost layers. Beneath the peat is a gravelly deposit, in view only at the eastern or right end of the exposure, and there it is in beds which dip westward at an angle of about 30°, soon passing with the peat below the level of the creek bed. Wright remarks, concerning this deposit, that ‘‘the appearance is that of a saucer-shaped deposit of peat, such as would form in a kettle hole, and which was subsequently filled and covered over with the advance of the glacier.” At the time of the writer’s visit, in 1889, no exposure of the underlying gravel could be found, and no further data concerning it can be given than appear in the reports by Orton and by Wright. It is not evident from these descriptions whether the gravel beneath the peat is of glacial origin, though there appears to be no reason for doubting that it is, and Wright evidently so considers it. The peat appears to be in situ, since its layers are undisturbed and have a continuous outcrop for about 75 yards. It seems scarcely probable that so large a mass would sutfer removal and deposition by the ice sheet without being in a more disturbed or fragmentary condition. The drift deposits resting on the peat have a thickness of nearly 100 feet and are well exposed by the undermining action of the stream. T'Se drift presents a peculiar variation in color and also abrupt variations in structure. The exposure is nearly one-fourth of a mile in length and extends about an eighth of a mile west from the point where the peat disappears. Near its western end the following series of beds are exposed: Section of Twin Creek Bluff, near Germantown, Ohio. Feet. SWelllowatil Pee se casio sclweicot osicuie esc oee menses ciecit a4 seis Eee Senne eee 8-10 Blue till, lens-shaped in outcrop, disappearing in either direction within a few rods....-------- 0-6 Vellow hill Saeco ea Se cin. hoi to HEE cicjnites ow nde ene cs Sacn meee cece eee eee eee 6-8 Blue itil eee es rei © teste seo sepa se s Seige © clo ete sees wline See Re aon eee ee 12-15 Yellow till, local, soon passing horizontally into blue till -.-..-..........-..------..---------- 5-6 Ble xia Seesaw sacs co eioe Ste etan es noc osu are oe aac eiee a ee 10-12 Wellows tills ocaleicoonimeplaced by;sandrandorayell == = seas aa ees ee eee ne 3-4 Seine! gino areniell oe eos ocpeaseaesauese debas poneBE Doo oSooncE osm sesocoasesocsusudesencoseise 10-12 Creek bed, gravelly. otal Vaboutwessecee acces oe omic ec isceiccsiccce est yacic eke Aegee none See cee a eee ee eee 70 U. S. GEOLOGICAL SURVEY MONOGRAPH XLI PL. XIV A. SECTION OF PEAT AND TILL NEAR GERMANTOWN, OHIO. B. SECTION SHOWING WOOD INCLUDED IN TILL, 1 MILE SOUTH OF OXFORD, OHIO, MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 365 Just west of this exposure is a partial one in which gravel extends from the creek bed up to a height of nearly 40 feet, a portion of the gravel being cemented. Passing eastward, about an eighth of a mile to the place where the peat comes to view, there is a nearly solid bed of till 95 feet in height without the alternations of yellow and blue color seen in the western end of the exposure. There is at the top of the bluff 10 to 15 feet of yellow till. The remainder of the section is blue till, with the exception of occa- sional pockets or thin beds of gravel, a few inches, or at most 3 or 4 feet in thickness. Between this point and the western end of the exposure there are places where much gravel appears. The whole exposure is subject therefore to abrupt horizontal changes, and a description which will apply to one place may not apply to another 10 rods distant, the only constant bed observed being the capping of yellow till at the top of the bluff. The cause of the occurrence of yellow till at several horizons is diffi- sult to determine, especially since it is confined to a very small part of the exposure. Possibly the till was of a yellow color when deposited. There may have been four distinct ice advances, as suggested by Professor Wright, each bringing in blue till, which became oxidized at the surface, forming the yellow till. The occurrence of four such series or successions of beds in one part of the exposure and but one series in the other may perhaps be due to an accident resulting im the preservation in one place and removal in another of the yellow or oxidized portions of the earlier depositions. It seems quite as probable, however, that the oxidized portions of the till were caused by percolating waters which followed lines where the till happened to be most pervious. ; Above Germantown, along Twin Creek, there are other extensive exposures of the drift which show in places a double series of yellow and blue tills, but nowhere else within the entire district under discussion have four successive series been found. In the case of the peat at the base of the till near Germantown, there seems good reason for believing that it indicates the lapse of a considerable interval of deglaciation. Whether the interval preceded the formation of the early Wisconsin moraine or succeeded it remains to be determined. Orton calls attention ' to the occurrence of soil at considerable depth in wells in this vicinity, showing that remnants of an old buried surface are not uncommon. 1 Rept. Geol. Survey Ohio, 1869, Geology of Montgomery Co., pp. 165-167. 366 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The presence of buried oxidized tills and of sand and gravel deposits between till sheets can not, in the writer’s opinion, be cited as demonstra- tive evidence of retreats and advances of the ice sheet unless accompanied by other and more certain lines of evidence, such as peat beds or soils, leached and eroded surfaces, etc. Their occurrence seems rather a problem demanding investigation than a line of evidence from which conclusions can be drawn. In the western limb of the moraine no extensive natural exposures were observed; we pass, therefore, to the data afforded by well records, beginning the discussion at the northern end of the eastern limb of the morainic¢ loop. The following record of drift, penetrated in a gas-well boring at the Buckeye Portland Cement Works, near Harper, was furnished by G. W. Bartholomew, jr., treasurer of the company. The well mouth is about 1,260 feet above tide, and the well is situated in the valley of Rush Creek, about 1 mile east of Harper station, at the edge of a marshy tract. Section of drift beds in a gas boring near Harper, Ohio. Feet. IBWeKClay ere steers ce ceioeisin ies eee Nee apm eee ie aaa ee Se Se Pee eae eee eee eae eee 15 Gravel (water stood 7 feet below well mouth) ............-.--.--.------+------2+-+-+------------ 20 Clay cetera enei st season sess ts< SoS sists oss Se sleet sees eee ee ae ee eee eee se ees 20 GravelN(wateristoodilosteetia bowie swellsrmo tla) ee ee ee ee ee a ree 10 Clay eis wei Satis einele a2 ai arse Ss emcis SORES S| Se re cm ee cate Se SEO ra ee ake ate Se 20 Gravell(water)stood 17 tect above welll mouth) 2222525 = e228 ===) 5 eee eon eee 95 Yellowish and brown bowlder clay (probably Illinoian) -........-..-..--.-.-..--:--.-----.---- 65 Helderberg limestone at 245 feet. Bartholomew reports that a well for water was bored about a mile north of this gas well. It penetrated 100 feet of drift before reaching a’ water-bearing gravel, thus presenting a marked contrast to the upper 100 feet in the gas well. On the bordering uplands the rock surface reaches in places an altitude of 1,400 feet, or nearly 500 feet above the rock floor in Rush Creek Valley. A well for water at Benjamin Easton’s, near the Hogue Summit, east of Bellefontaine, is reported by the driller, J. A. Hartzler, of Bellefontaine, to have penetrated 350 feet of drift, of which the upper 60 or 70 feet is largely gravel, while the remainder is mainly blue till. No Devonian shale was encountered, the first rock being the Helderberg limestone. The alti- tude of the well mouth is about 50 feet below that of the Hogue Summit, or 1,490 feet above tide. The well was not a success in the yield of water, MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 367 and only a short piece of projecting pipe marks its position; but it is of much scientific value in that it indicates that the supposed highest point in Ohio is in a region of very heavy drift deposits, and, since it carries an unusual amount of drift, owes its great height only in part to a high altitude of the rock surface. Hartzler reports other wells in the neighborhood of Bellefontaine which show large amounts of drift, as follows: At Mr. Kaston’s, 1$ miles south of Bellefontaine, a well 140 feet deep penetrated ordinary till about 120 feet, then a red clay, very hard and dry, 20 feet, beneath which water-bearing sand was struck, from which bits of wood were pumped up. In a well on Charles Scott’s farm, on the hill north of West Liberty, wood was encoun- tered in a red, sandy clay at a depth of 160 to 170 feet, after a thick bed of blue till had been passed through. The well terminates in gravel at a depth of 200 teet. Just above the water-bearing gravel there is a bed of blue bowlder clay. The altitude of the well mouth is about 1,200 feet. A well at Mrs. Dille’s, 4 miles south of Bellefontaine, penetrated 93 feet of drift, mainly gravel, and at that depth entered limestone. A well near Spring Hili, on the farm of Daniel 8. Corey, penetrated 390 feet of drift, the ereatest amount yet found by Hartzler. The following succession of beds was passed through, as given from memory, but the exact thickness of each bed was not remembered: Section of Corey well near Spring Hill, Ohio. Feet Gravel Wabouteaee sae seat sacs = tent eee oe Sette sieeic ee manna Samana as cee a meete eee 90 Bluegill ewatherhinbedshotassontedsmatenial=aeeeeee sees se ee eee ree Heese erase eee eee 200 Rediclaya(atabouts20—o40eeh) tatscac case tee riste qaceis ese -ecelstiecl- See acres see see ceees 20 IBIS GEW/s s5e6 csccasbsecaescspesoeeuoeronses asaudtossaL seasooeeaesosdeneeuaHesanesosuaseor 30-40 Green and red clays resting on the rock. The wells in Bellefontaine made in prospecting for natural gas have the following amounts of drift, as reported by Dr. Covington, of that city: Thickness of drift in Bellefontaine gas borings. Feet. Carter’s well, three-fourths mile south of court-house..........---..----.---------.------------ 95 Well on Huntsville road, 1 mile northwest of court-house---.--.----------...------_.--._--....- 50 Wielliwestofaraillwaygstatlony sexes er ae sae oes sicies eic woe sere a= =e ise Mee eee ns Sere ee 150 In the vicinity of the Ludlow survey line, at a distance of 4 or 5 miles south from Bellefontaine, the rock rises to the surface in prominent portions of the uplands, and it also lies near the surface just north of Bellefontaine at altitudes much aboye the level of the railway station. > 368 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Three wells in Degraff, made in prospecting for gas, have the following amounts of drift: Thickness of drift in Degraff gas borings. Feet, Lippincott well, one-half mile north of railway station ------.-------.--- so teeeesgsrageeteesee 300 Harris well, one-fourth mile west of railway station ........--..-.-.--------------------------- 33 Renel welll, Gaeta mole Werdiloer WeEsic scossnssosoceSsa ne ass se esacesSesosgesce zosessssssesscse 86 A well for water at H. A. Hill’s, 2 miles north of West Liberty, pene- trated 18 or 20 feet of till and then entered gravel, in which it continued to a depth of 87 feet. Several other wells near Hill’s have a depth of 60 feet or more and do not strike rock. At John Newell’s, in section 10, Union Township, about 3 miles north- west of West Liberty, a well penetrated about 150 feet of drift, nearly all till, and struck no rock. In West Liberty a prospect drilling for gas pene- trated 216 feet of drift, striking rock at an altitude less than 900 feet above tide. At St. Paris a gas-well boring was attempted near the station at an altitude about 1,216 feet above tide, which penetrated 530 feet of drift, and was abandoned without reaching rock. Orton has called attention’ to the occurrence of a tough brown clay at a depth of 360 feet, the section above that depth being mainly blue and gray tills. At 400 feet gravel was struck in which, as reported to Orton, wood, bark, and fragments of mussel shells were struck. Dr. J. J. Musson, a resident of St. Paris, informed the writer that the report that mussel shells were pumped out from this depth seems based only on the Paleozoic fossils which are found in some of the pebbles. Fragments of the wood were preserved and pronounced to be red cedar. Beneath the gravel which contained this wood quicksand of some depth was passed through, but the well terminated in bowlder clay. Orton sug- gested that this deeply filled valley was the ancient channel of the Miami River, but the exact course of the valley southward from this point remains undetermined. It is also doubtful if it had a southward discharge, there being some evidence of a channel leading northwestward into Indiana. Toward the north a valley of similar depth has been struck at Port Jefferson, Anna, New Bremen, and near St. Marys, and it has recently been traced by Bownocker into Indiana.” No surface indications of the position of the channel are to be found, 1 Geology of Ohio, Vol. VI, 1888, p. 277. 2 Am. Geologist, Vol. X XIII, 1899, p. 182. ———————————— se — ee MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 369 for the drift has filled that whole region to a level above the tops of the highest limestone ridges of the preglacial divides. The data concerning the wells referred to are presented later, in connection with the discussion of the region in which they occur. A well in St. Paris, 80 rods northwest of the one reported above, struck rock at 370 feet, but no data concerning the character of the drift were obtained. At Troy the drift has a known variation from 50 to 133 feet in thickness. At New Carlisle a large amount of drift was penetrated, but the writer was unable to learn its exact thickness and structure. The uplands north of New Carlisle, for a distance of 10 miles or more, are thinly coated with drift, and so also are those south of this village between Honey Creek and Mad River. West of the Miami River, also, the drift is thin from Troy southward to Dayton. Some of the wells west of Tippecanoe on the uplands strike a dark-colored clay, perhaps a soil, just above the rock. In Tippecanoe water wells penetrate 30 feet or more of till. Below Tippecanoe, in the vicinity of Tadmor, there are lowland tracts along the Miami River, where tributaries enter from the uplands, in which 50 to 75 feet of till is exposed. , The greater part of the city of Dayton stands on a gravel plain, but in the portion west of the Miami, known as Dayton View, the drift has an undulating surface, and, though mainly composed of gravel, has a capping of till thickly set with bowlders. A gas-well boring near the corner: of First and Findlay streets penetrated 247 feet of drift, mainly till. A well on the waterworks grounds near Mad River, 225 feet in depth, did not reach the rock. This penetrated clayey deposits (probably alluvial) for about 50 feet, beneath which depth the drift was mainly gravel. The supply of water for the city is obtained from a series of wells which barely enter the gravel _ beneath the alluvial clays. At Osborne, a village on Mad River, a few miles above Dayton, drift was penetrated to a depth of 207 feet, but its structure was not learned. At Miamisburg a portion of the valley has rock near the level of the river bed, but a gas-well boring made in that village penetrated 181 feet of drift, mainly gravel. The deep portion of the valley lying below the level of the stream here seems to be a narrow gorge. The valley above stream level is somewhat constricted for 2 to 3 niles below Miamisburg, though it is probably of preglacial excavation. MON XLI D4 370 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. From the Great Miami westward along the terminal portions of the morainic loops and northward along the western limb of these moraines the drift is much thinner than in the eastern limb, and contains a larger proportion of till. The majority of the wells are mainly through till, penetrating but little assorted material, though the water-bearig bed at bottom is usually gravel or sand. On the road from Dayton to Chambers- burg the wells located on the middle moraine penetrate 30 to 40 feet or more of drift, but north of that moraine in the village of Chambersburg they penetrate but 6 to 15 feet. West from Dayton, in the vicinity of the Soldiers’ Home, and northwestward from there in the district lying between the middle and inner members of the morainic system, rock is near the surface; but in the moraines to the north and south the drift has a thickness of 30 to 40 feet or more, and in Stillwater Valley near Little York its thickness exceeds 100 feet. Along the lower course of Twin Creek, as previously described, the drift is exposed to a depth of nearly 100 feet, but in its upper course there are many quarries along the stream, and the amount of drift filling is slight. In the outer border of the morainic system 3 miles southwest of Germantown, on an elevated portion of the uplands, a well on the “‘Anderson farm” is reported to have penetrated bowlder clay nearly 100 feet without reaching rock. This is the greatest thickness of upland drift reported from this portion of western Ohio. At Pyrmont (on the inner member) wells 50 feet deep do not reach rock. At Wengertown, West Baltimore, and Gordon, villages situated on the border of the inner member, wells 30 feet deep do not reach rock. At Ithaca, on the inner member, rock is struck at about 25 feet. Flowing wells are obtained along a small creek in this village at a depth of about 15 feet. At Arcanum, near the border of the inner member, one gas well has only 22 feet of drift, but five others have 50 to 55 feet. There is in this village 10 to 20 feet of till at the surface, beneath which the drift is largely sand and gravel. At Eaton the waterworks well in Sevenmile Creek Valley, in the north- west part of the town, penetrates 75 to 80 feet of drift, mainly till, but in the southern part rock is struck in the valley at about 10 feet. There may, however, be a deep gorge traversing the valley southward, which has not yet been touched in wells. At Camden, about 8 miles below Eaton, the drift in this creek valley has a thickness of 181 feet. MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 371 At New Madison there are outcrops of rock in the valley of White- water River, but the gas well, which is also in the valley, penetrated 75 feet of drift. The only records of deep wells obtained in the Indiana portion of this moraine are at Lynn and Losantville. In Lynn one gas well has 117 feet, the other 124 feet of drift. In each well there is about 50 feet of till at the surface, beneath which the drift is mainly gravel. In Losantville the drift has a thickness of 240 feet, the greater part of which is blue till. Some gravel beds were passed through within the upper 100 feet. BOWLDERS. Frequent references have already been made to the large number of bowlders which characterize the middle member of this morainic system. Reports by earlier observers, Orton, Hussey, Chamberlin, and Phinney. contain descriptions of portions of the belt,' and Chamberlin recognized it as an accompaniment of a moraine of the Miami lobe There are few, if any, bowlder belts within the drift-covered portion of the Mississippi Basin which exceed it in strength and extent of development There is scarcely a mile along the whole length of the morainic loop, from the northern end of the eastern limb in central Logan County, Ohio, around to the northern end of the western limb in Henry County, Ind. (a distance of about 120 miles), in which bowlders are not a conspicuous feature. The belt has an average breadth of more than a mile, not including the eastern limb, in which its breadth is much greater, averaging 2 to 3 miles. The bowlders are much more plentiful in some localities than in others. An estimate made from an actual count of the bowlders at several points gives an average of about ten surface bowlders per acre whose size exceeds 1 foot in diameter. Professor Orton noted a field near West Alexandria, in Preble County, where by actual count there are over 1,200 bowlders per acre which exceed 2 feet in diameter. The aggregate number in any portion of the western limb is probably as great as in an equal length of the eastern limb, since the bowlders are dropped in greater numbers per unit of area in the former than in the latter situation. The size of the bowlders ranges from:a cubic foot or less up to 1,000 1B. Orton, Geology of Ohio, Vol. III, 1878, pp. 412-414; John Hussey, Geology of Ohio, Vol. III, 1878, pp. 475-476; T. OC. Chamberlin, Third Ann. Rept. U. S. Geol. Survey, pp. 334-335; A. J. Phinney, Fifteenth Ann. Rept. Geol. Survey Indiana, 1885-1886, pp. 112-115. ol2 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. cubic feet or more, but the majority contain only 10 to 20 cubic feet. They are largely granitic rocks and fine-grained greenstones, but quartzites and conglomerates from the Huronian ledges of Canada are also common. Very few limestone or local bowlders of any kind oceur. The vast majority of the bowlders are partially rounded or subangular, but scarcely one in one hundred shows glacial planing. They lie on the surface, or are but slightly embedded in the ground. From accounts given by residents it appears that very few are struck in making wells or other excavations except within a foot or so of the surface. The large proportion of crys- tallme Canadian rocks, the slight amount of glacial planing, and the restriction of the bowlders to the surface, individually as well as unitedly, indicate that the bowlders were englacial, becoming superglacial at the border rather than subglacial; but the underlying drift appears to be largely subglacial, being composed of thoroughly intermixed local and distant material whose rock fragments are much more conspicuously gla- ciated than are the surface bowlders. If this interpretation be correct, the amount of englacial material was very slight compared with that of the subglacial. This bowlder belt continues beyond the limits of the Miami lobe at each end, being traceable southwestward along the eastern limb of a moraine of the Kast White lobe some 12 to 15 miles, when it loses its strength and can with difficulty be traced farther. In the Scioto moraines, as noted elsewhere in this report, bowlders are present from the reentrant angle in Logan County southward for 30 miles or more in greater abun- dance than throughout the remainder of the loop, but not in such great numbers as in the Miami lobe. If these continuations of the bowlders into the Scioto and East White lobe be included, the length of the bowlder belt will be increased to about 160 miles. There appears to be no reason for separating the bowlders in the other lobes from those in the Miami lobe. Indeed, they seem to have been deposited at the same time and serve a valuable purpose in indicating the correlations of the moraine. The outer member of this morainic system has comparatively few bowlders on its surface, the only points where noteworthy numbers were 1Comp. Chamberlin: Third Ann. Rept. U. S. Geol. Survey, pp. 331-332; Am. Jour. Sci., May, 1884, pp. 378-390; Bull. Geol. Soc. America, Vol. I, pp. 27-28; Jour. Geol., Vol. I, pp. 47-60. Upham: Am. Geologist, Vol. VIII, Dec., 1891, pp. 376-385; Bull. Geol. Soc. America, Vol. III, pp. 134-148. Salisbury: Am. Geologist, Vol. IX, May, 1892, pp. 304-316. MAIN MORAINIC SYSTEM OF THE MIAMI LOBE. 343 observed beg southeast of Dayton, in the vicinity of Beavertown, and south and southwest of Germantown, but in neither of these places do they compare in number with those in the main belt. On the immer member the distribution of bowlders is somewhat irreeu- lar. The eastern limb is liberally strewn with them throughout its entire length, though they are not so numerous as in the bowlder belt of the middle member. The terminal portion of the loop and the western limb are sparingly supplied with bowlders, but have small areas in which the number is as great as in the main belt. . There are parts of the inner border plain on which bowlders are as numerous as anywhere in the main bowlder belt. The most conspicuous of these tracts les along the Stillwater River, the bowlders occurring abundantly along this stream for several miles below Ludlow Falls and also on the plains east of the stream along a line running from West Milton to Troy. Over an area of several square miles they are so thickly strewn that stone wall fences are made from them and they form a serious hindrance to the cultivation of the soil. The entire district embraced between the morainic system under discussion and the next moraine to the north is plentifully supplied with bowlders, scarcely a farm being free from them, but they seldom so greatly interfere with agriculture as they do about Ludlow Falls. These bowlders probably represent englacial mate- rial dropped during the recession of the ice sheet. So far as the writer could discover, they do not form belts that can be correlated into well- defined systems or lines and are not so suitable as moraines for showing the outline of the ice margin. , CHARACTER OF THE OUTWASH. In this discussion the deposits of the valley of Mad River will first be considered, after which the valleys to the west will be taken in turn. Mad River finds its source in the reentrant angle between the Scioto and Miami lobes, at an altitude about 1,250 feet above tide. There is not such deep gravel filling here as at points lower down in the valley. The village of Zanesville ‘is located in the valley about 2 miles below the head of the river, and it is reported that the gravel has here a depth of but 12 to 20 feet, the remainder of the drift to a depth of 120 feet being mainly clay. The surface of the valley bottom at Zanesville is nearly plane and has the 374 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. appearance of a glacial gravel plain. Tributary plains enter near this vil- lage from the Scioto moraine on the east, and the valley soon becomes broader, having in Champaign County a width of 2 to 3 miles. The pres- ent stream has cut but a shallow channel in the upper half of its course and in flood seasons still overflows the bed of the glacial stream, though it has here, as throughout its entire course, an average fall of about 9 feet per mile. The moraine comes down to the border of this plain west of West Liberty, and probably glacial waters issued from it at this point into the Mad River Valley. About 6 miles below West Liberty a gravel plain enters the valley from the northwest. It is nearly a mile in average width, and extends fully 3 miles back into the moraine. At its northwest end this tributary gravel plain grades into and fits about the morainic knolls, showing that it is of the same age as the moraine. The plain is traversed by two streams, Muddy and Crayon creeks, whose beds are only 12 to 15 feet below the level of the plain. One of these streams enters from the north and the other from the southwest side of the gravel plain, and they take parallel courses through it, being distant from each other one-half mile or more. The size of their valleys compared with that of the plain which they enter is an indication of the small amount of work they have accomplished com- pared with that accomplished by the glacial stream which formed the gravel plain. A few miles farther south, and nearly opposite Urbana, another tribu- tary glacial gravel plain enters Mad River Valley from the west. This plain is 80 to 160 rods in width, and is traversed by Nettle Creek, the source of the stream being near the head of the gravel plain. It lies in a valley which is continued farther west, and into which the moraine descends at the head of the gravel plain, there forming the divide between Mosquito Creek, a tributary of the Great Miami, and Nettle Creek, a tributary of Mad River. The peculiar features here produced by the ice sheet merit a brief description. The moraine consists of a series of gravelly hummocks, rising only 10 to 20 feet above the level of the head of the gravel plain, which occupy the valley for less than one-half mile, and into which the gravel plain merges as if it had been formed in connection with them. The same knolls stand about 60 feet above the level of Mosquito Lake, a lake which forms the head of Mosquito Creek, the stream leading northwest OUTWASH OF THE MIAMI LOBE. SD from the moraine. The ice sheet apparently occupied the northwestern end of the valley while its waters were filling the portion of the valley outside the ice with gravelly deposits, and withdrew without fillmg up the portion of the valley which lay beneath it to as high a level as the glacial waters had filled that outside. Near Springfield the present Mad River enters a narrow rock-bound valley for a few miles, but emerges near Snyder’s station into a broad plain several miles in width. he plain extends on the northwest nearly to New Carlisle, where it connects with a gravel outwash or apron of the moraine. Here we find phenomena similar to those just described in the Mosquito- Nettle Creek Valley. From the outer border of the moraine there is a plain descending southward to Mad River, while on the inner border is the valley of Honey~ Creek leading northwestward to the Great Miami, the highest poit between the two rivers being at the junction of the moraine with the gravel plain near New Carlisle. From the expanded portion of the gravel plain under consideration a valley leads southward to the Little Miami River. It is occupied through- out its entire length by Beaver Creek, the head of the-creek being in the Mad River gravel plain and the mouth at the Little Miami. It is much smaller than Mad River Valley, its width near Byron and also near its mouth being but 60 to 80 rods. This valley was probably occupied by a stream at the time of the highest stages of the waters which formed the Mad River plain, but seems on account of its small size not to have carried the main stream for any great length of time. The valley may be older than the Mad River gravel plain, though it was apparently somewhat enlarged at the time that plain was occupied by glacial waters. About 4 miles west from the point where Beaver Creek Valley leaves the Mad River gravel plain, the river enters the outer member of the morainic system under discussion. It joins the Great Miami at Dayton, and that stream passes southward along the inner border of the outer member and leaves the moraine about 25 miles below the point where Mad River entered it, its course throughout much of that distance being about 3 miles back from the outer border of the moraine. This extension of the ice sheet beyond the valleys of Mad and Miami rivers raises some interest- ing questions. Did this bridging of the valleys by the ice sheet produce an obstruction or dam sufficiently strong to prevent the waters of Mad River 316 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. from following their present course? And if a dam was produced, was it maintained continuously throughout the entire period during which the outer member of the morainic system was forming? That the ice sheet occupied this portion of the valley for a considera- ble period is shown by the strength of the portion of the moraine developed along the southeast side of the valley, and that it would, while occupying the moraine, present a serious obstruction to the flow of a stream along the valley can scarcely be doubted, especially since the course of the stream did not conform to the direction of ice movement but was almost at right angles to it. The open valley (Beaver Creek), leading southward from the Mad River plain to the Little Miami, to which attention has already been directed, may have been utilized because of an obstruction to the flow of the water down the valley. The obstruction may have been complete for a brief period, but that it was not complete for the entire period required in the formation of the moraine seems to be shown both by the small size of the outlet through Beaver Creek Valley and by terraces along Mad and Miami rivers. The portion of the Mad-Miami Valley under discussion is occupied by a broad gravel plain similar to that along the upper portion of Mad River and much broader than that along the portion of the Great Miami above the mouth of Mad River. This plain has, so far as the writer could detect, no trace of morainic features on it where the moraine crosses Mad River above Dayton, and no well-defined morainic features at the point where it crosses the Great Miami below Dayton, the only peculiarity of the plain at the latter place being a series of channels and slight undula- tions doubtfully referred to glacial action. So far as noted, the Mad River plain has no terraces above the point where the moraine crosses that are not present below that point. Indeed, there seems to be but one broad and well-sustained plain higher than the present flood plain either above or below the pomt where the moraine crosses, and this has a general elevation of 30 to 40 feet above the river. The great size of the gravel plain in the vicinity of Dayton, when contrasted with the narrowness of the Beaver Creek Valley, supports strongly the view that this portion of the valley afforded a passage for the stream throughout much of the time the moraine was forming. Mad River Valley was occupied by glacial waters only in the periods during which the outer and middle members of the morainic system were eee ee ea OUTWASH OF THE MIAMI LOBE. Be forming, the position of the inner member being such that water from it could not have been discharged down the valley; and of the two periods the earlier one seems to have furnished nearly all the glacial material to the valley, the glacial terraces leading into the valley being more numerous and also more capacious from the outer than from the middle member. The Great Miami, above the mouth of Mad River, has a much nar- rower valley than below, or than the valley of Mad River itself, the general width being one-half mile or less. In the vicinity of Troy it is, for a few miles, expanded to a width of a mile or more, and contains a gravel plain standing about 20 feet above the river, on the borders of which there is a terrace or remnant of a higher plain standing 30 to 35 feet above the river. It is thought that this higher plan may have been connected with the ice sheet at the time the mmer member of this morainic system was forming, but the connection is not clearly established. The lower plain appears also to be of glacial age, and apparently finds its head in the Union moraine, a few miles above Piqua. A description of it is given in connection with that moraine. Below the point where the outer member crosses the Great Miami (near Carlisle) that stream flows through a gravel plain, 1 to 3 miles wide, which, throughout much of its length, stands less than 50 feet above the river, but which near the mouth attains a height of 100 feet above the river owing to the more rapid descent of the present stream. Attention was called on a preceding page to the presence of a buried soil beneath this plain, a few miles below Hamilton, at a depth of about 60 feet. It is thought that the valley received an average filling of at least that amount at the time these moraines were forming, as a result of the overburdened condition of the glacial floods. That the stream which deposited this mate- rial was vigorous is shown by the coarseness of the deposit, the greater part of the material being clean gravel, with a general freedom from silty or fine material such as would have been deposited under slack-water conditions. There is a small gravel apron along the outer border of the outer member on the uplands east of the Great Miami, at an altitude about 200 feet above the river, which is crossed by the Springboro and Dayton pike nearly due east of Miamisburg. It is situated in a narrow plane tract lying between the moraine and some limestone ridges to the southeast, and forms 378 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. a divide, the waters from the northeast part of the apron flowing north- ward to enter the Great Miami near Alexandersville, while that from the southwestern part flows southwestward along the outer border of the moraine, entering the Great Miami near Franklin. On Isaac Miller's farm a well on this apron penetrated gravel of medium coarseness to a depth of 17 feet, where water was obtained. It is Mr. Miller’s opimion that the gravelly phase of this outwash apron does not extend much beyond his farm, but that the remainder of the plain is underlain by clay or silt, and has a black mucky soil. The gravelly portion of the apron has a red loamy soil. On the uplands between the Great Miami and Sevenmile Creek there is also a small outwash apron. It covers 2 or 3 square miles in the vicinity of West Elkton. Its altitude is about 200 feet above Sevenmile Creek and still more above the Great Miami Valley. It occupies a part of the divide between these streams, its eastern portion draining southeast to the Great Miami below Middletown, while its western portion drains to Sevenmile Creek near Collinsville. Exposures near the border of the moraine show well-rounded clean gravel of medium coarseness, which has a variable thickness, owing to the irregularities of the substrata, but its own surface is quite smooth. The valley of Sevenmile Creek contains gravel terraces which are thought to be of the age of the outer member of this morainic system, but the connection was not clearly worked out. The valley of this creek con- tains till as well as gravel below the point where the moraine crosses, the till being capped by a coating of gravel several feet in thickness. Above the point where the outer member crosses there is far less gravel than below, the outwash from the later members being chiefly sand or silt. This valley has been deepened but little since the gravel terraces were formed, their surfaces throughout much of the lower part of the valley being only 30 or 40 feet above the present stream, while the bluffs bordering the glacial terrace rise to a height of 200 feet or more above it. On the uplands west of Sevenmile Creek there is, in the vicinity of the State line, an extensive till plain just outside the outer member of this morainic system, whose surface on the border of the moraine is capped by a silt deposit 1 or 2 feet in thickness which appears to be a morainic out- wash. The extent of the silt deposit was not determined, though it is ee ee OUTWASH OF THE MIAMI LOBE. d719 known to be absent from portions of the plain a few miles distant from the border, and quite uniformly present near the border of the moraine. The plain occupies a part of the divide between the Whitewater and Great Miami rivers, and stands much above the level of the gravel terraces in these valleys. The presence of gravel terraces in the valleys is evidence of high altitude and good drainage, and, assuming the silts to be of the same age as the terraces, it is evident that the conditions of slack drainage under which they were deposited is not attributable to a low altitude of the country. It seems mstead to be due to the absence of drainage channels adequate to connect the plain with these valleys. This interpretation naturally raises the question whether the silts which cap the Ilimoian drift sheet in the district outside the outer Wisconsin moraine were also formed when the country was sufficiently high to afford good drainage had channels been opened. Were these older silts contined to poorly drained portions of the uplands, they might be very inconclusive evidence of a low altitude of the country, but since they cover, as well, districts which would have had good drainage were the altitude high, and districts where no known obstruction to drainage could have existed, their presence is considered conclusive evidence of low altitude. Several of the tributaries of Whitewater River, in Wayne County, Ind., carry gravel plains which apparently find ther head in this moraine system. The head of the plain on Kast Fork is found in the middle member near the point where it crosses the State line, the Ohio portion of the valley being occupied by drift hillocks, while the Indiana portion carries a smooth plain underlain by gravel. On Nolands and Greens forks there are broad plains from the outer member southward and somewhat narrower plains extending up to the middle member. It is probable that the main gravel fillmg occurred while the ice sheet was forming the outer member. On Martindale Fork the gravel plain finds its head at the outer member nearly due east of Hagerstown. The plain along this stream is much broader near its head than a few miles below, its width at the head being a mile or more. This plain is called the ‘‘ Walnut level,” on account of the level surface and the walnut timber which occupies it. On the west fork there is only a narrow plain, that stream having been a less important glacial outlet than Martindale Fork. With the exception of East Fork, all the tributaries of Whitewater are 80 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. flowing in valleys that are usually deeply filled with gravel. There is, however, occasionally considerable till beneath the gravel. East Fork has in places but a small amount of drift, for it is largely in a new course opened since the early Wisconsin stage of glaciation. At Richmond the stream has eut about 50 feet into the rock, while the depth of rock excavation is still greater farther south. The other tributaries of Whitewater have for many miles south from the moraine shallow valleys, their beds being but 15 to 30 feet below the glacial terraces. It is probable that the Whitewater Valley received important contribu- tions of glacial gravel throughout its entire length at the time this morainic system was forming, for the feeders are numerous and the valley has a rapid descent, there being in the gravel terraces a fall of nearly 500 feet between their heads and the mouth of the stream, a distance of about 75 miles. It is not certain whether the terraces formed at the early Wisconsin stage rise at any point above the level of the gravel filling which accompanied the glacial stage under discussion. STRIZ. Thirteen observations of strize have been made, or have come to the writer’s notice within the limits of this moraine and its inner border plain. With two exceptions these are all in the eastern portion of the district. With three exceptions they bear either directly or obliquely toward the eastern limb, the exceptions being found near Piqua, where the bearing is nearly due south and in western Darke County, where the bearing is slightly west of south. Strize are rare in the western portion of the morainic loop, several rock outcrops having been examined, both within the western limb and on the inner border plain, without success in finding striation.- The following is a list of the observations. The bearings obtained by the writer and probably those by other observers have not been corrected for magnetic variation. Striv in the vicinity of the main morainic system. Nave) Ms) GPOENAALES| tial SMOG noon wa eoanobo asso sana Ses dono sssescoscdsoecesecseee ce S. 10° E. SUAS Geis, iy, wails! sowie Git INGE oo ece ence Sdosacacdes slaocat be secennlon cess N.-S. Zinn’s quarry, 3 miles northeast of New Carlisle, near outer border of moraine.....-.------- ish Zo Ie Ay ROMINA, I Taille WREST Oi VALINE GWEN Soo 5kose p65 5k sos cosecnsocsoncedslecesolcesenene S. 80° E. Troy, 6 miles southeast of, on east-west center road in Elizabeth Township.-...........--- 8. 25° KE. Troy,e2 miles}southyot soni weshibluitof Great Maamie == 282-425 92 5s te ee S. 28° E. Light’s quarry, Dayton, 6 miles north of, east bluff of Great Miami!__..........___.._- S. 19°-33° E. ‘Reported by Dr. John Locke, Geology of Ohio, 1838, pp. 230-232, fig. 2. ee et INNER BORDER OF THE MIAMI LOBE. 381 Dayton, 4 miles southeast of, in Beavertown quarries!............-.....---.--.--.-.------ Sse 27/2 1d Liberty, 1! mile northeast of, on west bluff of Great Miami_...-....-..-.....-.------.----- S. 28° EB. iberhyaromatll es mOnvhnOhe mer seercica ae so oa wie scan anos goals sons melee AeA eee Sees §. 28° HE. INecanmWwiesia vin tonweasoluiuolstillwatern River =a. 22 4-62. 2525 5055s 8 ees ee eee S. 30° E. (Candusra Ualnyamm call Gree mivillll Gian acres ese cee yale ineva cy tse ,= eta §. 5° W. Weavers station, Darke County”. .........---.---------- Be Se ee ase es ea S. 5° W. INNER BORDER PHENOMENA. The district lying between this morainic system and the next moraine to the north varies in width from 20 miles in the axis to a narrow neck with a width of 5 miles or less near the borders of the lobe. It has throughout nearly its entire extent a very smooth surface. Along portions of the valleys, however, a few drift knolls of large size occur. The valley of Mosquito Creek, which enters the Great Miami near Sidney, contains several very sharp knolls 50 to 75 feet high; smaller ones are found in the Miami Valley in the vicinity of Piqua and between Piqua and Troy, and there are other belts along tributaries of White River in Indiana. These valley knolls form chains nearly at right angles with the course of the moraine, and since they are comprised largely of gravel it is thought that they may have been formed by subglacial streams in their passage toward the ice margin, and are, perhaps, to be classed as imperfect eskers. The surface of the upland, as remarked above, is liberally strewn with bowlders, and in places they form a conspicuous feature. The drift consists largely of till, and owing to the irregularities of the underlying rock surface presents much variation in thickness, as shown below. The gas-well bormg at Port Jefferson, in the Great Miami Valley, 5 miles above Sidney, penetrated about 300 feet of drift, but in the same valley, from Sidney southward, rock exposures are numerous up to a level within 50 or 75 feet of the bordering uplands. At Piqua there are quarries in the valley, but a well at Mr. Wiley’s, 14 miles north of the city, extends to a level nearly 150 feet below the river bed without reaching rock, and one at Joseph Sawyer’s, on the bluff in the west part of the city, strikes rock at a level fully 100 feet below the river bed. The well driller, J. M. Stoker, of Piqua, reports that Wiley’s well was in gravelly material for about 30 feet, beneath which 140 feet of blue till was penetrated. In Sawyer’s well 8 or 10 feet of yellow till was succeeded by about 20 feet 1The main bearing is 8. 26° E. Orton’s map, Geology of Ohio, Vol. I, p. 413, indicates strize in that vicinity bearing 8. 18° E. * Geology of Ohio, Vol. III, p. 501. 382 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. of gravel, beneath which there was blue till extending to the rock, which was struck at a depth of 190 feet. On the uplands borderimg Stillwater River the drift seldom exceeds 50 feet, and is, in places, 10 feet or less in thickness, while along the river there are rocky bluffs with scarcely a break throughout the entire course of the stream through this plain. Toward the west the thickness of the drift increases, borings near Union City having 60 to 200 feet or more, while those west and south of Winchester, Ind., show a range from 80 to 333 feet. In wells in the vicinity of Union City the drift contains but little assorted material, and the same is true in the majority of those near Winchester. The boring near Winchester (about 14 miles west), in which 333 feet of drift was penetrated, passed through a large amount of quicksand. The Lockport (Niagara) limestone, which covers nearly the whole of the elevated portion of eastern Indiana, was absent in this well and also in one north of it, on the north side of White River. In the latter well also there was more than 300 feet of drift. SECTION II. IN THE SCIOTO LOBE. THE MEMBERS OF THE SYSTEM. DISTRIBUTION. This main morainic system connects definitely with that of the Miami lobe on the uplands of Logan County and also with a similar morainice system of the Grand River lobe. There are perhaps some advantages in setting forth the distribution in the reverse order from that here presented; but, as originally prepared, this part of the Monograph dealing with the Scioto lobe was intended to be published as a separate bulletin of the Survey; and since it would mvolve a practical rewriting of the paper to reverse the order of presentation, the old order has been retained. This morainic system, as shown in the glacial maps (Pls. II and XIII), connects on the northeast with the western limb of the outer moraine of the Grand River glacial lobe, forming with it an interlobate belt which occupies much of Stark County and extends northward through eastern Summit and western Portage counties to a later morainic system, which continues the interlobate tract into Geauga County. 2 MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 383 From southern Stark County the morainie system under discussion swings abruptly westward, and between there and Mansfield covers a tract 8 to 14 miles wide, the greatest width being in the vicinity of Killbuck Creek, where it is separated into three somewhat distinct belts with inter- vening tracts 2 miles or more in width, in which morainie features are rare. Immediately west of Mansfield the whole system swings abruptly southward. Its breadth for a few miles along the western border of the highland tract of Richland County is but 5 or 6 miles, but south of this tract it spreads out, the main belt continuing southward, while a some- what distinct outer moraine passes eastward along the south border of the highlands nearly to Mohican Creek at Greersville, where it also tums southward. At this eastern point it is separated by an interval of but 4 miles from the outer portion of the moraine that lies north of these highlands. Where this eastern member of the belt swings southward (near Greers- ville), the breadth covered by the whole morainic system is fully 25 miles, but the strongly morainic features are found mainly within the western half. There is scarcely a square mile, however, on the eastern half of the belt which does not contain drift knolls of rather sharp contour. Apparently the eastern portion was occupied by the ice sheet for a much briefer period than the western, the drift being thinner as well as less closely aggregated into knolls and ridges. From this point of greatest expansion the eastern and western mem- bers converge, the breadth of the system decreasing toward the south to about 16 miles, in the latitude of Newark, and 13 or 14 miles at the Licking reservoir, and southward from there to Lancaster. The system consists, near Lancaster, of three distinct members, separated from each other by intervals of 2 to 3 miles,in which morainic features are rare. Throughout this north-to-south portion of the eastern limb of the Scioto - lobe one member, the inner or western, is maintained distinctly and has a breadth ranging from 4 up to 10 miles. The remainder of the system is made up of two more or less distinct members, whose variations in width and strength are great, as shown in Pl. XIII. Near Lancaster the morainic system shifts abruptly westward a few miles, producing the appearance of a shoulder or slight lobation north of the city, after which it trends west of south to the Scioto River, the inner 384 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. member coming to that stream near Circleville and the outer some 14 miles farther south. West from the Scioto River for 15 miles or more the morainic system leads over a hilly district and morainic features have an interrupted devel- opment, the inner member, which east of the Scioto is everywhere strong, becoming here vaguely defined; but in western Ross County the morainic system again shows distinct members, four of them being readily traced northwestward from this county. The cuter one follows the southwest side of Rattlesnake Creek across northeastern Highland County. Leaving this creek, it continues northwest- ward through Clinton and northward through eastern Greene County, con- stituting the divide between tributaries of the Scioto and Little Miami rivers. Continuing north, it enters the Miami drainage area in Clark County, and is distinctly traceable about to the latitude of Springfield, where it becomes difficult to trace because of its close association with later members of the system. ‘Uhis belt is the one whose course is outlined by Professor Cham- berlin in the Third Annual Report. Its breadth is about 2 miles, and it is clearly distinguishable, by its prominent morainic features, from the nearly plane tracts on either side. The second member of the system follows the northeast side of Rat- tlesnake Creek from its mouth to its source and determines the course of that stream. It becomes merged with later belts in southeastern Clark County. Its width is scarcely a mile, but throughout its entire length it presents sharp knolls and ridges that produce a strong contrast with border- ing plane tracts. The third member passes from Roxabell, in Ross County, in a course north of west, lying mainly south of the Dayton and Southeastern Railway, to Paint Creek, which it crosses between Washington and the mouth of Sugar Creek. From Washington its course is northward along the east side of Sugar Creek to the source of that stream, and thence a few miles north in conjunction with the member west of it. It then becomes merged (near the latitude of Sprmegfield and London) with the remaining members of the system. This member has a general width of about 2 miles. The fourth member follows the southwest side of North Paint Creek for a few miles in northwestern Ross and southeastern Fayette counties. It leaves that stream near the line of the Cincinnati and Muskingum Valley MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 385 Railway, and passes northwestward to Bloomingburg. From that village it passes northward along the east side of a tributary of Paint Creek to its source near Midway, and continuing north passes the Madison County infirmary, 3 or + miles west of London, near which it becomes merged with earlier members. Its breadth is a mile or more. Reference is made to this belt by Chamberlin in his paper in the Third Annual Report. The combined moraines pass northward through northeastern Clark, eastern Champaign, and southeastern Logan counties, constituting a belt 6 to 9 miles wide, the width decreasing northward. Near Bellefontaine it connects with the main morainic system of the Miami lobe, as already indicated (pp. 354, 382). RANGE IN ALTITUDE. From the northern end of the interlobate tract on its eastern margin, westward to the meridian of Wooster and Millersburg, the moraine has few points that exceed 1,300 feet above tide, and none that fall below 800 feet. A change of altitude of 250 feet is frequently made, however, within a distance of 1§ to 2 miles in passing from ridges to valleys. In Killbuck Valley, between Wooster and Millersburg, the moraine is lower than at any other part of this shoulder of the lobe, being but little more than 800 feet above tide. The hills near this creek are capped by drift ridges of morainic type at an altitude of fully 1,100 feet. Near Mansfield, on high points 2 or 3 miles southwest of the city, drift knolls occur at an altitude of 1,490 feet (barometric). The principal valleys in that vicinity are 1,100 to 1,150 feet, making the range in altitude within short distances about 350 feet. In the eastern limb of the main lobe the strongest part of the moraine occupies the divide between the Scioto and the Muskingum and Hocking drainage systems, but owing to the hilly character of the region the range in altitude is not slight. There are parts of the Hocking and Licking valleys where the altitude is but little more than 800 feet above tide, while on neighboring hills it is 1,100 to 1,200 feet or more. In many places changes of altitude of 250 to 300 feet occur within a mile or two. In the Scioto Valley and the lower portion of Paint Creek Valley morainic features are developed at an altitude as low as 700 feet above tide, while on neighboring hills north of Paint Creek they occur at an altitude of 1,150 feet. In the western limb the outer member follows so nearly the water MON XLI 25 386 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. parting between the Miami and Scioto drainage basins that it has no large valleys to cross, and as the district is not so hilly as on the east border of the lobe no abrupt changes in altitude occur. There is, however, a gradual increase in altitude in passing from south to north, the altitude in western Ross and northwestern Highland counties bemg about 1,100 feet and in eastern Logan County 1,400 to 1,500 feet. The other members of the morainic system show about the same range in altitude as the outer one, the altitude of the eastern member being about 900 feet at the line of Ross and Fayette counties and 1,300 feet or more im Logan County. This member of the moraine may perhaps include the highest pomts in Logan County and reach an altitude of 1,500 feet above tide, for it is possible that the ice sheet extended to these high points down to the time this member was forming. RELIEF. Tn each of the several members of the western limb the outer border is abrupt and quite marked, though usually but 20 to 30 feet in height; but on their inner border the moraines blend into the plains so gradually that there is no marked relief. The portion of this western limb in which the moraines are not distinct ridges (in Logan and Champaign counties) stands in places 200 feet above the valley of Mad River, which in Logan County follows its outer border, but this relief is due in part to an under- lying rock ridge, the thickness of the drift of the moraine being less than 200 feet. ‘There is in this portion of the moraine an inner border relief nearly as great as is the outer, which is also due in large part to its location on the rock ridge. The eastern limb of the main lobe is not so distinctly ridged as the western. ‘The member that follows the water parting has a higher altitude than the remainder of, the system, but this is due to a rock ridge rather than to increase in thickness of drift, though the drift in this member is considerably thicker than in the members or portions of the morainic system east of it, and the rock ridge is interrupted by notable gaps which have been completely filled with drift. In the shoulder east of Mansfield the thickness of the drift in the moraine is, on the whole, markedly greater than on the tract northeast of it, but so much variation exists that the amount can hardly be estimated. The interlobate tract, though as a rule more heavily covered with drift than the MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 387 district west of it, does not possess a marked relief. This is due to its being heaped up in irregular accumulations instead of in the form of a definite ridge. TOPOGRAPHY. The height, degree of sharpness, closeness of aggregation, form, and trend of the knolls and ridges which constitute this morainic system, vary greatly, both in the pronouncedly morainic and in the more vaguely defined portions of the belt. In general, however, it may be said that the system consists of rather small but well-defined knolls and ridges somewhat closely aggregated. ‘The height of knolls and ridges usually falls below 20 feet, though instances were noted where it becomes as great as 75 feet. A knoll 20 feet in height covers usually 2 acres or more, though it occasion- ally occupies a much smaller area. The prevailing form is a somewhat symmetrical cone, but in association with knolls of this form there are hillocks with irregular or hummocky surface, and ridges with various form and trend. Basins are not common except in the interlobate portions, and even there they are not conspicuous. In the interlobate belt formed at the junction of the Scioto and Grand River lobes, there are several basins a square mile, more or less, in area, which are occupied by small lakes. The most prominent of these are the Twin Lakes, near Earlville, in Portage County, and Springfield, Summit, Long, Turkeyfoot, and Mud lakes in Summit County. Of these, all except Springfield Lake lie in gravel plains whose general level is but a few feet higher than the surface of the water, but Springfield Lake is bordered on all sides by prominent moraine hillocks. The portion of the interlobate tract lying north of the bend of the Cuyahoga was formed, in part at least, in conjunction with a later series of moraines in connection with which it will be discussed. South of the bend of the Cuyahoga, the interlobate moraine lies mainly east of the meridian of Akron, and is so closely associated with the western limb of the main Grand River morainic system that no distinct line of separation could be found. A lime drawn directly from the point of separation near Canton, northward past Kent, passes through a goodly number of small gravel plains situated among the moraine hillocks, and these features appear to be the natural results of a junction of ice lobes, while the strize on either side of this line indicate clearly a movement from 388 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. opposite directions toward it, those on the west being eastward and south- eastward, while those on the east are westward and southwestward. But in the course of the formation of the interlobate tract, the line of junction between the lobes (or their individual margins in case no junction was effected) may have shifted back and forth to a distance of several miles. On the assumption that this is the line of junction, there remains a belt 5 or 6 miles wide west of this lime, which is sharply morainic. The knolls seldom exceed 60 feet and are usually scarcely 30 feet in height, but they have, as a rule, very sharp contours. West of this strong belt there is a gravel plain one-half mile or more in width, which runs from the bend of the Cuyahoga southward through Akron to Turkeyfoot Lake. On its western border there is a feeble morainic belt in which basins are a prominent feature. Some basins 20 feet or more in depth have an area of scarcely one-half acre each. This moraine is well exhibited from the west part of Akron northward along the west bluff of Little Cuyahoga River and also west of New Portage. Its width is a mile ‘or less. West of this is another gravel plain called Ayer Flats, which is 1 to 1$ miles wide and runs southward several miles from near the forks of the Cuyahoga to the Tuscarawas, its southern end bemg known as Copley Marsh. This gravel plain was apparently a line of outwash from the outer member of a later series of moraines which crosses the Cuyahoga near the bend below the mouth of the Little Cuyahoga. From a few miles north of Canton a narrow outer belt continues nearly south to the Tuscarawas Valley just above Bolivar, while the main belt turns southwestward, crossing the Tuscarawas above Massillon. The outer belt has some prominent knolls near Canton 50 to 75 feet in height, but as a rule its knolls fall below 20 feet. They are seldom so closely aggregated as in the united belt farther north. This outer belt apparently forms the glacial boundary and shows an interesting irregularity of outline on its outer border, there being in nearly every valley or lowland tract. a projection of the moraine beyond the line on the bordering hills, the amount of projection being in some cases a mile or more. This is well shown on the road from Canton to Bolivar, where scarcely a trace of drift appears on the uplands, while in the valleys drift abounds in sharply outlined knolls and ridges which rise abruptly 10 to 15 feet. A similar irregularity of border was noted farther west along the road leading from Wiensburg through Berlin to —— — MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 389 Millersburg. The freshness of contour of this outer member is such as to denote that it is not much older than the other members of the morainic system. The main member, which crosses the Tuscarawas Valley above Massillon, consists of closely aggregated, sharp knolls, 20 to 50 feet high, among which are occasional basins. The morainic topography west of the Tuscarawas is much weaker in expression than it is east of that stream, the knolls from the Tuscarawas westward to Killbuck Creek being usually but 10 to 15 feet high, and less closely aggregated and gentler in slope than in the interlobate tract. On Pl. XIII, two, and, in places, three, members of the morainic system are indicated as crossing from the Tuscarawas to Killbuek Valley; but it should not be understood that the belts have a clearly defined line of separation; there is simply a comparative scarcity of drift knolls in the portions indicated as nonmorainic. On Sugar Creek Valley there is, toward the south from the glacial boundary at Beach City, a well-defined gravel plain or terrace, standing about 35 feet above the stream, while toward the north the valley is oceu- pied by morainic knolls of gravelly constitution, and terracing is not well exhibited. The terrace here appears, therefore, to connect with the outer member of the morainic system. The knolls at the head of the terrace are small, 5 to 10 feet in height, but farther north rise in some cases to a height of 20 to 25 feet. In Killbuck Creek Valley there is at the glacial boundary a morainic accumulation, fillmg it up to a height of 75 to 100 feet or more, whose surface is gently undulatory, having knolls only 10 to 30 feet in height. South from the glacial boundary is a plane-surfaced terrace standing about 70 feet above the creek. Wright called attention to this terrace in his paper on the glacial boundary in Ohio, in the followig words: The terraces upon the Killbuck are extensive both above and below the glacial limit. One mile and a half below Millersburg, on the west side, on the farm of A. Uhl, is a terrace about a quarter of a mile wide, containing kame-like ridges and knolls, the surface of which is 102 feet above the flood plain. This gradually rises until it is merged in the till of the hills beyond. Two miles farther south, in the northwest corner of Mechanic township, near Stuart Mills, the terrace is composed of finer material and is level-topped, and gradually descends toward the south, being here but 70 feet above the flood plain.’ 1G. F. Wright: The Glacial Boundary in Ohio, Indiana, and Kentucky, 1884, pp. 45, 46. 390 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. It will be observed that the gravelly knolls in the valley, as well as the level-topped gravel deposits, are included by Professor Wright in the terrace. In the writer’s description the terrace is considered to have its head where the level-topped gravel deposit begins. The gravelly knolls are included in the moraine, since they owe their existence largely to the mechanical agency of the ice sheet, like portions of the moraine on the uplands. With this in mind the reader will find no difficulty in harmonizing the two descriptions. — The moraine fills the valley for a couple of miles north from the glacial boundary. There is_then an interval of 3 miles or so where the valley is comparatively open, and is bordered by a low plain nearly one-half mile in width. Near Holmesville this low plain rises into a gravel terrace, and about three-quarters of a mile north of that village the terrace heads in the middle member of the morainic system. At its head it stands 35 or 40 feet above the creek. It is well displayed on the east side of the valley. In the western portion of the valley there is a low plain which has no connection with the middle member, but passes entirely through it and also through the inner member, the middle and inner members extending down to the borders of the plain on either side of the valley. The width of the plain is nowhere less than one-fourth mile, and in the vicinity of Wooster it expands to a mile or more. It was occupied by glacial waters at a later date than the time when this morainic system was being formed, probably while the ice margin stood near the continental divide. The inner member crosses the valley 2 to 4 miles below Wooster, but no terrace was dis- covered in connection with it. The morainic knolls in this valley seldom exceed 30 feet in height, and more commonly are but 10 to 15 feet. Between Killbuck Creek and Lake Fork of Mohican Creek there are, near the southern border of the drift, large dome-shaped hills, 50 to 100 feet in height, covermg 20 to 40 acres or more each, which probably contain in every case a nucleus of sandstone, but whose outline is markedly in con- trast with that of unglaciated hills near them on the south. In one large hill, about a mile south of Nashville, the north slope was smoothed, like its neighbors, by the ice sheet, while the south side remains rough, like hills in the unglaciated district, and is covered by immense detached masses of sandstone. The drift knolls in this district are but 10 to 20 feet high. They present fresh contours out to the very borders of the glaciated district. pis & GL MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. a9! No indication of an attenuated sheet of drift was noted south of this outer member. In the middle member of the morainic system, near the line of the Pittsburg, Fort Wayne and Chicago Railway and between the villages of Lakeville and Shreve, the morainic knolls are somewhat larger, but none exceeding 40 feet in height were observed. A few basins occur among the knolls. The northern member is well exhibited a few miles north of this railway, in the vicinity of Springville, and thence westward to Lake Fork. The several members become combined near Lake Fork, and it is probable that for a few miles west from that stream the middle member has overriden the outer, for the knolls south, southeast, and west from Loudonville have a size and sharpness somewhat greater than the outer member usually displays, their height being often 30 feet or more, and that, too, at altitudes fully 1,100 feet above tide. Some basins occur among the knolls where closely aggregated. These features are more common on the middle than on the outer member. In the valley of Lake Fork there is a terrace standing at the glacial boundary about 100 feet above the creek. At Greersville, 4 miles south of the glacial boundary, it has a height of only 75 feet, and at Gann, 4 miles farther south, its height is not more than 60 feet. Upon following up Lake Fork from the glacial boundary one soon finds knolls at an altitude lower than the terrace. For several miles the high terrace appears at intervals along the border of the valley, while in the midst of the valley, at consider- ably lower levels, there is a knob-and-basin topography. The basins cover several acres and the centers are depressed 10 to 15 feet or more below their rims. Their bottoms are peaty and marshy, and therefore presumably filled to some depth. They are surrounded by knolls of various sizes, form, and trend, while near them at the border of the valley are level-topped gravel deposits standing 50 feet or more above the general level of the morainie tracts in the valley. Phenomena somewhat similar to these are displayed in several valleys in northwestern Pennsylvania just above the glacial boundary, and may be common in other parts of the glaciated district. Their cause is not well understood, but it is thought that they are probably due to the lingering of an ice mass in the central portion of the valley after a passage for the escape of water from beneath the ice had been opened along the borders of the valleys. The ice sheet may have been broken up and the terraces formed around its detached masses, 392 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. or it may have been comparatively unbroken, but traversed by tunnels in which the terraces were built up. About 5 miles north of the glacial boundary a remnant of the high terrace was noted, which was bordered by a low sag on the side next the bluff, resembling somewhat the sag which so often accompanies the esker ridges. Phenomena such as these may serve as a connecting link between the eskers, which are probably sub- glacial, and moraine-headed terraces which, having their origin at the ice margin, are extraglacial. The morainic features and the high, level-topped terraces both disappear somewhat abruptly near the north border of the moraine, and the valley for some miles above has a low, nearly smooth, plain but little higher than the stream. From this it appears that the ice sheet at the late Wisconsin invasion deposited but little material in this valley except at its margin, a feature not uncommon in other valleys of northeastern Ohio and northwestern Pennsylvania. On the uplands bordering Lake Fork the sharpest knolls and ridges are found near the southern border, there bemg in the northern portion gentle till swells but 10 to 20 feet high. The moraine is exceptionally strong from Lake Fork westward past Loudonville and Perrysville to the vicinity of Lucas. In a lowland tract south and west of Perrysville numerous knolls and ridges rise abruptly to a height of 30 to 50 feet, and among them landlocked basins occur. It is probable, as indicated in Chapter II, that Clear Fork and Black Fork had, in preglacial times, a course north of the present one, from the lowland tract near Perrysville eastward, near the lme of the Pittsburg, Fort Wayne and Chicago Railroad, past Loudonville to Lake Fork, as a lowland tract there occurs a mile or more in width, deeply filled with drift, while the present streams are in narrow, rock-bound valleys for several miles above their junction with Lake Fork. This lowland tract is now occupied by a strong morainic belt. East from the reentrant angle near Mansfield the moraine for several miles is weak compared with its strength on the west side of the reentrant angle, or compared with its strength a few miles farther east. It is repre- sented by scattering drift knolls and occasional low ridges whose height seldom exceeds 20 feet. The strize east of this reentrant angle, near Wind- sor and Mifflin, instead of bearing west of south toward the moraine, bear southeastward, approaching it at an oblique angle, a fact which strengthens MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 393 the view that this portion of the district is a shoulder rather than a distinct lobe. By this interpretation the moraine here in its weakly developed por- tion is lateral rather than terminal. Farther east the striz bear southward or at right angles to the moraine, so that the moraine is there terminal in its position, and its strength is greater than where lateral. West of the reentrant angle, near Lexington and Iberia, striae bear obliquely toward the moraine, but it is nevertheless strong, the movement in the main lobe being more vigorous than that on the shoulder. The variations in the strength and direction of ice movement seem therefore to afford ample cause for such variations in the strength of the moraine as are displayed. In the midst of the elevated district lying southeast of Mansfield there is a small tract known as Chestnut Ridge, on which careful search along several routes failed to disclose any drift. It takes the form of a narrow neck about 3 miles in width and 10 or 12 miles in length, which extends from Mohican Creek, just above Greersville, westward nearly to Independ- ence. Its altitude is scarcely 100 feet greater than that of districts border- ing it on the north and south, bemg about 1,400 feet above tide, and it is somewhat lower than drift-covered hills lymg northwest of it, which in some cases reach an altitude about 1,500 feet above tide. These hills to the northwest, however, are not heavily glaciated, the drift being but a few feet in thickness, and showing little tendency to aggregation in knolls. Around ‘this tract of thin drift curves the moraine under discussion, the trend being from south of east to north of west on its north side, north to south on its west side, and north of west to south of east along its south side. On the meridian of Mansfield the distance from the portion of the moraine on the north to that on the south of this tract of thin drift is 10 or 12 miles; but on the meridian of Perrysville, 10 miles east of Mansfield, the distance is but 5 or 6 miles, and at the Mohican Creek it is scarcely 4 miles. The space is so narrow in this eastern portion that Wright and Wooster each connected morainic features on the south with those on the north. Thus, Wright carried the glacial boundary from near Greersville northward to the mouth of Lake Fork along the west side of Mohican Creek,’ and Wooster carried the moraine from Fredericktown direct to Perrysville.* Taking into consideration the bearing of the strize, the position of the thin 1See Glacial Boundary in Ohio, by G. F. Wright, 1884. *See map (Pl. XXXI) accompanying Chamberlin’s paper in Third Annual Report, U. 8. Geol. Survey, 1883. o04 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. drift. tract, and then the course of the morainic belts bordering them on the north, west, and south, there seems reason for concluding that the ice cur- rents parted a few miles northwest of this elevated district, one portion of the ice passing southeastward along the northern side of the highlands, while the other passed nearly south along the western side, and then swung eastward, doubling about the southern side. A cause for this parting of currents and winding of the ice sheet 1s found in the obstruction presented by this highland tract, whose highest points stood 200 feet or more above the general elevation of the districts north and south of it, the highlands being 1,400 to 1,500 feet above tide, while the bordering tracts are 1,200 to 1,300 feet. The ice sheet seems to have overridden the highest hills, but not to have had sufficient force to continue beyond them, while the stronger currents on the lower lands, both to the north and the south, continued east- ward, and by their convergence nearly coalesced east of these highlands. Though partially overridden by the ice sheet, the highlands seem not to have been subjected to so long nor so vigorous glaciation as the lower tracts that surround them. Northwest and west from Mansfield the moraine consists of closely aggregated knolls 15 to 20 feet, more or less, in height. Near Lexington the knolls occasionally reach a height of 30 feet or more. Basins are numerous in the vicinity of that village on the lowland tracts bordering Clear Fork. Several were observed which have an area of about an acre and a depth of 15 or 20 feet. They occupy a gravel plain which stands 40 or 50 feet above the stream. This gravel plain constitutes the head of a terrace, and is of importance, since it apparently indicates that the ice margin, at the time the main moraine was forming, was as far west as Lexington. Instead of crossmg Clear Fork 20 miles southeast of Mansfield, as interpreted by the earlier students, it seems more probable that it crossed the stream 6 miles southwest of that city. The knolls near Fredericktown, just referred to, are in chains which have a northwest-southeast trend, following nearly the course of the West Fork of Owl Creek. They constitute the border of the moraine that sweeps around the western end of the belt of thin drift whose outline was given above, and they lie several miles east of the main morainic belt. Their contours are sharp, and the larger ones rise abruptly to a height of 25 or 30 feet. his member of the morainic series appears to continue directly east es, MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 390 from Fredericktown, there being just south from North Liberty and Jelloway a series of drift knolls and drift ridges 10 to 20 feet high. Eastward from North Liberty the drift knolls set in at the very border of the high ridge that seems to be driftless, but westward from this village there is an outlying belt of thin drift. As noted above, the morainic features within the tract lying between the main moraine and the glacial boundary south of the — abrupt turn in the boundary are not so clearly outlined as in the main moraine, yet scarcely a square mile occurs which does not contain drift knolls of rather sharp contour. The whole may perhaps be considered a morainic tract formed during the brief space in which there was lobation on the south border of the nearly driftless highland. In presenting morainic features it differs from the tract with thin drift which lies on the border of the highland, there being in the latter little or no aggregation in knolls or ridges. Between Mount Vernon and Newark the moraine presents marked differences in topography. For 5 or 6 miles, perhaps more, on its western border it has closely aggregated knolls and ridges constituting a con- tinuous, well-defined moraine. ast of this main belt the knolls and ridges of drift are very unequally distributed, there being areas of a square mile or more where drift knolls are as closely aggregated as in the main belt; but equally extensive tracts appear which have very few knolls. No decided differences in age were detected between the main moraine and the knolls of the district east of it; on the contrary, the one seems to be a close successor of the other. The eastern part of the moraine shows strong development from Mount Vernon southward as far as Utica along the east side of the Baltimore and Ohio Railway; also about the Licking reservoir south of Newark, and south from there -to Pleasantville. The knolls in these situations, though no higher than in bordering tracts, are more closely ageregated and consequently give stronger expression to the belt. They are ordinarily but 10 to 25 feet in height, are usually conical in form, and have gentle slopes. In the vicinity of the Licking Valley, both to the northeast and south- west of Newark, the drift is aggregated in knolls even where it fails to form a continuous sheet, many of the elevated hills and ridges showing scarcely a trace of drift, while the lowland tracts among them are dotted with drift knolls. In the district northeast of Newark these features are displayed to 396 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. advantage along the direct road from Newark to Wilkins Run, and thence to St. Louisville, and in the district southeast along the road from Newark to Linnville, and thence west along the National road to the valley of South Fork. There is a lowland tract, lying northeast of Newark, with a general elevation about 100 feet above the Licking River, which Wright refers to in his paper on the glacial boundary (p. 53) as a terrace. It is, however, dotted by drift knolls 10 to 20 feet in height, among which shallow basins are inclosed, the whole aspect being morainic. In structure also it resembles a moraine rather than a river terrace, since it contains much till and its assorted material is frequently disposed in arching or inclined attitudes. On the north side of the Licking Valley, just east of Newark, is a less elevated lowland than that just described, standing about 40 feet above the river. It has slight surface inequalities, but they are perhaps attributable to fluvial action, and being made up almost entirely of gravel, the name terrace is probably applicable. There are also in this portion of the valley two smooth- surfaced gravel terraces, standing about 30 feet and 20 feet above the river, the lower one constituting the plain upon which the business portion of Newark is built. On each of the several forks of the Licking, which unite at Newark, terraces occur at heights of 40 feet or less above the streams. On the South Fork the head of the upper terrace is about 3 miles south- west of Newark. where the valley is crossed in a north-northwest to south- southeast course by a moraine. On the Middle and North forks the terraces are well displayed for a few miles above Newark, but were not traced to their heads. A low gravel plain several miles in extent lies in the angle between the three forks of Licking River west of Newark, and carries occa- sional low drift knolls. These knolls were apparently formed at the time the gravel plain was being built up, and are thought to indicate that the head of the gravel plain was built up as a submarginal deposit to about its present height before the ice sheet had withdrawn from over it. The morainic system is, on the whole, stronger northward than it is southward from Newark. Not only are the belts broader, but the knolls and ridges are sharper. South from the latitude of Newark the western or main member is only 3 to 5 miles in width, and with the exception of an occasional large gravelly knoll, the height of its swells and ridges falls below 25 feet. They are, however, closely aggregated, rendering the belt readily distinguishable from bordering plains. The eastern portion of the morainic MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 307 system is feebler and the aggregation less close than in the western, the majority of knolls are but 8 to 10 feet in height. In portions of Ross County, however, the outer belt is strong, especially between Adelphi and Hopetown, where the moraine swings westward to the Scioto Valley. The larger knolls there are commonly 20 to 40 feet high, and associated with them are numerous lower ones. Some near Hopetown, noted by Wrigit, are about 100 feet in height. They are, in fact, short gravelly ridges, with a trend nearly at right angles with the course of the moraine, and may be allied to eskers. Several large gravelly ridges occur on the west side of the Scioto between Paint Creek and North Paint Creek about midway between Chillicothe and Frankfort. These ridges interlock and inclose deep basins. Their height is in some instances 150 to 175 feet above lowland tracts east of them, but scarcely half that above their western bases, which are on a hillside slope. The terraces and gravel plains along the Scioto River from Circleville southward seem to pertain chiefly to the inner member of this morainie system. A gravelly tract several miles in width, known as the Pickaway Plains, leads down the river from Circleville. It is dotted here and there by drift knolls and ridges of considerable size, and in many places its sur- face is gently undulatory, but fully one-half the district presents a plane surface. Its variations in topography are probably due to the combined effect of an overhanging ice sheet and a discharge of water from the melting ice. The plane portions of this gravelly area vary somewhat in their height above the Scioto, being about 40 feet in the vicinity of Circleville, while 8 or 10 miles below they are fully 50 feet. This difference is not due to an increase in the altitude of the gravel plain, but to a greater rate of fall of the river, there being a fall of about 50 feet in the stream between Circleville and Chillicothe, a distance of but 18 miles in direct line. The occasional drift knolls on the gravel plain apparently indicate that the ice margin overhung the Scioto Valley for at least 10 miles below Cirele- ville at the time the later moraine was forming. ‘The terraces along the Scioto are discussed on a subsequent page. The morainic features among the hills of western Ross County are variable. Some of the larger knolls have already been referred to, ‘There are others in the valley of Paint Creek whose height reaches 100 feet or more, and others in a group near Lattas are equally high. Aside trom these 398 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. large knolls, the height commonly falls below 25 feet. Drift knolls 10 to 15 feet high occur on the elevated tract east of Lattas, in the vicinity of the Greenfield and Chillicothe pike, but such features are not common on the high ridges, the sharply defined morainic knolls in this vicinity being confined mainly to lowlands and valleys. Of the four members that appear in the southwest portion of this morainic system, the outermost one is by far the strongest. Along Paint Creek, near the mouths of Rocky Fork and Rattlesnake Creek, and thence up the west side of Rattlesnake Creek for several miles, this member is characterized by numerous large, gravelly knolls, many of which are 30 to AQ) feet, and a few 75 to 100 feet in height, while among them are many smaller ones. The aggregation is close and the contours are sharp, so that an exceptionally rugged topography is presented. From northern Highland County northward large knolls are infrequent, but closely aggre- gated knolls and ridges 10 to 25 feet or more in height occur. Besides having these minor ridges and knolls, the moraine carries a basement ridge with well-defined relief of 20 to 30 feet, so that one standing at the base of the knolls is somewhat above the outer border plain. The outer members of this series display generally a ridge with well-defined crest on which the small knolls and ridges are deposited. The height of these knolls seldom exceeds 25 feet and is commonly only 10 to 15 feet, but they are so closely agoregated as to make the belt conspicuous. The intervening tracts between the several members are plane or very gently undulating, with scarcely a knoll worthy of notice. At their northern ends these several members do not at once form a bold moraine, but for a space of 10 miles or so the features are rather more subdued than in the separate members. But in northeastern Clark County the moraine assumes greater prominence, and from there northward through Champaign and Logan counties it exhibits as strong and characteristic morainic features as anywhere in its course. There are winding and inter- locking ridges ranging in height from 10 feet up to 75 feet or even more, among which numerous basins are inclosed. The slopes of the larger knolls are frequently dotted with small knolls and ridges, and carry an occasional basin. Near Mechanicsburg the moraine rises abruptly on its eastern border to the unusual height of 75 or 100 feet, and.a series of ridges whose height is 30 to 50 feet and whose contours are exceedingly sharp, lead MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 399 northeast from this village for a distance of about 3 miles. The ridges are somewhat disjointed, but at least two well-defined chains exist. These ridges terminate abruptly, but at the northern end of the eastern one is a network of lower ridges, closing a small lake. From here the inner (eastern) border of the moraine is shifted 2 miles or more westward, there being a very flat tract toward the north. The moraine west of the plane tract just noted consists of a massive ridge with north-south trend, which has on its crest and slopes a series of knolls and ridges of varying shape, size, and degree of sharpness. The highest rise 30 to 40 feet above their immediate borders, but the ridge on which they are situated has also some variation in altitude, so that in following the crest oscillations of 150 feet or more are in places made within a distance of 2 miles. From the passes, or lower portions of the ridge, gravel plains lead westward into Mad River and Buck Creek val- leys, joining the main stream that drained the Scioto and Miami lobes. The most prominent of these tributary gravel streams noted are the following, beginning at the south: (1) On a tributary of Buck Creek, through which the Big Four Railway passes from Mechaniesburg to Catawba station; (2) on a tributary of Buck Creek west and north of Mutual; (3) on a tributary of Mad River from Cables westward; (4) on a tributary of Mad River from Mingo westward; (5) on Mackocheek Creek; (6) Mormon Bottoms, east of Zanesfield; (7) Hadley Bottoms, northeast of Zanesfield. In each of these tributary plains there appears to have been an out- wash of gravel from the ice sheet, and an escape of waters to the Mad River plain. From the crest of the moraine, which forms the water parting in these passes, there was vigorous drainage westward, producing a flat- bottomed valley, while eastward the streams flow among morainic swells until they reach the till plain east of the moraine. This district affords excellent opportunities for studying the phenomena of glacial drainage as well as of glacial deposition. STRUCTURE AND THICKNESS OF THE DRIFT. A comparison of numerous slight exposures, such as the region affords, makes evident the fact that the sharply morainic tracts have a larger pro- portion of assorted material than have those with subdued expression. ‘The knolls which are composed entirely of till have usually gentle slopes. Those which contain gravel and sand with the till may have gentle slopes 400 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. but are more likely to be sharp in contour. The large sharp knolls, 75 to 100 feet in height, are almost wholly, while those from 75 down to 30 feet are mainly, composed of gravel and sand. This relation between the form and structure is not an exceptional one confined to this particular morainic system, but a common one in nearly all the moraines yet examined between Wisconsin and New York. The list of well sections given below serves to bring out a second fact, namely, that the thick deposits of drift in the valleys contain a larger pro- portion of sand and gravel than deposits of similar thickness on the uplands. This is generally true not only of the morainic tracts, but also of plains between the moraines. It is not uncommon to find a surface deposit of till on uplands and valleys alike, while the substrata in the valleys are assorted material, and those on the uplands are till. This relation between the structure of drift in valleys and that on uplands seems to have wide prevalence in hilly portions of the glaciated districts. Among several causes which may have been operative in producing the phenomena are the following: First, streams flowing from the ice sheet as it made its earliest invasion would, under favorable conditions, deposit much assorted material in the valleys in advance of the ice sheet; second, during oscillatory retreats the ice sheet would be withdrawn somewhat from the valleys, and the assorted material would then, under favorable conditions, be added to the portions outside the ice sheet; third, while the ice was occupying the hilly districts it may have molded itself so imperfectly to the irregularities of the surface as to have left comparatively free passage for waters beneath it along the principal valleys. In the cases cited, where valleys would probably receive contributions of assorted material, the uplands would not be likely to have received such contributions, and it is scarcely probable that an ice sheet under conditions of free drainage, such as the Scioto lobe seems to have had when this morainic system was forming, could do other- wise than fill the valleys with assorted material before the deposition of till . had fairly begun. When the valleys became so filled as to greatly impede the flow cf water the subglacial drainage would be checked and till would be deposited in the valleys as well as on the uplands. To what extent the valleys were filled at the earlier invasions (lowan, Ilinoian, Kansan and pre- Kansan) is not clearly determined, though the amount was probably great. In the detailed account of well sections and other exposures of the drift given below, the districts are taken in the following order: (1) The inter- Ea MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 40] lobate tract east of the shoulder; (2) the portion of the moraine on the shoulder; (3) the eastern limb of the main lobe; (4) the western limb of the main lobe. } INTERLOBATE TRACT EAST OF THE SHOULDER. As the portion of this interlobate tract that lies north of the bend of the Cuyahoga was being occupied by the ice sheet at the time when a later series of moraines was forming, the discussion of its structure is deferred, only the portion of the moraine that lies between the bend of the Cuyahoga, near Akron, and the glacial boundary at Canton being taken up here. In the interlobate tract between the bend of the Cuyahoga and Canton sections showing clayey till are rare, the drift being of a very stony character, not only in the knolls and ridges but in the lower tracts among them. The stony drift is in places poorly assorted, and apparently represents a slightly modified till from which the clayey ingredient is largely removed. In the Cuyahoga and Little Cuyahoga valleys there are extensive exposures of an exceedingly fine silt or sand forming the main body of the bluffs. It shows distinct Imes of bedding, which are usually horizontal but which arch slightly in places or exhibit signs of disturbance. A few pebbles and very rarely a large stone may be found embedded in the sand. The silt is slightly calcareous, and contains in places nodules of carbonate of lime and crystals of sulphate of lime. It is decidedly ferruginous, there being in its upper or oxidized portion numerous balls of iron oxide and thin horizontal bands of iron following lines of bedding. The upper 10 to 15 feet, and occasionally as great a depth as 40 or 50 feet, is of a yellow color, the tints of which are somewhat variable, depending upon the staining by iron. At greater depth it is of a nearly uniform blue color, like the ordinary blue till. Exposures of it 100 feet or more in height occur in the northwest part of Akron, along the Valley Railway, and at numerous points between Akron and Cleveland. Borings show a similar silt below gravel at Summit Lake and Clinton, and at a deep well near Portage. The gravel is connected on the north genetically as well as geographically with moraines that cress the Cuyahoga below “the bend,” and lead southward across the present continental divide to the Tuscarawas Valley. The silt is apparently confined mainly to valleys and deeply filled lowland tracts, and was probably deposited in a glacial lake. On uplands and where the drift 26 MON XLI 402 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. is thin there is usually till, gravel, or sand resting directly upon the rock. A fuller discussion of the silts of northern Ohio is given m connection with descriptions of later moraines. About 1890 a deep well was made in the southern end of Copley Marsh, one-half mile west of New Portage, in which the drift was found to have a thickness of nearly 400 feet, and the rock floor an altitude about as low as the surface of Lake Erie. The boring is on a tributary of Tuscarawas River, and therefore south of the present continental divide. However, a broad lowland tract, deeply filled with drift, leads from it northward to the Cuyahoga Valley, indicating that this deep channel once had a northward discharge. Borings, though not numerous, are sufficient to mdicate that the rock floor of the Cuyahoga has been cut to a very low level, and the valley may have been an outlet for some of the northern Ohio drainage, as already discussed in Chapter III. In the Tuscarawas Valley at Clinton, near the inner margin of this morainic system, several flowing wells have been obtained from the drift. They are on low ground near the Ohio canal, and but a few feet above the level of the river. Their depth is 35 to 40 feet, and water rises about 5 feet above the level of the canal. They are mainly through blue silt, which is described by the well owners to be putty-like and free from grit. The water is obtained from an underlying gravel bed. There are several wells between Clinton and New Portage which penetrate a similar blue silt and obtain water from gravel beneath it, but the water does not overflow. On Charles Harmon’s land, in the Tuscarawas Valley near Mud Lake below Clinton, is a boring which struck rock at 80 feet, but this is a remarkably shallow depth to rock. At Canal Fulton, which is situated in the midst of the moraine, rock is exposed in the west bluff to a considerable height above the Tuscarawas River, but on the east side of the river wells 60 to 80 feet deep do not reach rock. In these wells a small amount of blue till is struck, but the material is mainly sand and gravel. Newberry has made the following statements concerning the drift in the Tuscarawas Valley below Canal Fulton:’ From Fulton to Millport and thence to Massillon many borings have been made, and in these where the course of the auger was not arrested by bowlders the drift 1 Geology of Ohio, Vol. ILI, pp. 152-153. MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 403 deposits have often been found to be more than 100 feet in thickness. For example, two wells were bored by Mr. E. Roberts northeast of Millport. In one the gravel was penetrated to a depth of 84 feet without reaching the rock; in the other, it was found to be 97 feet in thickness. On the farm of General Beatty two wells were sunk for water within 100 yards of each other. One reached rock at about 50 feet; the other, more westerly, is 100 feet deep, all drift. At the Charity School, as I heard from the Hon. A. C. Wales, a well was sunk to a depth of 90 feet through beds of sand and gravel without reaching rock. An interesting fact connected with this well is that near the bottom logs of coniferous wood, apparently cedar, were taken out. THE SHOULDER OF THE SCIOTO LOBE. On the uplands west from Canal Fulton, near Fox Lake, the drift has a known thickness of 80 feet at H. Meibert’s wells, and 60 to 80 feet in several wells at farmhouses 1 to 2 miles west of Fox Lake. Southward the uplands are more thinly coated, and many hills and ridges in the vicinity of Fairview, Dalton, West Lebanon, and Mount Eaton afford numerous outcrops of rock on their slopes and summits. The valleys are, however, filled deeply with drift and contain morainic features. In passing from these valleys eastward to the Tuscarawas Valley one finds considerable increase in the amount of drift on the uplands. At Beach City, near the outer border of the moraine, but within its limits, borings in Sugar Creek Valley strike rock at 90 to 110 feet, the drift being mainly assorted material. A boring at Nathan Rose’s farm, 14 miles southeast of Beach City, penetrated 88 feet of drift, a portion of which is cemented gravel, It is situated on the gravel plain which heads in the moraine at Beach City. In the vicinity of Wilmot several coal shafts have been sunk. Of these the drift in Putnam’s shaft is 43 feet, in Wyandot’s 71 feet, and in Hurrah’s 56 feet. The thickness of drift on the hills and ridges from Sugar Creek westward to Killbuck Creek probably averages less than 25 feet, but in the lowlands it is so thick that ordinary wells seldom reach its bottom. It was in one of these lowland tracts, in eastern Holmes County, that the skeleton of a megalonyx was discovered, described by Claypole.’ It was found in a marsh beneath a bed of peat 6 feet in thickness and on a bed of shell marl. Such marshes are not uncommon along this morainie belt, but are a less prominent feature than in the interlobate tract. 1 Am. Geologist, February, 1891. 404 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. In the comparatively low tracts that lead back into hilly districts along the glacial boundary in Holmes County the till is underlain by fine calcareous sand or silt of blue and yellow colors, like that in the Cuyahoga Valley near Akron. Wherever this silt was noted the drainage is northward from the unglaciated toward the glaciated tract. This situation makes it probable that the silt in question was deposited in small glacial foot lakes formed in advance of the ice sheet. These were subsequently invaded by the ice sheet, which filled the place the lakes had held and deposited till upon the silts. An excellent exposure showing several feet of silt may be seen on the Weinsburg and Berlin road, about a mile northeast of Berlin. On the elevation where Berlin stands there is scarcely any drift, but a mile east or west from this village on lower land it attains considerable thickness. John Miller, 1 mile west of Berlin, has a well 45 feet deep, and his neighbor, Chalmers Sharlock, one 40 feet deep which did not reach rock. These wells are within a mile north of the southern margin of the well-defined drift, if not of the glacial boundary. At Millersburg rock is struck in the vicinity of the court-house at about 75 feet, which gives the rock surface an altitude slightly below the bed of Killbuck Creek. Drift exposures of considerable extent occur in the north part of Millersburg, along the east side of the Cleveland, Akron and Columbus Railway. There is a small amount of ordinary pebbly till, but the great bulk of the drift is a poorly assorted gravelly sand with a slight clayey admixture. Where stratification is traceable the beds are horizontal, with considerable cross bedding, but arching or contorted beds were not observed. No records of wells of sufficient depth to show the thickness of the drift were obtained along Killbuck Valley, between Millersburg and Woos- ter. At Wooster the drift is thin on the slopes of the valleys, and a well in the village, two blocks south of the court-house, struck rock at 40 feet. The breadth of the valley bottom in the vicinity of Wooster is such, how- ever, that a channel of considerable size may be concealed in it. J.H.Todd, of Wooster, has furnished the writer with records obtained in the vicinity of that city, which in some cases extend to a depth of about 100 feet without reaching rock, while on neighboring hills the rock rises 200 feet above the well mouths. Between Killbuck Creek and Lake Fork the uplands carry compara- MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 405 tively thin deposits of drift, there being numerous outcrops of sandstone on the large ridges. The thickness probably averaged no more than 25 feet; but an abandoned valley connecting the streams along the line of the Pitts- burg, Fort Wayne and Chicago Railway is deeply filled with drift, wells having reached a depth of 185 feet without entering rock (Todd). Along Lake Fork the terraces fill the valleys in places to a height of fully 100 feet above the present stream, and it is not improbable that the drift extends considerably below the present stream bed. A gas-well boring at Loudonville with about 150 feet of drift, entered rock at an altitude fully 50 feet lower than that of the bed of the creek at its nearest approach to the village. The drift consists of gravel at surface, while sand constitutes the main part of the section. A boring for water at Peter Long’s, in Loudonville, penetrated 125 feet of drift without entering rock. In the vicinity of Perrysville the drift is heavy, but no records of deep wells were found to show its full depth. There are knolls 50 feet or more in height, and the crest of the moraine south of the village rises about 150 feet above the level of Black Fork. It is probable that the thickness is even greater than the height of the moraine above the creek. In a tribu- tary of Black Fork, 3 miles north of Perrysville, a well at Mr. George Hay’s penetrated 150 feet of drift without reaching rock, and George Maurer’s well, on the adjoining farm, strikes no rock, though 115 feet deep. Near the northern end of the reentrant portion of the moraine north of Mansfield, a well in Black Fork Valley, at David Forkler’s, penetrated 180 feet of drift without reaching rock. In the lowland tract in the north part of Mansfield a gas-well boring penetrated 250 feet of drift, strikiug rock at an altitude about 900 feet above tide. The waterworks plant in this lowland has several wells 100 to 140 feet in depth, some of which reach rock. In the business portion of Mansfield, on the slope north of the public square, there are outcrops of rock at an altitude of about 1,200 feet. Many of che ridges and hills in the vicinity of Mansfield have but a small amount of drift, though all seem to have been glaciated. THE EASTERN LIMB OF THE MAIN LOBE. At Lexington, in the valley of Clear Fork, near the outer border of the moraine, wells 100 feet deep do not reach the bottom of the drift, but on the bordering uplands the general thickness is only 30 or 40 feet. The highland tract in southern Richland County was crossed by the writer 406 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. along the line leading direct from Mansfield to Fredericktown, and a coating of drift 10 to 20 feet thick was found to be quite generally prevalent. On a prominent point about 3 miles north of Bellville, and perhaps 1,450 feet above tide, a well at Mr. Shickler’s reached rock at 18 feet, and on points about the same altitude, south of Bellville, wells penetrate several feet of drift. One-half mile north of Palmyra, on comparatively low ground, a well at C. Snyder's, 67 feet deep, penetrated considerable till and entered gravel near the bottom South from Palmyra the drift is much thicker than it is to the north. Passing west to the less elevated country the thickness of the drift increases, and where morainic features set in near Darlington it is generally 50 to 60 feet, or even more, in depth. G. McFerrins’s well, near Darlington, has a depth of 61 feet without reaching rock. It penetrates much till. In Fredericktown rock is exposed along the east side of Owl Creek, and the creek here crosses a rocky point which extends westward slightly beyond the railroad track, making a rock cut necessary south of the station. Mr. Cummings’s well in the village, at a level about 60 feet above the station, struck no rock at a depth of 80 feet; but just east of this well, on. equally elevated ground, overlooking Owl Creek, Wesley Whitford has a well which struck rock at 25 or 30 feet. The wells in Fredericktown usually obtain water at about 40 feet from beds of gravel between till sheets. For several miles west of Fredericktown the preglacial ridges and valleys are quite effectually concealed by heavy deposits of drift, but from Fredericktown eastward the drift sheet is thin, its general thickness being not over 25 feet. It maintains a nearly continuous sheet up to the very border of the neck of apparently driftless land, that has already been described as leading from Independence eastward to Mohican Creek. In the village of Jelloway, which is near the south border of this neck, flowing wells have been obtained from the drift at a depth of about 40 feet; and at Mr. Richert’s, 2 miles west of Jelloway, a flowing well 50 feet deep was obtained without reaching rock, while a well on higher ground at his residence struck rock at 50 feet. These wells are practically at the border of the nearly driftless neck, there being scarely any drift on the uplands north of Mr. Richert’s or at Jelloway. They are, however, in valleys, and show a larger amount of drift than the uplands adjacent to them. The drift penetrated in these flowing wells is said to be a pebbly blue clay. ‘ a a MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 407 East of Danville, at the point where Wright located the glacial boundary, the Cleveland, Akron and Columbus Railway cuts through morainic accumulations to a depth of 36 feet without reaching rock. In Danville a well is reported by Wright, on the authority of A. J. Workman, to have penetrated 136 feet of drift, ‘passing through yellow clay, blue clay, gravel, quicksand, and cemented gravel, and still not reaching rock.” Another well in Danville, 65 feet deep and through similar material, was reported. On the uplands between this outer member of the morainic system and Mount Vernon there is but little drift compared with the amount in the main moraine west of Mount Vernon. In the valley of Owl Creek, near Gambier, the following section of the bluff of the stream is reported by Read:! Section of Owl Creck Bluff, near Gambier, Ohio. Feet. 1. Yellow clay, with drift bowlders and pebbles and many flat fragments of local rock.:---..------ 8 2. Blue bowlder clay, unstratified, with rounded granitic bowlders, gravel, and angular fragments . Oia OcalMnO CSP eerste e/a S aan toed Soe asain teens sc cess ciu tk osc Ge cioeat eae ay ae ees se eres 20 Sam Samim abe cn DLUCKC aiveeie sees Seer eivtira ean ye Seg ae ete te as cokcy ea erate eee ee 3 AE e CATSEVStRAUIMCCNOTAVC Lan anaes a erect ie eee eee sale Senter Se. See SEL ee ee ee etre eee 4 Org COALSCrStraUieGIsAn Cemmass= Jest ae eee hed oo aoe siciics eel ce ee clonic Ss See SEC eR ee eee 2 Gaenvelil oval amin ate day chav ee eat ey yacale se sete ys oe I a setae a) a ah ec Sh ee a ve Sa 2 (emluicplanaimatedyc lagers eters eter coe Sonia ci eee coe cet ieiere le Dia ave See ee Bee ele eel aae ee 2 Sea Unstratinedgbowldenclayea ase tases se Sas ke Rk ee se So AS te ee Petee Se Sane yee ees ae ee 4 OMS tLapinedssamceam ci oravelerso mts orcs seals ah = sehr ayer epee (cha) ares epee ey are eae) Seer red Sea 8 In an exposure on Grannys Creek, a few miles northeast of Mount Vernon, a section of bowlder clay fully 60 feet in height is extensively exposed. In this section the surface oxidation extends only 8 to 10 feet, the clay below being blue. At Mount Vernon a large mAb of borings have been made in the valley of Owl Creek for the purpose of obtaining flowing wells. At the time of the writer’s visit to the city, in June, 1890, fully 100 successful flows had been obtained. The depth of the wells ranges froni 63 to 97 feet. Isaac Lafever, of Chicago Junction, Ohio, who made many of these wells, states that they penetrate about 45 feet of loose gravel and sand, at which depth a blue clay is struck which extends to the water vein. No statistics were obtained as to the rate of flow or to the height to which the water will rise above the surface. The flow is strong from a height of 2 or 3 feet 1 Geology of Ohio, Vol. III, 1878, p. 332. 408 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. above the surface. Mount Vernon derives its water supply almost entirely from these flowing wells. Several attempts to obtain natural gas have been made in and about Mount Vernon, and the borings show much variation in the thickness of the drift. The writer is indebted to A. D. Bunn, of Mount Vernon, for statistics concerning the drift penetrated. A boring at the waterworks, on ground about the same altitude as the Baltimore and Ohio station (991 feet), struck rock at 224 feet. The drift is mainly sand and gravel. This well is known as the Power-house well. About 2,000 feet south-southwest of the power- house well, and at about the same level, 234 feet of drift was penetrated. In the northern part of the city, on ground perhaps 1V0 feet higher than the station, a well, known as the Banning well, penetrated 90 feet of drift, mainly sand and gravel. A boring at the railway crossing in the west part of Mount Vernon penetrated only 90 feet of drift. About a mile east-northeast from the railway station, in a tributary of Owl Creek, where the altitude is about the same as at the station, only 8 feet of drift was penetrated. Two and one-half miles northeast of the central part of Mount Vernon a well called the Simpkins well penetrated 90 feet of drift. Its mouth has an altitude about 100 feet above the station. A well made many years ago at the court- house is reported by William McClelland, of Mount Vernon, to have obtained water in gravel at a depth of 75 feet, after penetrating much blue clay. At Bangs station, 4 miles west of Mount Vernon, several flowing wells have been obtained on ground having about the same elevation as the station, 1,102 feet. Their depth is 40 to 45 feet, and when first struck water would rise 20 to 22 feet above the surface. A well at Samuel Finnerty’s, on somewhat higher ground, has a depth of 74 feet. In all these wells there is till above the water vein. The source of the water supply is probably from adjacent upland tracts, whose altitude is 150 feet or more above the wells. On the elevated tract along the inner member of the morainic system in western Knox County the drift is so thick that rock is rarely struck in wells, and scarcely an outcrop of rock occurs in ravines. The appearance of the surface supports the conclusion that the hills and ridges have a drift mantle 100 feet or more in thickness, while buried valleys have 400 feet or more. W. G. Tight reports that a well at Homer, in northeastern Licking County, passed through 400 feet of drift. J. M. McFarland’s well, on an elevated tract at Appleton, has a depth of 167 feet and does not strike ——E—E———— MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 409 rock. The drift is gray clay with thin beds of sand. W.H. Wood's well, near Locke, has a depth of 123 feet without reaching rock. This well is in a slightly depressed portion of the uplands, and was made for the purpose of obtaining a flow. Eleven water-bearing beds were passed through, but water does not overflow from any of these beds. It stands, however, within 11 feet of the surface. An ocher-like bed was struck at the depth of 105 feet, whose material was so fine that it would not completely settle in water in forty-eight hours. At Hartford wells are only 20 to 40 feet deep, there being at these depths an abundant water supply from sand beneath beds of till. In Utica, in the valley of Licking River, a well at Levi Knowlton’s penetrated 58 feet of drift, mainly till, without reaching rock. Two miles north of Utica, at R. S Tullos’s, a flowing well on comparatively low ground terminates in drift at 85 feet. The drift is mainly till) On the uplands east of Utica wells in the morainic area penetrate 25 to 40 feet or more of drift. At Newark several borings for natural gas have been made, in some of which a large amount of drift was penetrated, in one instance 235 feet, in another 189 feet, and in another 147 feet. They are all in the Licking Valley, at about the same altitude as the Baltimore and Ohio station (819 feet). The drift is principally sand, but some clay appears in the surface portions. In the northern part of the city, wells penetrate from 3 to 6 feet of hard clay before entering the gravel. Exposures of till are numerous in the south bluff of Licking River, in the eastern part of the city, up to a height of about 60 feet above the stream. Bordering Newark on the northeast, as above noted, is a lowland tract, standing about 100 feet above the Licking River, which has considerable till in it. There is also sand, suitable for molders’ use, and gravel, the latter being sometimes disposed in arched and distorted beds. West from Newark, on the main moraine, the drift has a thickness of 50 to 75 feet or more on the uplands and is probably much thicker in the principal valleys. J.C. Wilcox’s well, at his residence near Kirkersville, on a very prominent part of the uplands, is 70 feet deep and does not strike rock. Near Etna several wells have a depth of 50 feet without reaching rock, and a boring made some years ago about a mile east of the village was thought to have gone to a depth of 183 feet without reaching rock, the information being given from memory. 410 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. At William Watson’s, on the south border of the Licking reservoir, a gas-well boring penetrated 150 feet of drift. It is on ground perhaps 100 feet above the level of the reservoir. Rock is exposed on Mr. Watson’s farm at levels still higher than the well mouth. A series of gas wells on Little Walnut Creek show a large amount of drift along its valley from near the source of the stream to Can: Winchester, near which it enters the Scioto Valley. The writer’s note» were obtained from the well drillers or officers of the gas companies soon after the borings were made, and therefore represent quite accurately the thickness of drift. The structure of the drift was not so weil observed, but a few apparently accurate records will be presented. A well at the border of the canal, between Baltimore and Basil, whose mouth is about 850 feet above tide, has 302 feet of drift. Its drift section, as given by the driller, J. H. Taylor, of Louisville, Ohio, is as follows: Section of drift beds in a gas boring near Basil, Ohio. Reet. Lee Conmmonmiclany (Mtr) tse eet Seles Pi one Scale ed Biel SE Sem yore eae yas ne eee ee earn 8 ONE COANSE’OTAV EM pee mie EN oe rear ete SO aie hoe esr Ni Sa Rey eevee ce 12 See oF © XG LA CRSA Cl satay ae eres ors Spe SPE ws te Tata t5)= oye) ale Case Ve Be oe eer re ea eT ae ee 110 LO CTE NYS an see eee ep eee ie ea ee a ee er Aare en ANA SOAs ae AS AAS ow A qos 40 SOO SHnIGI S22 aaa S Re RNG ato =e aaa ees eel ee ee Mea SE mae Mee se Wn Sue eB ul Lot 128 67 Bluerclayvextendingitospereaiontt,! 522s 5s 2 oe cee ee ee eee eee Eee eee eee 4 MotalKeMiitee sess es cee os Siti se cisiek eee Se 3 Pete Se Se Se ee ETE ee ree ee ie ea 802 Gas well No 1, at Hadley Junction, is reported by the driller, Frank Hugaboom, of Pleasantville, Ohio, to have penetrated 335 feet of drift. The altitude of the well mouth is 883 feet above tide, making the rock floor only 548 feet. The same driller reports that a well just east of the village, on ground about 900 feet above tide, penetrated 148 feet, and another near by only 45 feet of drift, while on much higher ground a mile or so east of Hadley rock is struck at about 30 feet. Hadley Junction is therefore near the east border of the valley. The deep valley extends south a couple of miles from Hadley before swmging westward. Wells near its southern border are reported by Mr. Hugaboom to have the following amounts of drift: The Lamb well, 1 mile west of Pleasantville, 225 feet; Levi Hite’s well, 14 miles west of Pleasantville, 326 feet; a well near Mr. Hite’s (owner's name not learned), 360 feet; the Watson well, near Hite’s, 225 feet. In all the wells reported by Mr. Hugaboom the main part of the till is within 50 MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 411 feet of the surface. Below this depth the drift is principally sand. At Carroll a gas boring was reported by a citizen to have passed through 264 feet of drift. The altitude of the well mouth is 835 feet, making the rock surface 561 feet above tide. The upper 15 feet is till, the remainder mainly quicksand, though some gravel occurs. In a boring at Canal Winchester, reported by the treasurer of the natural gas company, 216 feet of drift was penetrated. The altitude of the well mouth is 769 feet, making the rock floor 553 feet. The greater part of the drift is quicksand. This well boring is one-half mile north of Little Walnut Creek. Along the creek near Canal Winchester there are outcreps of shale, and 2 miles south of it, at Lithopolis, rock rises to an altitude 200 feet or more above the level of the mouth of the gas well, or nearly 1,000 feet above tide as indicated by the East Columbus topographic sheet. At Lancaster several gas wells show a large amount of drift. The following notes were obtained from Mr. Slocum, a citizen of Lancaster, who kept careful records of the wells. he altitude of the majority of the well mouths does not differ greatly from that of the railway station, 841 feet. Well No. 1, at the north side of the canal and west side of Maple street, altitude about 825 feet, penetrated 131 feet of drift, entirely sand and gravel; a log was struck at 26 to 27 feet. Well No. 2, just east of the canal reservoir and about 50 feet above it (870 feet above tide), penetrated 60 feet of drift. Wells Nos. 3, 4, and 5 start on the sandstone which is at the surface in the east part of the city. Well No. 6, on the Fair ground, penetrated 180 feet of drift; a log was struck at about 100 feet; altitude of well mouth about 850 feet. Well No. 7, at Forest Rose cemetery, pene- trated but little drift. Well No. 8, in northwest part of the city, passed through 180 feet of drift; altitude of well mouth about 840 feet. Well No, 9, near center of city, south of King street, has 180 feet of drift; altitude about 8!0 feet. Well No. 10, east of center of city and north of Main street, has about 180 feet of drift; altitude about 840 feet. There are several others not made by the city, each of which has 130 feet or more of drift. As above noted (p. 269), there is in Lancaster a drift ridge, upon which the court-house stands, containing much cemented gravel which has the appearance ot having suffered considerable erosion and leaching prior to 412 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the Wisconsin stage of glaciation. In the deeper part of the valley, also, the drift is probably of pre-Wisconsin age. Wright reports a well on a range of hills north of Clear Fork, at an altitude about 350 feet above the Hocking Valley, to have penetrated 40 feet of till, and another 20 feet. West of this range of hills, at Amanda, a gas-well boring at the flour mill near the station passed through 60 feet of drift, mainly till The altitude here is but 100 feet above the Hocking Valley at Lancaster (933 feet above tide). In portions of the village rock is struck at 10 feet or less. West from Amanda, on the divide, at an alti- tude 150 feet above the station, the drift is shown by wells to be in places 60 feet thick. Mr. Stout has a well 62 feet deep, mainly till, that does not reach rock. There are outcrops, however, between Stout’s well and Amanda, where the rock surface has an altitude but 25 feet lower than that of the well mouth at his residence. A well at John Crumley’s, 3 miles west of Lancaster, on comparatively low ground near Hunters Run, penetrated 78 feet of sand and gravel and did not reach rock. At D. Crumley’s, on the Circleville and Laneaster pike, about 3 miles west of Lancaster, a well has 39 feet of drift, the upper 18 feet being yellow till, the remainder sand. Near Crumley’s bold ledges of sandstone rise to a height of 125 feet above the well mouth, on whose surface there is scarcely any drift. A similar isolated sandstone ledge in Lancaster, called Mount Pleasant, carries scarcely any drift, aside from bowlders. On the uplands south of Circleville, near Thatcher, the drift is very thin compared with its thickness east and northeast of Circleville, the difference being due mainly to the absence of the inner or main member of the morainic system on the uplands southeast of the city and its presence on those east and northeast. In the Scioto Valley at Circleville two gas-well borings passed through a large amount of drift, one in the west part of the city having penetrated 140 feet, and one on slightly higher ground, in the eastern part of the city, 187 feet. The rock floor is 520 and 540 feet above tide in the two borings, the lower altitude bemg at the east well. In the west boring the drift is mainly gravel, but in the east boring there was a thin bed of gravel at the surface, apparently belonging to the outwash from the moraine, below which there was a heavy bed of blue till. MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 413 In a sewer excavation on Pickaway street, between Franklin and Mound streets, the following section was obtained: Section in a sewer ditch in Circleville, Ohio. Feet il, Clayy ainel Gayeyy erenell Or Ceylkel oon COMO ooo sos sen c osc rese sac: cooeSsseonenacecedseseeee 24-3 2. Grayel, horizontally bedded, containing many cobblestones, but in places composed only of fine SANG ac oan ecaneS eae aaa ED GH see Se OEE SEP E MTP ess ate maar ROMER Batre es aa 4-6 3. Yellow till, with streaks of blue till, the whole being calcareous from the very top, showing either that leaching had not occurred before the deposition of gravel, or that the caleareous ClEMEnUR WAS MES LOE dhaw ae Aap ne Sales Sia Sone atte Sees cee Say retane Cee a ee 5-6 In the till there are many small pockets of fine gravel. Theyare elon- gated horizontally, though they do not lie perfectly horizontal, their inclina- tion being in some cases as great as 25°. The pebbles in the till and also in the overlying gravel are mainly limestone. The gravel deposits capping the till are probably of the same age as the morainic hills east and north of the city, while the till may be slightly older. Its caleareousness at surface indicates either that no great amount of leaching had taken place before the gravel was deposited on it, or that, leaching having occurred, calcareous material was restored to it from the overlying calcareous gravels, or possibly the glacial stream that deposited the gravel. In a gravel pit m a morainic knoll one-half mile north of Circleville, some pebbles were collected and classified with the following results. The size determined upon included only pebbles an inch or less in diameter: Pebbles in a gravel pit new Circleville, Ohio. ILTTNVESOMO nd S66 6G Sea SSIS RECS SES een ae IEE Bn aa en ene emcee Va ee LR Ce ed 126 DIIGO Sad Soe Sdbeod bases cee Se nee Ee Res ne Seu et eee Sree Sern Sete Reape ee ee esa ta 6 QUETIY o devcossubdé docs obbesa585s Sopeeb a Bes Meee Cees eae Ee Hee ES Hee ee aes Ce ReeREE Wa ena ae ee 1 (Che ntigeeeen eats eran ea eres i= one Seis eee ee ele Reise ees eR SSS oe eee ee Ee ee eee 5 (GHD oc ode 2=semoocbecoouce sso coedogoc a sous oouscESsbasbosungessssesaesscoRsocdsecancsce 4 Cina Anelacem WANES. .o onneolsacsssasaeesecd some ao osor ese Sena oa cssdocoesassaooesonteatcuce 4 Ro tall are sew ene ecm see tiset eerie Cee beh abeeie tes ee Shs Ae ee ee wee auc eee 146 The pebbles are nearly all rounded and show no strie. Many nodules of clay, ironstone, and fragments of shale several inches in diameter occur in the pit. They are probably of Devonian age. There are cobblestones and bowlderets of limestone up to a foot in diameter. The stratification is nearly horizontal, but is subject to occasional abrupt departures from the horizontal. In a morainie tract west of Kingston a sharp ridge with north-south 414 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. trend is opened by a road crossing it, which gives an excellent section 20 feet deep at the crest of the ridge. In the lower 10 or 12 feet there is a gravel of medium coarseness interbedded with fine gravel. All of the beds arch with the surface of the ridge. Above these beds, occupying the summit and western slope of the ridge, are beds of coarser gravel which dip with the slope of the ridge westward at an angle of about 30°. The lower layers extend slightly beyond the summit of the ridge and rest upon the truncated ends of beds of fine gravel that dip eastward. Near the base of the west side of the ridge the gravel beds change somewhat abruptly to till. No records of deep borings were obtained along the Scioto Valley below Circleville. A deep gas-well boring in Chillicothe begins in rock, being at the base of a rock ledge. The drift is said to be about 100 feet thick in a gas boring near the bend of the Scioto at Richmonddale, a few miles southeast of Chillicothe, but the exact amount was not ascertained, nor ‘was the altitude of the well mouth. The Scioto Valley has probably been filled with drift to a depth of 100 to 2U0 feet along much of the course - between Columbus and the glacial boundary. THE WESTERN LIMB OF THE MAIN LOBE. On the comparatively low upland west of the Scioto, at Anderson, a well at Mr. Langdon’s penetrated 60 feet of drift. At Mr. Steel’s, near Anderson station, in North Paint Valley, wells 32 feet deep obtain water in gravel. On the elevated upland east of Lattas a well at Mr. McConnell’s is reported by Wright to have “passed through 12 feet of yellow clay and 5 feet of gravel. About 13 feet from the top a, piece of wood 3 to 4 feet long. and 3 inches through was found in clay. From this pomt the eye surveys a vast extent of till in the valley of North Fork of Paint, which is about 400 feet lower.” At several houses near McConnell’s, wells are reported to have penetrated 25 feet or more of yellow and blue till before reaching rock. In the valley of North Paint Creek, near Austin, there is a till exposure fully 50 feet high, yellow for a few feet at top, the remainder of blue color. This valley has but little gravel above Frankfort, but -below that village it carries a comparatively level gravel plain. About midway between Lattas and Greenfield are several wells along the Greenfield and Chillicothe pike which show considerable drift. At MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 415 W. E. Parrott’s 60 feet and at William Stinson’s 44 feet were penetrated without reaching rock, and other wells show 30 feet or more. Near Spout Spring station, midway between Greenfield and Bain- bridge, there are exposures of horizontally bedded, well assorted drift, 100 feet or more in thickness, some of the alternating beds being of fine sand and others of coarse cobble. Large masses of cemented gravel and cobble occur at different horizons from the base to within 30 feet of the top. The pebbles are composed largely of the local shales, but limestone and sand- stone pebbles and Canadian crystallines are not rare. The elevated hills in that vicinity are very thinly coated with drift, but along Paint and Buck- skin creeks it is in many places 100 to 150 feet thick, fillme up the valleys and resting on the slopes. At Greenfield drift exposures in the west bluff of Paint Creek show 50 feet of till, but a short distance west, on higher ground, rock is near the surface. In the several members of the morainic system, from Ross and High- land counties northward to the combined moraine in Clark County, the general thickness of the drift falls between 50 and 100 feet, there being, as a rule, 20 to 30 feet more of drift in the morainic tracts than on the bordering plains. The following represent the more important well records collected: Josiah Hopkins’s well, in the fourth or inner member, a few miles east of Washington, passes through 70 feet of till and does not reach rock. At Washington the gas well penetrates 70 feet of drift, mainly till. B. F. Coffman’s well, in the south part of the village, penetrates 60 feet of till. At Milledgeville the flouring mill well, 70 feet in depth, does not reach rock. Wells in Jamestown enter rock at about 12 feet, but the moraine near Jamestown rises about 50 feet above the altitude of the village, and it is probable that the drift has a corresponding increase in thickness. At South Solon a well at Harrod’s drug store, 187 feet in depth, pene- trates 140 teet of drift, largely till. At A. Gorden’s, on the crest of a moraini¢c ridge one-fourth mile west, a well boring 165 feet in depth is thought to have terminated in drift. At Midway the town well has a depth of 514 feet through till, and a well at a blacksmith shop has a depth of 54 feet. Neither of them enter the rock 416 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. At South Charlestown a well at a saloon north of the Little Miami station does not reach rock at a depth of 75 feet. In London one gas-well boring penetrates 155 feet and another 200 feet of drift. In both wells the drift is mainly till. A flow of water comes from the rock at a depth of 250 feet. At the waterworks in London there is a strong vein of water in gravel below till at 60 feet and another at about 150 feet. Chamberlin some years ago called attention to hillocks of angular gravel and disturbed stratification between London and Midway, Ohio." Several other exposures in that vicinity exhibit the phases of gradation from till into gravel, and the angularity of pebbles in the gravel to which Cham- berlin called attention, but no other instances of disturbed stratification were observed. From the frequent occurrence of gravel pits it is inferred that nearly all the knolls in the vicinity of London and Midway may contain gravel in their deeper portions, even where the surface is till. Less diffi- culty is experienced here in obtaining gravel for road ballast than in some of the later moraines of the Scioto lobe. In the morainic system under discussion gravel knolls are sufficiently abundant throughout its entire length to furnish gravel at convenient points for all the pikes. Two borings for oil near Vienna Cross Roads penetrate 265 and 245 feet of drift, mainly till. One is located 1§ miles east and the other a half mile south of the village, each at an altitude 1,200 feet or more above tide. At Mechanicsburg a gas boring near the station penetrated 130 feet of drift, and one at Major Baker’s, on an elevated drift ridge, penetrated 230 feet, the rock surface being at about the same altitude in both wells, 925 feet, more or less, above tide. In Baker’s well the upper 100 feet is a clay with comparatively few pebbles; the remainder is a very pebbly clay with but little sand or gravel interbedded with it. Several wells have been obtained at about 120 feet in the vicinity of this village, in gravel below till. At Catawba village Eli West has a well 215 feet in depth which did not strike rock. The upper 125 feet was mainly through soft blue till. Beneath this is a harder and more sandy till, which is probably Illimoian. The lower 25 or 30 feet is a soapy clay with few pebbles. At Fountain Park there are several flowing wells whose depth ranges 1 Am. Jour. Sci., May, 1884. MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 417 from 37 to 98 feet. Hach well has about 25 feet of till at the surface, beneath which is sand and gravel. The variations in the depth of the wells is due to the variations in the distance through the sand to a gravel bed coarse enough to be screened by the strainer placed at the bottom of the drive pipe. A gas-well boring at Fountain Park struck rock at 106 feet. At the railway station in Woodstock a flowing well obtains water from gravel below till at a depth of 50 feet. On the uplands south of Wood- stock and Fountain Park rock is struck in places at about 50 feet. At Cables and west from that village there is a lowland tract crossing the moraine, and near the water parting rock is exposed to a height of 5 or 10 feet above the level of the Columbus and Indianapolis Railway. Above the rock are heavy beds of gravel and cobble which are capped by till. The eastern slope of the morainic belt (both on upland and lowland) carries heavy deposits of till, but the western slope contains much more gravel than till, and the lowlands are underlain extensively by gravel, as indicated by the well sections. In northeastern Champaign and southeastern Logan counties there are numerous limestone quarries, the rock surface being higher here than it is farther south, and the drift correspondingly thinner. The drift has, how- ever, in many places a thickness of 50 to 75 feet or more. At Middleburg, near the inner (eastern) border of the morainic system, there are limestone quarries, but in portions of the village, at levels as low as the quarries, wells penetrate 60 to 90 feet of till before reaching rock. On “Bald Knob,” a large gravel hill near the outer border of this moraine, in southern Logan County, a well was sunk many years ago to a depth of 111 feet without obtainmg water. It was entirely through coarse gravel and cobble. On an elevated part of the moraine east of West Liberty, perhaps 200 feet above the station, a well on Jonathan Parker’s farm penetrated 194 feet of drift, striking shale at the bottom. A well immediately north of West Liberty, on the upland, penetrated about 170 feet of drift. The altitude is 90 to 100 feet above the railway station, or about 1,200 feet above tide. As noted previously, a gas boring in West Liberty penetrated 216 feet of drift. At Zanesfield a boring for gas is thought by citizens to have passed through 125 feet of drift, but no reliable record could be found. North of oT MON XLI 418 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Zanesfield, near the head of Rush Creek and Mad River (which have a common source in a swampy valley), is a well made by the Buckeye Port- land Cement Company, which, as noted on page 366, penetrated 245 feet of drift. The altitude of the well mouth is 1,261 feet above tide. On either side of this valley, in hills that stand 200 to 275 feet above the well, the rock surface is higher than the well mouth, being in places about 1,400 feet above tide. The well was at the border of a marshy lake (now dry) whose length was about 4 miles and breadth three-fourths of a mile. The cement manufactured by this company is obtained from marl beds im this marsh. The cement company made a boring for water three-fourths of a mile north of the gas boring and found no gravel until a depth of 100 feet had been reached, thus showing that the beds beneath the marsh have not a uniform structure. On elevated ground near the crest of the moraine east of Zanesfield Joseph Outland has two wells which do not reach rock at depths of 50 and 55 feet, water being obtained in gravel below till. A well at Aaron Taylor's, at the head of Mormon Bottom, on low ground but in line with the crest of the moraine, is 58 feet deep and does not strike rock. From Taylor’s farm water flows eastward through Mill Creek to the Scioto and westward to Mad River. The farm is located at the head of Mormon Bottom, a gravel plain leading west to Mad River. One-half mile west from Taylor’s, at Nelson Ream’s, near the south bluff of Mormon Bottom, rock is struck at 35 feet, and there is a rock quarry only 100 yards south of the well. The deep part of the valley probably lies to the north of Ream’s well. Immediately east from the head of Mormon Bottom, on the iner (eastern) border of the moraine, is the village of East Liberty, which has considerable local notoriety on account of its flowing wells. There are perhaps 100 of them whose depth ranges from 20 to 65 feet. ‘The water is obtained from beds of gravel in the drift. The source of supply is appar- ently in the higher land immediately to the west, a rapid decrease in head being exhibited in passing toward the east. The water is strongly chalybeate and is in good repute for its medicinal value. — Flowing wells are obtained at many points along the eastern border of the moraine for several miles north from Kast Liberty, near the head- waters of the several tributaries of Mill Creek. Some of them are but 15 MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 419 or 20 feet deep. The wells penetrate till until they reach the water-bearing gravel, The variability in depth at East Liberty is due mainly to varia- tions in the altitude of the water-bearing gravel, but in part to the altitude of the well mouth. Outcrops of rock occur along the inner slope of the moraine west of these flowing wells, at altitudes 100 feet or more above them, and the drift is thin for the breadth of a mile or more between these outcrops and the morainic crest. Along the crest of the moraine the drift is so thick that ravines and ordinary wells, which sometimes have a depth of 40 feet, do not reach the rock, and the highest points probably have 100 feet or more of drift. Devonian shales occur to a limited extent beneath the elevated portions of the moraine, but do not seem to form a continuous belt. The supposed highest point in Ohio, as indicated above (p. 357), lies between this moraine and Bellefontaine at the Hogue Summit on a moraine of the Miami lobe, its altitude being given by F. C. Hill, of the Ohio survey, as 1,540 feet. A point on the moraine under discussion at New Jerusalem is, by aneroid, but 25 feet lower. This great height has been ascribed to the presence of Devonian shales, and Mr. Hill estimated their thickness to be 110 feet beneath the Hogue Summit and 136 feet beneath New Jerusalem. In this estimate due allowance does not seem to have been made for erosion and partial removal of the shale, for, as already noted, 350 feet of drift was penetrated near the Hogue Summit. The most elevated point at which the shale was noted is at New Jerusalem Falls, one-half mile southeast of the village of that name, where its surface is about 100 feet lower than at the New Jerusalem Summit, or 1,415 feet above tide. The shales here have an exposure 60 to 75 feet in height in the gorge below the falls The New Jerusalem Summit is a small drift knoll covering but an acre or two, its highest point being 20 feet or more above the bordering portions of the moraine — Its highest point stands about 25 feet higher than the well at Mr. Kastman’s, where 350 feet of drift occurs. Attention has already been called to the fact that, were the drift removed from Logan County, the altitude of its highest points would fall 100 feet or more below that of the highest pomts of the rock strata in southern Richland County, and that even with the imcrease in height pro- duced by the drift, it is questionable if Logan County contains the highest points in the State. 420 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. BOWLDERS. This morainic system does not have such long-continued distinct belts of bowlders as characterize the equivalent system of the Miami lobe, but it is nevertheless liberally strewn with them throughout the greater part of its course. The number on its surface is markedly greater in the till tracts than where gravel predominates, though not rare in the latter situation. Wright has mentioned some of the larger ones that have been discovered. One at Buck Ridge, west of Canton, measured 55 by 46 by 18 inches. Another, on the bluffs of Tuscarawas River, near Navarre, measured 7 by 5 feet and is 3 feet out of the ground. In section 14, Hardy Township, east of Millersburg, is a bowlder 7 by 5 feet, projecting 3 feet above the surface. Near Oak Grove Nursery, west of Millersburg, at an altitude 430 feet above Killbuck Creek, is a granite bowlder 104 by 64 feet, projecting 34 feet above the ground. In the valley of Baldwins Run, between Lancaster and Pleasantville, a granite bowlder, mentioned by Andrews, of the Ohio survey, as well as by Wright, measures 18 by 12 feet, 6 feet out of the ground. It is described as hornblendic in character. In section 14, Colerain Township, Ross County, near the residence of Isaac-De Long, Wright reports several bowlders 6 by 8 feet in diameter. At D. H. Pricer’s, on an elevated upland north of Bainbridge (altitude about 550 feet above Paint Creek Valley), a bowlder of hornblendic rock 5 by 3 by 2 feet is reported. Bowlders of the sizes mentioned by Wright are exceptional, the great majority being but 1 to 3 feet in diameter. They are mainly Archean rocks except at the border of the drift, where there are in many places masses of local rocks which have been transported short distances by the ice sheet and mingled with material derived from greater distances. Many such local bowlders occur along the border of the shoulder east of Mansfield. The largest ones of which measurements were taken are on Adam Berry’s and John Ferguson’s land, about 14 miles northwest of Newville. A reddish sandstone is represented by several bowlders 15 feet or more in greatest diameter, whose thickness is 5 or 6 feet. A white sandstone bowlder was found to measure 14 by 24 feet, and stands 3 feet out of ground; another is 18 feet square and has been quarried down nearly to the ground; another, near by, dips into the hillside at an angle of 45°. It was originally large, but has been reduced greatly by quarrying. There are certain bowlders found in this region which are of great MAIN MORAINIC SYSTEM OF THE SCIOTO LOBE. 421 importance because of their bearing on the question of changes of ice currents. Newberry reports ‘huge bowlders of Corniferous limestone” in Northampton Township, Summit County, which he thinks have been brought from the islands in Lake Erie.’ If so, the early ice movements across these islands must have been southeastward—a very different course from that of the later movements. Bowlders of the same class were reported to the writer from Talmadge Township (which is southeast of Northampton), but they were long ago burned for lime. The source of these bowlders should be more conclusively demonstrated before inferences are drawn as to changes of ice currents. It has been reported by Whittlesey that copper occurs in the drift as far east as Weymouth, Medina County, Ohio.’ Bowlders of red, jaspery conglomerate, thought to be from the Huronian rocks north of Georgian Bay, are not rare in the vicinity of Mansfield and northward from there to Norwalk and Brownhelm, and they are occasionally found still farther east, one being reported near Andover, Ohio. They are quite common in western Ohio, northern Kentucky, and Indiana, and a few have been found as far west as southeastern Iowa. Those near the eastern limit of their known distribution indicate a transportation in a direction slightly east of south, though their main distribution appears to have been west of south. Chamberlin and Salisbury have cited the following evidences of southward movement into Ohio from the Huron Basin: To the east of the Lake Michigan trough lay the capacious valley of Lake Huron, flanked by Georgian Bay. There is strong evidence that these valleys directed these glacial streams southward in the retiring stages of glaciation, at least, and presumably at all stages. This is shown both by striation and by transportation. Copper, presumed to come from the Lake Superior region, has been found in eastern Michigan and even in Ohio. In the remarkable bowlder belt of Logan, Champaign, Miami, Montgomery, and Preble counties, Ohio, and Wayne and Randolph counties, Ind., are numerous peculiar greenish quartzite bowlders not common to the general drift. Professor Irving has identified specimens of these as derivations from certain quartzites of the typical Huronian region north of Lake Huron, samples in his col- lection being indistinguishable from the erratics collected by one of us. While it is possible that both the native copper and these quartzites may have had an origin farther eastward, these instances, taken in connection with a wider class of evidence, ' Geology of Ohio, Vol. I, 1873, p. 206. * Smithsonian Contributions, 1866, On Fresh Water Glacial Drift, etc., p. 11. 422 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. leave little room for doubt that the basin of Lake Huron determined a southerly movement of the ice current, and thereby rendered collateral aid to the Michigan Basin in directing the broad stream east of the unglaciated island.* A movement to the east of south from the region north of Lake Huron is also shown by strize to have taken place at some time during the Glacial epoch, there being strize with southeastward bearing south of Georgian Bay and southeast of Lake Huron, while the majority of those north of Lake Huron bear southward. The evidence from strize, therefore, supports rather than antagonizes the evidence from bowlders that there were south- ward movements over western Ohio at some time during the Glacial epoch. The later movements, however, seem to have been southwestward through the Lake Erie Basin, and thence southward into central Ohio, with lateral movement toward the southeast on the eastern side of the Scioto lobe. STRIZ, In the following table are arranged all the published as well as the unpublished observations of striz pertaining to the Scioto lobe so far as known to the writer. The strize all appear on the map of the Scioto lobe (Pl. XIID), where their relations to moraines may be readily seen. Table of strive in the Scioto lobe. Location. Bearing. Observer. Hampden, Geauga County, 1 mile south of..-..-.- Ne COS v5 ee ate see eas Leverett. Hampden Township, Geauga County....-.--.-..-- Sb ILS? 18, wo) (Sy WO? Wie ssesaass Read. @hard oneness te eee oem eases ec cie tele ees SHH? hy as Sees eee es Read. Chardon, 2 miles southeast of-.-.---.-..--..----. N. to S. and S. 5° W.....---- Leverett. Chardon, 2 miles south of........--.-----.------- Bis? Wises case See ere Leverett. Chardon, 4 miles south of........--.------.------ Sy Oo MWies 2. eae Seco neers Leverett. Newberry Township, Geauga County..-.--..----- Si0028H 42.3455 .2 eee see Read. Chester Township, Geauga County ..-.--.-------- PS Wre TA Ok openly arenes ena elena Read. Russell Township, Geauga County..-----.-.-----. Si GP IB, oS, WO 18 oe ecctce Read. Russell Center, 1 mile southeast of-.-.----......-- Sb Ga)? 19, OS: HS Wooo coos sss Leverett. Bainbridge Township, Geauga County.--.-------- §.,49° Rte foster area eee Whittlesey. Mantua Township, Portage County....-.--.------ Sh BOP 13, 1® S, GOP Ws se ssccs Whittlesey. Solon Township, Cuyahoga County........------- S045 OMG woth ee ey Seen Whittlesey. Solon Center, 1 mile north of.......--...-..-..--- She-40)2n OpeSeSSSe nee SEA So Leverett. South Euclid, Cuyahoga County......-.---.------ B.402 Wiscctes eters Se aeee | Leverett. South Euclid, Cuyahoga County--..-.----.-------- Sp AN 18, ro Sh WO oso 55e5-55 Whittlesey. 1Sixth Annual Report U. 8. Geol. Survey, pp. 318-319. STRL# OF THE SCIOTO LOBE. 423 n Table of striw in the Seioto lobe—Continued. Location. Bearing. Observer. Newburg, Cuyahoga County.-.-...--.------------ NGOS oe oe sec ea aes eee Whittlesey. Renimsulay summit Countyas==—- 92422222 o 2224 — SS, NO? 1B, tors; A0P 13), 5. = oan Leverett. Tyansbures Sumani Coumibyesss--2--5 ssssess es see Sh, BOP IB. tS, HH 2k Leverett. Boston Ledges, Summit County ---..---..-.------ Wis tOMBn =) seis seeememee metre Read. Boston Ledges, Summit County -..-....---------- Si BOY 13, WO) L445? 1-5 -36s5ce Read. Hudson Township, Summit County -.....--.----- S$. 35° BE. to S.90° H.___- Read. Northampton Township, Summit County-.----.-- Sh HOP 13, to St GOP 1-52 s2cese Whittlesey. Stowe Township, Summit County ---.....---.---- Spied ier wate ouaaseonaaonas Leverett. Cuyahoga Falls, Summit County ..-.-...-.------- S. 30° E. to 8. 45° H...-_..._. Leverett. East Akron (Middlebury), Summit County ------- VV FGA OWNE faee ets eu ee ee mt Whittlesey. Talmadge ‘‘Coal Hill,’ Summit County.--..-.----- Sh GO? IB, tho) SS, ZO 1) |e Whittlesey. Independence, Cuyahoga County.-....-.-.-------- Sime deawesrescdeeacecube aS Whittlesey. Brighton, 13 miles south of ...-........---.------ N. to S. to S. 10° E- seeeieceee | Leverett. North Linndale, 2 miles southeast of---.-.-.----- Sb O> WiYo TOMS: MOP Viv oo oesee ee | Leverett. iRereay-2amilesteastiOl aeepesa =e smaeas ease seas Sb 22 VWs WO) Ish CO WW coceonse Leverett. County line north of Brunswick ....----..-------- INL tO S tO S, BOP TBs cccscossce Leverett. Portage, near Akron, Summit County -.....---.-- S, 10° 18, to SB Wi 3 Read. New Portage, Summit County, 2 miles north of...| S. 40° E..__..._......_..._-. Leverett. New Portage, 3 miles southeast of -..-.-....------ So SUN acon HeSseas eee eS Leverett. Akron, 2) miles\southwest of-.-----.-.-----.---=--- INe TOS, HOS, BO? Wooccosse-se Leverett. Copley, Summit County --.....-..-..-......----- SS SO SOB eas 5scless see se eeee Whittlesey. Sharon; Medina County, 1 mile southeast of ------ SVS OA e eae Renee ores tees Leverett. Sharon Township, Medina County -....-...--..-- Ss AO SNE) Pt eae ee eee Read. Sharon, 14 miles northeast of.--..-...:.----------- Sh Gil)” 19, 1K) Sh ei? 15. 525 s554- Leverett. Wadsworth, Summit County, 4 mile east of-.-.---- Sh AO 19), 10) Sk BLO 19. so ssacecs Leverett. Wadsworth, 1 mile north of---...-_..------.----- Sheba dd sea te ssseasnesadescesas Leverett. Doylestown, Wayne County -.........-.--.--.--- S40 SHie sti! eta os eh cree Leverett. Doylestown, 13 miles south of.-.......--..------- Sh GP 135 WO) SHOWS Ica cceceec | Leverett. Ee Doylestowneownshipesesseece === em eee Rae INSELOIS evs Ps eee neh eens ..-| Whittlesey. Mount Eaton, Wayne County --..-.-.------------ 8. 40° E. to 8. 45° E.._._.-_--| Wooster. NoxthtoteMasslllonkeeseeeeee ene sees ee ace ae Sh (63> JD, 110) IS OHIO 1B) = 5555 | Leverett. Holmesville, 3 miles west of ....--.-------.------ Sn 825Wis as schsse sess | Leverett. Newville mile morthioie 3225 ss 2s5 see senses” INSto See ae cat eee seeps Leverett. West bluff of Black Fork, 5 miles east of Mansfield | 8.45° H _.____.___.----..---- | Leverett. Hill north of Windsor station....-.--.----------- SHEY+2n Oar, Se emia Anat Se | Read. At schoolhouse, 3 miles northeast of Lexington....| S. 10° E. to 8.12° E __._-___.- Leverett. Midway between Mansfield and Lexington ------- Selo S0By esse hate wae see | Wooster. West Amherst, Lorain County .......------------ B30 CCE keel esentreeee | Leverett. Henrietta, Lorain County ..-......---.---------- S$. 20° W. to §. 35° W ......--- | Leverett. Birmingham, Erie County, 2 miles south of... -.--- sh IGS Wie Sh HO WY escececse| Leverett. Townsend Township, Huron County ...----.-----. S 40m Wieseses see sess sacs | Read. Sandusky aaseereeme ese ae cece ssecee cats asee SED ee WWRLONSs Silica Vienna seer Newberry. 424 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Table of strive in the Scioto lobe—Continued. Location. Bearing. Observer, Put-in-Bay Island, Lake Hrie .....-..-..--------- Solos Wienges rc0s Wireaeeeee Newberry. Kelleys Island, Lake Erie._........-------------- Si GO? WoO AO? WY 22222225 Newberry. Marblehead penimsula 2222-222 2222222522. 52- 22 SH Mee R ERA Ata SE AEN oc Wright. Bellevue thea ase Sate eiece ea tec wales cle Mees SV602 Wi ss Bes eee erties Newberry. Republic, 4 miles east of..........-..------------ SE20°W goceee it Soars eee Leverett. Cann, Quiawe, Comat, 55. oS eeasccsaannasoacecn|| ShOHM W/o oceecencessectasce Gilbert. West Sister Island, Lake Erie.....-..------------ S.80% We Ssee eee eee eee Gilbert. West Sister Island, Lake Hrie.._-.....--.-------- INEtO}SSeeee Shee ee eee Gilbert. IHU cll yee eee ote hse sh ees re Sa See send S°40° W. to S. 45° W 2222-22. Winchell. Seneca Township, Seneca County .....--.-------- 8.5° E. and §. 23° W _-...--.- Winchell. Crawford, Wyandot County -....-.-.-.---------- S202 W. see cae sere oaseee Winchell. Crane Township, Wyandot County -.------------- Shot Wieceecae eae goocee eee Winchell. Grand Prairie Township, Marion County --------- INto Sea a esses eee Winchell. Marseilles ...._-- SRC UR DE BEB A eS ce ae ame pen ae S. 10° EH. toS: 10° W --2--22--- Winchell. Richland, Logan County, 4 mile south of -.-.----- SPD aN ie Nea nes eae tase oe Leverett. Beller Centers ee avss eee ces eeewesse Sees ske SEO Wi 52 Asap ee ees as Leverett. Musselman’s quarry, near Big Springs ------------ B.10° Wis ss eee ose eee cee Leverett. (BION S PRN Os eeeee usar sani sas araae cose mem eetelS 8. (8° 0Wh. jesemest oe aeeeeeeane Leverett. Middleburg, Logan County ...-..-------.-------- 8. 40° W.to 8. 45° W ..._._--- Leverett. Welawarewengn satis asers neice we ctesoeeacce seen 8.82 AB). Eee a see ees Leverett. QuamnyseastiotiJenomes sess ses =e es eee Shoo Wo WOS TP 13) oe noe Leverett. Bers Os GwenAy, ulsehe deo = |e sean S.3° MH) Sosece eee aa ee ae Leverett. East bluff of Scioto, west of Powell......-...----- foi Moho Dee aes ork Leverett. East bluff of Scioto, 7 miles above Columbus. .----- PSHohs OP eee Genet Mea ee Leverett. Columibus; 2 miles west of .........-...--..-....- SN 20S Hi rele iss eee ees Leverett. Meinl, 2) imaulles OWN Oia. Soccnceesonssesataoascce 288 Fe ce ee aaa ae ee eee Leverett. Sunbury, Delaware County, 2 miles north of. _-..-- 8.402 Rh a bok See Wooster. Suni umyee terete eens smears sce hassel ae S458 B28. tyes Seen Wooster. Near Hopewell Church, 2miles south of Carroll, | 8. 15° W.....-......-.....--- Leverett. Fairfield County. Near Buckskin station, Ross County.-.-.------..- INGtOIS ee a See eee Leverett. Rock Mills, north of Greenfield -.---..-..---.-..- SAS0 2 Wiss xce.c oe Seer eee ae Leverett. South bluff of Lee Creek, near mouth........-___- B22: Wek tiem ee Leverett. Leesburg, 2 miles southeast of..........--------.- Si O8Wis Re Seen ee cee Leverett. Wueesbung; lmile\ west (of= 22222222222 25.2522----.- SiS 2 Wess aaa ee ee Leverett. Neanibees butayee en aioe tela seis seine eee fees SEO S Wi Sie Se ee Chamberlin. Near Reesville ..... ---------- Se Sores opt AS eee 8. 45° W.to §.56° W ___.____. Chamberlin. Conklin’s quarry, near New Jasper-------..------ NB SW acne tae a eee Leverett. Bickett’s quarry, near New Jasper -.------------- INS SO miWihe aoe e ee ee eee Leverett. Xenia, 4 miles from, on Cvesars Oreek ----.------- Sea0 2 Wiste se ae ee ee ee Leverett. NeariOgdenaseenoc-e ena: oneness Sdsehssce see 8.37?) Wises isaac eee eee as Leverett. Wilmington, in Lytles Creek Valley...........--- 5.3227) Witetines aes areas Leverett. STRLH OF THE SCIOTO LOBE. 425 The general absence of strize on the numerous outcrops of limestone in the highlands of Logan and Champaign counties has been a cause of sur- prise, for they abound on either side and north of these highlands at nearly every outcrop examined. An exceptionally careful search was made for them in the highlands, as it was deemed important to gather all possible evidence shedding light upon the direction of ice movement at the junction of the Miami and Scioto lobes. Their absence seems to indicate that the abrasion was less vigorous in the morainic area than it was a few miles back beneath the ice, though the amount of drift deposited there was not less, but mstead rather more, than in the region within the morainic system. South from Champaign County there is scarcely a rock outcrop along the moraine or the inner border plain for a distance of 40 miles or more, which accounts for the lack of observations of strize in that region. South- west from this moraine, where the drift is thinner, strize are found in nearly every exposure examined between it and the outer moraine, and in the dis- trict farther west covered by the Miami lobe. The ice movement appears, therefore, to have been vigorous in the terminal portions of the lobe. The small number of striz observed near the eastern border of the Scioto lobe and southern border of the shelf or shoulder is probably due in large part to the texture of the rock. he shales in the southeast part of the lobe could scarcely retain striz long after exposure, as they soon crumble and decay. The coarse sandstone farther north is often of a loose texture, so that striz could not be preserved. The outcrops of Waverly sandstone are not extensive in the region investigated, and only certain layers of the formation would retain striz after long exposure. The large number of striated exposures reported from the vicinity of the Cuyahoga River is due to their remarkably perfect preservation on the EKocarboniferous conglomerate, and that, too, in the most exposed situations, where there has been little or no drift covering the rock since the ice dis- appeared. The sandstones in that region, being a firm grit rock, are also more suitable for retaining striz than in the regions farther west and south, where they are soft. The causes for the variation in frequency of observa- tions of strize in different parts of the lobe embrace, therefore, differences (1) in abrading power of the ice sheet, (2) in concealment by drift, and (3) in the texture of the surface rocks. 426 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. INNER BORDER PHENOMENA. GENERAL FEATURES. The district here discussed as the inner border tract embraces the portion of the Scioto Basin lying between the inner member of the main morainic system and the Powell moraine, which crosses the basin a few miles north of Columbus. The main part lies south of a line passing east to west about 10 miles north of Columbus, though narrow projections toward the north occur near both the east and the west border of the Scioto Basin, as indicated on PI. XIII. This district has lower altitude than border districts. Its lowest part is along the Scioto River, there being a gradual rise from the river, both east and west, to the moraine just described. There is a southward descent along the sides of the Scioto Basin as well as along the stream. The altitude of the river bluff at the border of the Powell moraine north of Columbus is about 875 feet, at Columbus 800 feet, and at Circleville 720 feet. The east and west borders of the basin are about 300 feet higher than the axis followed by the river, and descend southward at about the same rate. WEAK MORAINES. The greater part of this district presents a very smooth surface, and portions of it west and southwest of Columbus are known as “‘the plains.” A few quite conspicuous knolls were formed, however, on the east side of the river, and may indicate the position of the ice margin at a stage of halting during the retreat. The position of the larger of these knolls and ridges is indicated on PI. XIII. A conspicuous group known as the Spangler Hills is found on the east side of the Scioto, about 8 miles south of Columbus. As indicated by the Kast Columbus topographic sheet, there are,two points that rise nearly 100 feet above the border plain. Small knolls appear near this prominent group in a belt about 2 miles long from north to south, and about a half mile in width. They are often sharp and conical, but associ- ated with them are ridges which are more or less winding. The sharpest knolls are gravelly, while those with the gentler slopes contain till. From the north end of this belt northward a mile or more there are low swells inclosing basins 8 or 10 feet in depth. In some cases the basins cover several acres. This gently undulating tract carries a slight coating of till, perhaps 10 feet in thickness, below which there is gravel. The next knoll INNER BORDER OF THE SCIOTO LOBE. 427 of importance toward the north is Baker Hill, on the Groveport pike, 3 miles southeast of Columbus. This rises abruptly about 50 feet above the bordering plain. Its highest point, as shown by the East Columbus topo- graphic sheet, is 819 feet Orton once mentioned to the writer that he had noted evidences of disturbed stratification in it, some of the beds being crumpled and contorted as if by a shove from the ice sheet. There are no knolls near this hill toward the north, but about 7 miles east of Columbus, in the east bluff of Walnut Creek, a chain of knolls and ridges sets in which is maintained with slight interruptions from there northward for 8 or 9 miles, and possibly may find a continuation in sharp knolls of the same type that lie along the west border of the main moraine from near Hartford northward several miles. The tract east. of Columbus includes a sharp knoll at the south, 40 feet or more in height, standing by itself, a short distance north of which a sharp ridge in form somewhat like an esker sets in, which is quite distinct for a mile or more. It is 10 to 20 feet high, and but a few rods wide. It contains much assorted material, but has a slight capping of till, and its surface is liberally strewn with bowlders, features which, taken in connection with its trend, indicate that it is a frontal ridge of morainic character rather than an esker. Between . this point. and New Albany, which is 8 miles north, a few sharp knolls 20 to 25 feet high, and many lower knolls occur, forming a nearly contin- uous belt. No knolls of this class were found on a line east from Sunbury to Hartford and northward from that line. Since the belt does not appear to have a northward continuation from New Albany distinct from the main moraine, there is a probability that it became blended with that moraine. As noted above, there are, from the latitude of Hartford northward for many miles along the west borders of the main moraine, sharp gravelly knolls and ridges, similar to those near Columbus, while the remainder of the moraine is nearly free from such knolls. Quite often some dependence may be placed upon structure in tracing moraines; thus one moraine may be characterized by numerous gravel knolls, while the one next to it in the series may be nearly free from them. While it may not be safe to conclude from this class of evidence that the gravelly knolls in the main moraine are contemporaneous with those in the inner border district and markedly later than the remainder of the moraine, such a tentative classification seems legitimate. 428 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. THE PICKERINGTON ESKER. Besides the knolls and weak moraines above mentioned, there are two well-defined esker ridges in this inner border district which help to give relief to the nearly monotonous plain. One of these is called the Picker- ington esker, the other the Circleville esker. The position and trend of each is indicated on Pl. XIII. ; The Pickerington esker derives its name from the village of Picker- ington, in northwestern Fairfield County, which is situated at its northwest end. The length of this ridge is about 5 miles, its southeastern terminus being in the moraine just west of Basil. It consists of a very small ridge, only 6 to 10 feet high and 4 to 8 rods wide, but it has scarcely a break in it and is a conspicuous feature for one so low. It winds considerably, but has a general west-northwest to east-southeast trend. It is utilized for a wagon road throughout nearly its entire length, and is as dry as a gravel pike. In places the bordering tracts are slightly lower than the adjacent plain and are somewhat boggy, but there is not a well-defined esker trough. In these boggy tracts there is an occasional low knoll of gravel. The southeastern end of the esker does not show a well-marked delta; but there seems to be an equivalent in a greater amount of sand in the moraine than north or south from the esker. The sandy portion of the moraine occupies 2 square miles or more, and seems attributable, in part at least, to the escape of water at the margin of the ice sheet at a time when a portion of the escaping water farther back beneath the ice produced the esker. At its northwestern end the esker is associated with several drift knolls or short ridges of considerable prominence. The largest one is.just east of Pickerington and stands 30 feet or more above the bordering plain. It is one-fourth mile or more in length and about one-eighth of a mile in width. Its trend, like that of the esker, is west-northwest to east-southeast. It is strewn with bowlders that are slightly embedded in a yellow clay that caps the knoll. , The nucleus of the knoll is probably sand or gravel. Over an area of perhaps a square mile north, west, and south of this knoll there are knolls 20 feet more or less in height, which give the tract a morainic aspect. The bordering country on all sides is a plain. It is probable that their origin is in some way connected with that of the esker. The esker itself is made up of gravel and sand of various degrees of INNER BORDER OF THE SCIOTO LOBE. 429 coarseness. On its surface are occasional bowlders, and in places some clay appears as a capping to the gravel and sand. The bordering plains are underlain by till. THE CIRCLEVILLE ESKER. The Circleville esker lies along the east side of the Scioto River above Circleville, in places forming its bluffs, while in other places it is a mile from the river. Its gener2: trend is about N. 25° W. to S. 25° E., but for a couple of miles south from South Bloomfield it is nearly north to south. Its length is about 9 miles, but it has several interruptions, as indicated below. At its northern end there is a group of knolls which apparently have some relation to it, but they are much inferior to the esker in size, thus differmg from the knolls at the corresponding end of the Pickerington esker, which exceed it in size. The northernmost ridge of this Circleville esker belt is in section 3, Harrison Township, Pickaway County. The ridge is about a mile long, 100 to 150 yards wide, and is 15 to 50 feet high. The northern third trends about northwest to southeast, but the remainder trends north- northwest to south-southeast, or even more nearly south. At the south end of this ridge and just north of South Bloomfield is a knoll about one- fourth mile long and half as wide, standing in its highest points 20 to 25 feet above the bordering plain. It trends north to south. Both east and west of this one are a few knolls 10 to 15 feet in height. There is then an interruption of the esker for a mile or more; but about a mile south of South Bloomfield a gravel ridge begins abruptly with a height of fully 40 feet, its north end having a slope of 35° to 40°. It is a continuous ridge for 14 miles, terminating near the mouth of Little Walnut Creek. Its general height is 30 to 40 feet. It consists in places of a central ridge with parallel flanking ridges, connected more or less closely at one or both ends with the main ridge, the width of the system, including flanking ridges, being one-eighth mile, more or less. South from Little Walnut Creek there is a gap of fully a mile, in which no esker ridge appears. Much of this interval is overflow land, and it is possible that the esker was once present, but has been washed away. South of this interval there is a sharp ridge about one-fourth mile long and 30 to 40 feet high in its highest parts. This is succeeded on the south by a gap of about one-half mile. The esker there sets in again and is well developed for fully 4 miles. It 430 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. consists of a main ridge that stands 20 to 40 feet above the plain on its eastern border, and 40 to 60 feet above the Scioto River, which flows along its west side. In several places ridges separate from the main ridge and return to it one-fourth mile or so south, making a nearly complete connection with it at each end. In some cases very sharp basins are inclosed between the main ridge and these side ridges. ‘Two were observed that are about 40 feet deep. One of these was dry, tle other contained a pond. The ridges on each side have sharp slopes of fully 30°. These slopes afford a means for calculating the amount of filling the basins may have received since the ice retreated. By continuing the slopes down- ward beneath the basins from opposite sides, they would meet at a point about 20 feet below the present surface, which represents the possible amount of filling. It could not well be greater and it may have been less, espe- cially if the basin originally was somewhat flat in the bottom; but, granting a fillmg of 20 feet, it follows that the amount is small for such steep slopes of loose material to have contributed, and it affords evidence in favor of the brevity of postglacial time. At its southern end the esker branches, like the mouths of a stream in a delta, and is lost in a marshy plain. Low ridges or knolls occur in this plain south of the terminus of the esker proper, and on the border of the plain, in the northern part of Circleville, there are gravel knolls which may bear some relation to the esker, though they are situated in the moraine. The termination of the esker proper is but a mile or so from the moraine. In all probability the esker was formed before the ice sheet had withdrawn frem the moraine. But few exposures occur to show the structure of the esker. A well at R. D. Harmon’s residence, on the crest of the esker, about 3 miles north of Circleville, penetrated 60 feet of sand and gravel and obtained water at about the level of the Scioto River. The water contains sulphur in such large amount that stock will not drink it. The sulphur is probably from sulphuret of iron contained in fragments of shale. Mr. Stevenson has a well near the base of the ridge, a short distance north of Harmon’s, which penetrated 6 or 8 feet of clay and then 30 feet of gravel before obtaining water, probably reaching the level of the Scioto. In places the ridge is capped by a few feet of clay, through which pebbles are scattered, but quite as often the gravel is at the surface. At a slight exposure near INNER BORDER OF THE SCIOTO LOBE. 431 the top of the esker, by the east end of the bridge, 3 miles above Circleville, there is at surface a clayey gravel with a depth of 2 to 5 feet, below which is a series of beds of fine gravel dipping sharply westward with the slope of the ridge. These terminate abruptly like a cross bedding in a layer of cobble, which dips slightly eastward. In an exposure south of South Bloomfield there are cobble beds dipping abruptly southward. This expo- sure gives only a partial view of the structure. So far as examined the pebbles are largely limestone, but fragments of black shale and granitic rocks are not rare. An interesting feature connected with this esker is its very slight elevation above the Scioto, its base being but 20 to 30 feet above the river bed. The river has, therefore, cut down but a few feet since the Glacial epoch, and that, too, notwithstanding the rapid fall. In the 40 miles (by direct line) from Columbus to Chillicothe the stream falls nearly 100 feet, or about 2 feet per mile if the main deflections of the stream be taken into account. This slight erosion, like that shown by the esker, appears to be strong evidence of the brevity of the postglacial time. The esker lies in the midst of a gravelly belt through which the Scioto River flows. The width of this belt is about 2 miles in northern Pickaway County, but below the mouth of Little Walnut Creek it expands to a breadth of not less than 4 miles, the expansion being mainly on the western side of the river. This gravelly tract is slightly lower than the bordering till plains and its border is very distinctly marked. With the exception of the esker it stands but 20 to 40 feet above the Scioto River. The esker is slightly higher than the till tracts adjacent to the gravelly belt. This gravelly belt was apparently formed while the ice sheet still covered the region, for the gravel in places carries a thin capping of till) The presence of an esker in its midst is also an evidence of subglacial deposition. STRUCTURE AND THICKNESS OF THE DRIFT. With the exception of the valleys of the principal streams and a few small areas on the uplands the surface portion of the drift in this inner border tract is ordinary till. The district may, therefore, be considered a great till plain. On portions of it there are thin deposits of silt or clay which are less pebbly at surface than at a depth of 4 or 5 feet. There does not seem to be a weathered zone or interval between the silty portions and the pebbly till below, but instead the evidence favors the idea that there is a transition upward from pebbly till to clay with but few pebbles. 432 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. In the upper 2 or 3 feet there are ordinarily not more than one-fourth as many pebbles as there are 5 or 6 feet below the surface. This is true in the immediate vicinity of the Scioto. At higher levels, near the border of the basin, pebbles are not so scarce. On the contrary, surface bowlders are numerous near the border, while in the central portion they seem to be covered, in places at least, by the clay just mentioned. Orton called the writer’s attention to several exposures in the city of Columbus where bowlders abound at a depth of 4 or 5 feet beneath the silty clay. This peculiar distribution of bowlders has not been observed outside the city of Columbus, either by Professor Orton or the writer, but may be widely developed in the silt-covered portion of the basin, no special search for the bowlders having been made. | The gravel belts along streams are most conspicuous on the Scioto and Olentangy rivers, Darby Creek, and the lower course of Big Walnut (from the latitude of Columbus southward). The gravel along the Scioto is in places capped by a few feet of till which seems to indicate that its deposi- tion occurred before the final retreat of the ice from this region and opposes the view that it was an outwash from the Powell moraine. The belt on the Scioto is narrow above Columbus, but is well defined all along the brow of the bluffs of the rock gorge extending back 100 to 200 yards on either side of the rock bluffs. Below Columbus the rock bluffs disappear and the gravel belt has a width of a mile or more. Its eastern border is followed nearly by the canal all the way from Columbus to Circleville. The west border lies back from the river at varying distances from a few yards up to nearly a mile and, in the vicinity of Circleville, is, as noted above, 2 or 3 miles from the river. On Olentangy River the gravelly belt is one-half mile or more in breadth. Possibly it marks the line of discharge for the main glacial stream leading down from the Powell moraine north of Columbus, though it seems quite as probable that its deposition preceded the formation of that moraine. On Darby Creek the gravel in the lower part is confined to the valley of the stream, but in the upper part above Plain City considerable gravel is found in the plains bordering the valley. This gravel is perhaps an out- wash from the Powell moraine, which lies north of that part of the creek. South from Plain City the bluffs wherever examined contain till. In the valley in Pickaway County, are terraces which may be of glacial age, INNER BORDER OF THE SCIOTO LOBE. 435 standing 20 or 30 feet above the stream, and occupying in places nearly the whole width of the valley. These terraces may perhaps have suffered . some reduction from their original level. If not they indicate that less excavation has taken place since they were formed than took place between the withdrawal of the ice from the border plain and the deposition of the gravel. On Big Walnut Creek till is present above the latitude of Columbus, but from that latitude southward there seems to be but little within a mile or more east from the creek, the drift being gravelly. For a few miles above the mouth of Black Lick, an eastern tributary, the interval between the two creeks, 1 to 2 miles in width, is occupied by a gravel plain which stands 20 to 30 feet above Big Walnut Creek. The belt is narrower below the mouth of Black Lick, but continues to the Scioto.. Bowlders were observed on the surface of the broad portion of this plain, about 2 miles above the mouth of Black Lick, which are either at the surface or embedded a foot or two in a brown clay that caps the gravel. This clay is seldom more than 3 or 4 feet thick, and usually but 12 to 18 inches. In Madison County there are belts of land slightly depressed below bordering till plains that are said to be underlain by gravel. They are known as ‘“‘glade,” and the timber on them differs from that on the border- ing till tracts, bemg nearly all white oak without underbrush, while the bordering tracts have a variety of timber and much underbrush. The gravel of these glades is probably of glacial age, but the mode of deposition and points of connection with the ice margin have not been worked out. The following represent the principal well sections obtained in which the drift has notable thickness. At Westerville the gas well passed through 94 feet of drift. The boring for gas at Plain City penetrated 119 feet of drift. This boring has about 10 feet of gravel and sand at surface, the remainder of the drift being mainly blue till. The well mouth stands 15 feet below the level of the railway station, or 919 feet above tide. At Columbus the statehouse well, sunk in 1857-1860, penetrates 123 feet of clay, sand, and gravel.’ The gas well made on the banks of the Olentangy River in 1886 penetrated 104 feet of drift.” The altitude of the well mouth is 737 feet above tide. At J. M. Linton’s, near the Scioto, 2 1 Geology of Ohio, Vol. I, 1873, p. 113. *Tbid., Vol. VI, 1888, pp. 281-282. MON XLI 28 434 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. miles south of the statehouse, an artesian well passed through 106 feet of drift, of which the upper 50 feet is gravel and the remainder sand. Water comes from below shale at a depth of 148 feet. The water rises 3 or 4 feet . above the level of the canal at Columbus. : At the starch factory in the south part of Columbus, near the canal and river, several flowing wells have been obtained from the drift at depths ranging from 40 to 90 feet. They are said to pass through “hardpan” just above the water vein. Whether this hardpan is till or cemented gravel was not learned. The main part of the drift penetrated was gravel. At the Lutheran College, in the east part of Columbus near Alum Creek, a well 110 feet deep did not reach hard rock, but may have entered shale. At the waterworks on Alum Creek several flowing wells were obtained at depths of 30 to 40 feet. They penetrated about 12 feet of gravel at the surface and were then in till to the water vein. This water is strongly chalybeate. The bluffs on Alum Creek on each side of the waterworks are composed of till; the gravel is therefore strictly a valley deposit. Orton has made the following statements concerning the erosion near Columbus: . The erosion has been especially extensive near the junction of the two rivers. For 3 miles at least above the mouth of the Olentangy the rocks between the rivers have been cut away to such a depth that no trace of them is now visible even in the deepest wells that are dug. The drift deposits that take their place do not rise to the same altitude that the surrounding uplands attain, and thus the whole of the country, from North Columbus westward to the Scioto, belongs in the category of lowlands. Immediately north of this lowland tract the altitude is not only greater, but the drift much thimner, so that the erosion was far greater than is indicated by variations in the level of the present surface. On the plain southwest from Columbus the drift is 10 to 50 feet or more in thickness. On Darby Creek there are occasional outcrops of rock in Franklin County as far south as Harrisonville, but from that village to its mouth no outcrops were observed, though the valley is in places 75 feet in depth. In the portion of Deer Creek immediately west from the lower portion of Darby Creek, rock outcrops are numerous. The heavy drift does not, therefore, extend much farther west than Darby Creek. It may occupy the entire interval between that creek and the Scioto in Pickaway County. 1Geology of Ohio, Vol. III, 1878, p. 599. INNER BORDER OF THE SCIOTO LOBE. 435 Near the southwestern border of this plain, in Madison County, the drift probably exceeds 100 feet in average depth. The borings for gas at London are the only ones reported that have reached rock. These, as pre- viously noted, have in one case 155 feet of drift, and in another 200 feet. East from the Scioto numerous exposures of rock occur along the main creeks, and some hills, near Lithopolis, rising much above the level of the plain, have rock at surface. This does not, however, prove the absence of valleys with heavy drift deposits; deed, such valleys probably traverse this district. Orton called attention, as follows, to evidence that in pre- glacial times the Olentangy Valley was a prominent channel traversing the Scioto Basin:’ The levels run in the construction of the Worthington and Dublin turnpike show that low water in the Olentangy west of Worthington is 16 feet lower than low water in the Scioto at Dublin. The Scioto exceeds the Olentangy several times in volume, and, other things being equal, its valley should be much deeper. It is also to be noted that the disparity would be still more striking if the actual depths of the valleys were taken into the account. The Olentangy runs upon drift beds, the shales having been cut out to an unknown but probably considerable depth, while the Scioto at the point named has a rocky floor. The contrast between the valleys in width is equally marked. As already stated, the Scioto Valley in the northern half of the county is but a narrow gorge, walled with vertical cliffs. Its bottom lands are of small extent and often there is no interval whatever. The valley of the Olentangy, on the other hand, often attains a width of 2 miles, and is seldom less than half a mile. BOWLDER BELTS. The impression prevails among the residents on the plains southwest of Columbus that there are bowlder belts some miles in length that traverse the district at angles quite different from the trend of the bordering moraines. One of these is said to pass from the uplands 14 miles southwest of Darbyville, eastward across Darby Creek and the uplands between that stream and the Scioto, coming to the Scioto nearly opposite the mouth of Little Walnut Creek. The writer has crossed this supposed bowlder belt at several points and endeavored to outline its course and width, but found that it is not sufficiently well defined to admit of ready mapping. Ina general way, however, it may be said that bowlders are more numerous along the line designated than on the bordering tracts, though intervals of one-half mile or more occur along the line where bowlders are rare, while 1Geology of Ohio, Vol. III, pp. 598, 599. 436 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. in places on bordering tracts. they are numerous, so that there does not appear to be a well-defined belt. Probably the bowlders were deposited during the retreat of the ice from west to east, surface bowlders having accumulated on the ice sheet along a line in harmony with the direction of movement. Another tract where bowlders are sufficiently numerous to excite remark lies between Midway and Mount Sterling. The writer did not examine this district so carefully as the other, but has the impression that it will be even more difficult here to make out a belt or train of bowlders than in the district just described. Aside from these two districts no exten- sive tracts were reported where bowlders are conspicuous; they are, how- ever, not rare in any part of this inner border plain except where silt deposits occur, as noted above. INNER BORDER PHENOMENA IN THE SHOULDER. In the shoulder east of the main Scioto lobe, there is, between the main morainic system and a series of moraines which follow the continental divide, a hilly district covering southwestern Summit, southeastern Medina, northern Wayne, and central Ashland counties, in which occasional small tracts were noted that have morainic topography, but the greater part of which is nearly free from drift knolls and covered with but a thin drift deposit. It is thought that these small morainic tracts are the correlatives of the feeble though well-defined moraines which appear im the northern part of the Scioto Basin, and which are deseribed below under the name of Powell and Broadway moraines, since they lie, as those moraines do, between the main morainic system and that series. These moraines are easily trace- able in the smooth Scioto Basin, but in this hilly district would be recognized only by very careful tracing. The ice sheet appears to have formed less continuous ridged or morainic deposits in this district than in the Scioto Basin, for, after careful examination, the writer has been unable to connect into a belt the several patches of morainic topography which were observed. The drift has an average thickness of scarcely 20 feet.on uplands, and is composed mainly of till. It is thinner and more compact than the drift in the moraines to the south. The valley drift has greater thickness. That found in tributaries of the Tuscarawas and of Killbuck and Mohican creeks, which head in the moraines north of this district, is considered in connection with those moraines. AN -H1I709 9 NZIS SOnie / ~T , f uoqnosmg (| / Beene = s Mien soe ss 5 everetieee esses | Notes, 1890. Leroy Township, Lake County.--.| S. 45° W .-_....._...._.- REA Cee ee | Vol. I, p. 530. In the majority of the striated exposures, the bearings of which are given in the above table, no striking peculiarities were noted. The expo- sures are usually but a few square yards in extent and exhibit well-defined erooves of various sizes from an inch or more in breadth down to those more properly denominated striz. Nearly all the striated exposures yet discovered are on the Carboniferous sandstone and conglomerate. Owing to the coarseness of texture of these rocks, they received few fine strize, but coarse strize are common, and glacial planing is very marked in many of the exposures. The occasional striz noted in the above table, whose bearings are out of harmony with the general glaciation of the districts in which they occur, can not perhaps be wholly accounted for at the present stage of investigation, but it is probable that local topography exerted a measurable if not a controlling influence on the movement of the ice sheet at such places. No clear evidence was discovered that they were the product of a distinct ice invasion of a much earlier or of a much later date than the general glaciation. J. C. Anderson’s quarry near Jamestown, Pa., where an instance of cross striation was found, is situated on the north side and about 100 feet above the bottom of an east-west valley. There is a general glaciation, including glacial planing and grooves bearing 8. 18° E., across which there —— STRLZ IN THE GRAND RIVER LOBE. 467 are scattered strize formed subsequently, which bear 8. 2° to 10° W. The rock surface dips southward; i. e., away from the advancing ice sheet. The later striation and possibly the whole glaciation may be due in large part to a sloughing of the ice from the quarry toward the valley, giving the striz a more southerly course than the ice sheet had as a whole, for nearly all the strize in the vicinity have a southeastward bearing. At the exposure 4 miles southeast of Greenville, near Salem Church, where cross strize occur, a projecting pomt of the east bluff of the Shenango River is glaciated. The glaciation where the Greenville and Mercer road crosses covers a part of the north slope, the crest, and considerable of the south slope of this ridge-like pomt. On the north slope and crest the striae have a general southeasterly bearing, with variations of but a few degrees, but on the south slope great divergence occurs. About 20 rods south of the crest and 15 feet or so lower is an exposure in which the heavy glaciation is §. 17° E. About 20 rods farther south is a glaciated surtace which descends southward with the slope of the hill, the descent being about 4 feet in a distance of 40 to 50 feet. The striz vary from $. 8° to 50° E., the earlier and heavier glaciation being nearly southeast. The later glaciation varies from §. 8° to 35° E., and includes several large grooves. It consists of scattering strie and grooves, with but little glacial planing, the earlier glaciation being but slightly effaced. The deflection toward the south on the south slope of this point of land may have been influenced largely by the lower land there. The absence of cross strize on the north slope and crest seems to favor this idea. In the quarries 14 miles southeast of Cortland, Ohio, where cross strize occur, there are two sets, an earlier, bearing 8. 10° E., and a later, bearing about 8. 8° W. The earlier is a heavy glaciation with grooves several feet long, the later a series of irregular gouges a few inches in length. This quarry shows signs of disturbance, the blocks in it inclining toward the west with a dip of several degrees. Whether or not the disturbance occurred while glaciation was going on, and whether, if it did take place at that time, the change of dip caused the change of bearing, the writer was unable to decide. In Bartholomew’s quarry, southwest of Andover, Ohio, the heavier glaciation is 8. 25° E. The lighter glaciation, bearmg 8. 5° to 8. 10° W.., consists of scattering grooves. he relative ages of these sets was not determined, there being no place where both sets occur on a single surface. 468 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The ledges southeast of Garrettsville, Ohio, which exhibit striz ranging from 8. 55° to 86° W., do not -present clear evidence that separate sets are inscribed, there being numerous striz and grooves with intermediate bearings. This is also the case with the striee at Hiram, Ohio, there being in the ledge west of Hiram College strize at all angles from 8. 40° to 62° W. In the above table appear several cases of cross striation which were noted by the earlier observers, but which the writer has not examined. INNER BORDER PHENOMENA. GENERAL FEATURES. The inner border district is limited in this discussion to the small area between this morainic system and the Cleveland moraine, the latter being described in a later chapter. This district is about 10 miles wide in Chau- tauqua County, N. Y., and Warren and Crawford counties, Pa., and 15 to 25 miles in Mercer County, Pa., and Trumbull, Mahoning, and Portage counties, Ohio, comprising in these counties almost the whole area drained by the Mahoning and Shenango rivers. Lying, as it does, adjacent to the outer morainic system, it presents nearly as much variation in altitude as the district covered by that system. The drift, ike that in the morainic system, conceals to some extent the glacial ridges and valleys in the Ohio portion, but is insufficient to do so in the Pennsylvania portion because of the higher elevation and consequent greater depth of the river channels, though its thickness is as great as in Ohio. The drift in the valleys has ereat range in depth, as shown by borings at Jamestown and Fentonyille, N. Y.; Lottsville and Corry, Pa.; French Creek Valley, near Meadville, the Shenango Valley at and below Greenville, Pa., and the Mahoning Valley at Niles, Ohio. There is an average depth of over 100 feet and an occasional depth of 450 to 475 feet. It seems probable that the Shenango Valley has throughout its entire length a narrow gorge filled to a depth of 125 feet or more, there being borings at Greenville, New Hamburg, Big Bend, Sharon, and Neweastle, all of which have between 100 and 150 feet of drift. In certain other valleys borings showing deep drift are very rare, but this does not disprove the existence of channels as deep as in the Shenango, for the valleys have not been adequately tested by borings. Indeed, it is probable that all the large valleys have throughout much of their course nearly as much filling as the Shenango. INNER BORDER OF THE GRAND RIVER LOBE. 469 The following table represents the deepest wells and sections of drift in this inner border district not previously mentioned: List of wells with thick drift. Feet. Greenvale waren CVO Ven Shae se safe: ateta ar crere ia eis miapaiatatoy esa] sieleicia Sistem miner ee Se eee 127 GreenvillewParschoolhouse.s - a. 222s = 2c Jace ews ne ome hes Sek ce sabia nee aelee Seles esteios eae 122 GreenvillesbasDralbeetisuas essa nace aos 5 he Sak sees Sac aae ode dames a ne sewieae eee sane ease 120 Gmreenwilllewear Vine ac kan sae sees os ate = A ee, 6 Se Nos ope inte eal Aopen oie nee ER eee 122 HamaNaEKOnnrol, IL. IN, 1B, \/Gloley Eh too) IROC iNew 6 Seed Socgnegece seaduaebeanc ceoscedeoessuscescas 70 Biog Bend peas aivavyenn WM Oso Chast Ck wer iselseme ance ase sees sesne eee ee eee eases 112 New Hamburg, Pa., boring for gas in Shenango Valley............--.-----.--=.---.---------- 147 ivzaractitere, 12... CLAUS EIKO), 1X0) WOKS eS OURO ao sen eare na aeen oases acon apecses ses saecdoUdosecaso Neoeae 60 Swamp south of Pymatuning station, no rock struck by spiles ...--...-.-..---..-------------- 100 Sharpsvillewbann(seevRepti@)i:8) ie ssaci steccee a sieeinee oa saa ae base oaseess URS See ere 63 Oakland No. 2, Mercer County, Pa. (see Rept. Q°, p.115) ............------.------------------ 110 Slogan Moraes, lea, (See leis QE, jos WIS SNIS)) — ooo e scacs seca sesecoeaccnsosaceecoseseoscces 100 MucddlesexPasi(seelRiep tals) masta se micisine eieeisa Water in gravel at top of rock. ° Sec. 33, T: 8 N., R.5 H---..---.- 178 0 —11 | Water in gravel at top of rock. Stee, G1}, 40 SIN on Wi So oeooooe +120 0 =_ 5 | Several flowing wells about 120 feet deep. Secsyl 273) 0.7 No R. 5 Hees i an 0 =_ 5 | Several flowing wells 120 to 140 feet deep. George Pound, sec. 3, T. 7 N., R. 136 0 + 3] Throwsea strong half-inch stream at 3 feet 5 E. ‘ above surface. Water from gravel. Stes 10) 40 7 ING Ieee seaoseos 143 0 (?) Water in gravel; rock was not reached. FSteo5 1G}, ANS 7 Ilan Jes) ies Soogseoe 180 12 (?) Water from gravel above the rock. Stee; 1G, "IN, 7 Wop lis Besceossece 135 0 —10 |} Water in gravel; rock was not reached. Stee; 25}, 10 7 Nh, Ik) ee oes oocs 227 70 —25 | Salt water obtained in the rock. iStees 2b IN. Als IS Odes aesccos 226 69 —25 | Salt water obtained in the rock. Slee, 245 INS INlog 1p @) ce esocooes 218 50 —14 | Water found in the rock. Steves 225), 10S (Ios 1861) ins seocgso6 150 0 —15 | Water in gravel at top of rock. NStat@; ay, 10 INA 1B) eooeesoe 150 8 —15 | Water from gravel above the rock. Sth 0h UN ff INlop 18, Oe secceae 130 0 —17 | Water in gravel at top of rock. ISOs 205 40S 7/ ING 1a, Go Soc ea ane 160 3 —14 | Water from the rock. Archbold village --....-----.-- 146 2 (?) Water from the rock. J. Sigg, sec. 11, 7.7 N.,R.6E., 280 80 Dry. | Nineteen wells were bored, of which this 2 miles north of Wauseon, on is the deepest: all dry. crest of moraine. (Steves 118}, 10, 7/ Slog 18 GID sooeeaens 210 45 —38 | Water from the rock. Secu vin /MNe RG Heese acess 180 10 —40 | Water from the rock. Sec. 15, 7.7 N., R.6 E., 2 miles 300 100 Dry. | Two holes were drilled; both dry. northwest of Wauseon, on crest of moraine. BLANCHARD OR DEFIANCE MORAINE. 601 Deep wells in Fulton County, Ohio—Continued. Location of well. aoe Feet. Sec. 15, T.7 N., R.6 E., perhaps 210 } mile south of last boring. Sec. 20,T.7 N.,R.6 H...--..--- 210 Sec. 20, 1.7 N., R.6 H.._.:-.--. 179 Wauseon, C. S. Clement ----.-- 265 Wauseon, William Hubbell ---- 154 Wauseon waterworks, 1 mile 159 south of city. Sec. 24,T.7 N., R.6 H...------- 190 Stee, AS IU, 77 Who lit G1 ocsasccece 228 Sec. 28, T.7 N., R.6H.-...----- 160 Sec. 30, T.7 N., R.6 H.-.------- 168 Near Pettisville, sec. 30, T. 7 N., 162 R.6 E. Near Pettisville, sec. 30, T. 7 N., 154 R.6 E. Near Pettisville, sec. 31, T.7N., 164 R.6E. SecyolmDa7iNp i Gebeene meee 150 Sec: olds 7 N-, Rh. GBeseee ess. - 226 Sec. 31,2. 7 Ni, R.6 B.-----.--- 218 Sas B10 77 Whog 18s 818i acecedoce 225 Sec. 33, T.7 N., R.6 H...-...--- 266 Sees 68h, Us 77 Wop 186 OSes eacesens 161 S23, BBY WU Tf Ion In Wisscsccoses 218 Sec. 34,1. 7 N., R.6 H.-._....-- 154 Sec. 34, 7.7 N., R.6H.......... 165 Seo, By, 0 0 Who, is Ol ooccssoee 185 See: 36; 1.7 N.,R.6 Be. ---.-__- 165 Sexes 10 HN [og 18s 0 ee cedosened 182 Stoen G 0, 7 Nos IR Wy cooueesee 160 SOs 10 Nios 18s 7 Wine seoeeee 156 Delta on Belmore beach ------- 122 Sec. 14, T. 7 N., R. 7 E., near 90 Belmore beach. Sexes U5), 40S 7 Who Tks 7 Bicep co aeoods 176 Neca Gnd Neher bee eee ae 142 Altitude ee Remarks Feet. Feet. 10 (?) Brackish water obtained in the rock. 10 —30 | Water from the rock. 16 —15 | Water from gravel above the rock. 115 (?) Brackish water from the rock. 2 36 | The head was at first only 16 feet from top; water suitable for boiler use. 0 —50 | Water from gravel; rock was not reached. 34 —12 | Water from the rock. 50 (?) Water from the rock. 0 —20 | Water in gravel at top of rock. 12 —24 | Water from the rock. 0 —22 | Water in gravel at top of rock. 0 —22 | Water in gravel at top of rock. 0 —26 | Water in gravel at top of rock. 10 —30 | Water from rock; altitude of rock surface about 620 feet. 0 —24 | Water from gravel at top of rock; altitude of rock surface about 530 feet. 0 —24 | Water from gravel at top of rock. 0 —30 | Water from gravel; rock not reached. 50 —30 | Water from the rock. 0 —20 | Water in gravel at top of rock. 18 (?) | Water from the rock. 0 —22 | Water in gravel at top of rock. 0 —s30 | Water in gravel at top of rock. 0 —30 | Water in gravel at top of rock. 10 —30 | Water from the rock. 12 —25 | Water from the rock. 3 —18 | Water in gravel at top of rock. 0 —14 | Water in gravel at top of rock. 12 —22 | Water from the rock. il -++ 5 | Flows a strong 2-inch stream. of well mouth about 730 feet. 36 —80 | Water from the rock. 7 —22 '! Water from the rock. 602 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Deep wells in Fulton County, Ohio—Continued. Depth in Head from Location of well. depth rock. surface. Remarks. Feet. Feet. Feet. Secs LS iNes Rend Hs = sees 160 10 —25 | Water from the rock. Steve 1G), 77 Wop J&ts (/ We coocescar 133 (?) —20 | Water from the rock. Sec:..20) 0.7 N.,R. 7 Be. ------ == 147 12 —16 | Water from the rock. Sec. 21,T.7 N., R.7E..--....-- 150 | 15 | —22 | Water from the rock. Sec. 21, T. 7 N., R. 7 E., near 135 17 —15 | Water from the rock. Belmore beach. Sere, 2B} NS 70 Whos dkts (Bic coaoo occa 97 0 (?) Rock at bottom. Sece2 aaa (eNe Rer(abece eee 137 17 —14 | Water from the rock. Seex27eu7eNRaMbescesee cee 170 0 0 | Water flowed when first struck from gravel at top of rock. See, BO, 0S 7 Whag ls (les ccascaoc 168 @) —10 | Water from the rock. Sec. 30, T.7 N., R.7 E._.------- 160 20 —18 | Water from the rock. Secvol Da 7aNe) Riv Beeseecese- 165 0 —30 | Water in gravel at top of rock. See, Sil, O 7 Np Rb 7 We osesccoce 126 5 (?) | Water from the rock. Secyo2aeiimNe, Raise aes 116 23 — 4 | Water from the rock. Sec. 32, T. 7 N., R. 7 E., near 167 6 — 5 | Well overflowed when first made; water Belmore beach. from gravel at top of rock. Sect 34) MeV 7Nee Rea Beane cee 80 3 —18 | Water from the rock. SechiSncla7Nuk Subens seen 95 2 —12 | Water from the rock. Stee, Gh AMS. 7 Wlop Jets Ip oecosaes 78 2 —12 | Water from the rock. SEG Jb WE IN IR, SI desesssse 85 3 —12 | Water from the rock. Sec. 20, T. 7 N., R. 8 E..-.-..- 103 12 —16 | Water from the rock. Sec2 2s eiieN eee Smee ae eae 82 | 2 —12 | Water from the rock. Reo, Diy 50, 7 Wey IR, B Wesesosne 87 | 3 — 6 | Water from the rock. Slats ZB); Als 7 Why IRh 8) I ceceoce 92 0 (?) Water in gravel at top of rock. Secuodaminw/m@ NE wR ate ase ene 72 12 —18 | Water from the rock. Sees by AN, 7 Whey IRs 3 Wiscsescon 60 2 — 9 | Water from the rock. Stas Wh Ws @ INloy Io (8 Doo scesce 140 0 (?) Water in gravel at top of rock. Sec. 1, T. 6 N., R. 6 E., near 142 10 —32 | Water from the rock. Belmore beach. See. 1, T. 6 N., R. 6 E., near 64 2 — 8 | Water from gravel above the rock. Belmore beach. Sec 2y ela OU Nese Ry nominee oe ar 175 4 (?) Water from gravel above the rock. Seems UDNiGRNE RS Gel eeee eee ae 142 10 —32 | Water from the rock. Sec. 5, T. 6 N., R. 6 H.-.--..-. 182 0 Dry. | Four holes were bored; all dry. Sec. 6, T. 6 N., R. 6 E., near 180 0 —42 | Water found in gravel; rock not reached. crest of moraine. See5 7 105 GING Ik GDS ssosccoe 175 40 —22 | Water from the rock. Sees 0 Who @ Nhs 185. G18 .se6ecce0 135 0 —18 Three wells, 132 to 185 feet deep, obtain water at top of rock in gravel, head 17 to 22 feet from surface. BLANCHARD OR DEFIANCE MORAINE. 603 Deep wells in Fulton County, Ohio—Continued. Total Depth in |Head from Location of well. depth. walle. Rnracel Remarks. Feet. Feet. Feet. Sere, fh Us GINS Ge ee cescre 142 0 —24 | Water in gravel at top of rock. Three others, 126 to 137 feet, from same bed of gravel. Sec. 10, T. 6 N., R. 6 E., near 122 2 — 7 | Water from the rock. Belmore beach. Sect il2;i6UN.4 ReG) Bes. 5-- 5. 181 41 (?) | Water from the rock. Sees Gh dbs GAINES Ry (fee oesoocad 89 5 — 5 | Water from the rock. Sec. 0, T. 6 N., R. 7 HL. 2 22-2. 100 0 — 8 | Water found in gravel. SEG, fh Wt GI gs. Y lie bSaccsce 97 0 (?) Water in grayel at top of rock. Sees Sh IE ING IRs Wee send 61 38 —l1 | Water found in rock; a neighboring well 82 feet. Sieve; 10, 40s @ Nes 1, 7/ Bee seooae 90 22 —10 | Water found in rock. North part of T. 6 N., R. 8 E_-- 82 12 —14 | Several wells in rock at 65 to 82 feet. A buried channel shown in the above table in a boring near Pettisville in sec. 31, T. 7 N., R. 6 E. appears to lead eastward, passing about 14 miles south of Wauseon, where it is filled with 225 feet of drift, and thence north of east. Its course was roughly determined by Orton for a distance of about 9 miles by means of well borings, there being no surface indications of its position.’ Orton in the paper just cited also made the following state- ment concerning the drift deposits near Wauseon: The uppermost 10 to 15 feet consists of yellow clay, oxidized. Below comes blue clay, often so charged with slate fragments and waste as to be almost black. Thin seams of sand are irregularly distributed through the mass. Large bowlders, though rare, are not unknown. ‘The boundary between the yellow and blue clays is not sharp or well defined. The change in color simply marks the line to which the surface water is able to descend. The blue clay reaches a general thickness of 130 to 150 feet. Below it about 5 feet of hardpan is found. This is here described as cemented gravel. Under it a few inches of sand are usually found, and then the Ohio shale is reached. Many of the Fulton County wells contain a small amount of inflam- mable gas which is usually struck at the base of the drift. It is probably derived from the underlying shale rather than from decomposition of organic matter in the drift. The salinity of the water obtained in the Ohio shale is 1 Rock waters of Ohio, by Edward Orton: Nineteenth Ann. Rept. U.S. Geol. Survey. Part IV, 1899, p. 708. 604. GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. quite general, though seldom so strong as to render the water unfit for use. The drift deposits also yield a slightly saline water, the salt being obtained probably from the shale fragments in the drift. SILT DEPOSITS BENEATH MORAINIC DEPOSITS. Along several valleys in northern Ohio there are heavy deposits of silt beneath the till, which are of considerable interest, not only because of their great amount, the depth being in places fully 200 feet, but also because of their position beneath deposits of till and coarse assorted material. E. W. Claypole some years ago called attention to the silts in the Cuyahoga Valley in a paper entitled ‘““The Lake age in Ohio,” read before the Edinburg Geological Society,’ and outlined the probable extent, in this and other valleys tributary to the’ Lake Erie Basin, of lakes in which it is supposed the silts were deposited. This outline was based largely upon a hypothetical conception as to the position of the ice margin, the lakes being considered glacial foot lakes, held between the retreating ice sheet on the north and the Great Lakes—Ohio divide on the south, with outlets across the divide into the Ohio drainage system. The history of the deposition of these silts proves to be more complex than the paper leaves the reader to suppose, since the occurrence of morainic deposits upon their surface shows clearly that they are of earlier date than these moraines. Furthermore, the actual outline of the ice margin (as shown by its moraines) is so different from Claypole’s theoretical outline that his mapping of glacial foot lakes needs revision, there being bulky moraines in the midst of the districts where he supposed lakes to have been, and in which no evidence has yet been recognized of deposition in lake water. The Fort Wayne and Wabash moraines, in their distinct portions in northern and western Ohio, carry little silt on their surfaces and are not underlain by heavy deposits of silt, such as underlie the moraines of this series in the Cuyahoga Valley and other valleys in the hilly district, though they cross the districts where the supposed lakes were located. The geographic distribution of these silts is, therefore, much more restricted than Claypole’s maps indicate. On the Cuyahoga Valley and in the Grand River Basin the deposits are rather extensive, being 1 to 3 miles in width and 100 to 200 feet or more in depth, but in Chagrin, Rocky, Black, Vermilion, Huron, and Sandusky River =A) 1 1 Trans. Edinburg Geol. Society, 1887. BLANCHARD OR DEFIANCE MORAINE. 605 valleys their amount is very slight, the greater part of the sections exposed in their bluffs being ordinary till with little or no surface capping of silt, and with only occasional exposures of silt beneath the till. The slight exposures which occur may indicate that there were extensive deposits of silt in these valleys previous to the last ice invasion, the greater part of which was removed by the advancing ice sheet. In the Cuyahoga Valley the amount was too great for the ice sheet to remove The silts exposed along the Cuyahoga are not so fine (at least in the southern portion of the valley) as those in certain other valleys, being sufficiently coarse for the detection of individual grains by the naked eye; they are called quicksand when penetrated in wells. So far as examined by the writer they are entirely free from pebbles, but Claypole reports the occurrence of an occasional pebble and very rarely a large stone. They are horizontally bedded, or nearly so, the thin layers or laminz being dis- tinctly traceable, since they are in places separated by thin partings of sand. The color is generally blue, though in the upper portion it is yellow to a depth rangmg from 10 up to 50 feet or more. The silt is notably siliceous, but contains also considerable lime and iron. The amount of lime increases perceptibly in passing from south to north along the valley, there being in the southern portion scarcely any nodules of lime and but a faint response upon application of hydrochloric acid, while in silts from the northern portion, from the vicinity of Peninsula northward, lime nodules abound. The silt is also more compact in the northern than in the southern portions of the valley. In exposures east of Everett, crystals of sulphate of lime occur in the blue silt. The silt here rises in a solid bank to a height of 225 feet (barometric) above the river or about 360 feet above Lake Erie, and is capped by 15 to 20 feet of till in which large bowlders are embedded. The yellow silt here has a thickness of about 50 feet, the greatest thickness observed in any exposure along the valley. The highest observed altitude of the silt is in the lowland tract west of Akron (which leads from the Cuyahoga through Copley Marsh to the Tuscarawas River), where it reaches an altitude 375 to 400 feet above Lake Erie. It stands higher here than in the valley that leads through Akron along the line of the Ohio Canal. In each valley there are heavy deposits of gravel or other coarse material above the silt. In the western valley there is till as well as sand and gravel; in the eastern, sand and gravel alone are reported. The 606 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. summit in the valley west of Akron, as shown by the survey of the Northern Ohio Railroad, stands 425 to 435 feet above Lake Erie, while the summit along the Ohio Canal is 396 feet. In the northern portion of the Cuyahoga Valley the upper limit of the silt decreases to 200 feet or less at the borders of the old lake terraces. In the other valleys tributary to Lake Erie the silt deposits which have been observed beneath the till have the compact texture and nearly entire freedom from pebbles of those in the northern portion of the Cuya- hoga Valley, and, like them, contain a large amount of lime, as shown by nodules and by effervescence with hydrochloric acid. In the valley of Chippewa Creek and River Styx, which lead southward into the Tusca- rawas, the silt deposits are known only by records of wells bored in them, and the writer had no opportunity to see specimens from these wells. The streams which lead northward from the continental divide are more rapid than those leading southward, and consequently have deepened their valleys sufficiently to expose nearly the whole section down to the rock floor. It is not improbable that silt deposits similar to those exposed along these northward-flowing streams occur also beneath considerable portions of the low interfluvial districts of northern Ohio, whose altitude is but little above the streams, as is the case between the tributaries of Black River and between Black and Rocky rivers, but no exposures were observed in that district which reached the bottom of the till. In the hilly districts from Rocky River eastward the silts are apparently confined to the valleys. The age of these silts and the conditions under which they were deposited afford material for much study and speculation. The silts may represent several distinct depositions at intervals widely separated, though no evidence was found to support this conception, the heavy deposits on the Cuyahoga presenting, so far as examined, no unconformable beds and no alternations of oxidized and unoxidized silts. The silts were probably deposited, as suggested by Claypole, in bodies of water outside the ice sheet, the ice sheet acting as a barrier to prevent northward drainage of the water, though it is possible that in some cases they are the deposits of sub- glacial waters. The scarcity of coarse material in these deposits, however, seems to strongly oppose the hypothesis of subglacial deposition. The fringing lake may have been formed either during an advance or a retreat, or have embraced both an advance and retreat in cases where the ice failed BLANCHARD OR DEFIANCE MORAINE. 607 to reach to the divide, the size of the lakes varying with the position of the ice margin. The greater altitude of the silts at the southern end of the Cuyahoga Valley than at the northern presents an interesting problem. The silt may have reached, at one time, as great altitudes along the sides of the northern portion of the valley as it presents on the southern, and have been removed afterward by the advancing ice sheet or concealed by its morainic deposits; or it may never have had as great altitude in the northern as in the south- ern portion of the district, the northern portion being a deep-water and the southern a shallow-water deposit. Since it is a partially concealed deposit its limitations, both geographic and hypsographic, are difficult to determine. The extreme rarity of pebbles seems difficult to explain, for if the silt were deposited in narrow lakes outside the ice sheet it is to be expected that tributaries would discharge large amounts of coarse material with the fine into the valleys occupied by these lakes, which would make a percep- tible increment to their deposits. This coarse material might, however, have been dropped at the borders and only the fine material have passed out into the midst of the lake. A more careful examination of the gorges tributary to the valleys may throw light upon this matter. STRILZA. The strie of this district, so far as observed by the writer or reported by previous observers, are represented on the glacial maps (Pls. 1, dk XIII, and XV), and their bearings are given in the table of striz below. In general, the strize bear directly toward the moraines; thus, in the vicinity of the lower course of the Cuyahoga, they bear southeastward; in the Sandusky-Scioto Basin, southward; in the Maumee Basin, west of the San- dusky River, southwestward to westward, while in southeastern Michigan the bearing is north of west. There are, however, slight changes of course in the ice currents, shown by cross striation or by lack of harmony in the bearing of strize in neighboring districts, which may be better comprehended by reference to the maps than by a description. The greatest variation on any single surface which the writer has noted is that east of Vermilion River, near the line of Erie and Huron counties, where the strize appear at nearly all angles, from 8. 19° W. to S.. 77° W., their prevailing bearing being 8. 35° W. They all consist of 608 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. short lines, none of them exceeding a yard in length, while many are out 6 to 12 inches. A few of them are curved, with their convex side toward the south. The best-defined curved striz are about 2 feet in length, and their departure from a straight line within that distance is fully 2 inches. Gilbert reports an observation on West Sister Island, in Lake Erie, showing still greater difference in bearing, there bemg a general glaciation S. 80° W., and a single observation of striation in a north-south direction which he designates the ‘intersecting series.” He considers the southward striation merely a local feature formed by the retiring glacier at a time subsequent to the heavy glaciation, the strize being parallel to a steep bluff over which the older grooves rise obliquely. Still greater divergencies were noted by W H. Sherzer in southeastern Michigan,’ the range being from about 8. 6° W. to N. 20° W., or 154°. In that region a southwestward movement was followed by a northwestward one. Winchell has reported cross strize in Seneca Township, Seneca County, Ohio, in which the older set bear 8. 5° KE. and the later and intersecting series 8. 23° W. Chamberlin has called attention to the disruptive crescentic gougis displayed in the surface of the quarries at West Amherst,’ whose concave side is turned toward the point of origin of the ice movement. Crescentic cracks of this class he considers the natural result of a movement in which the gouging agent is master of the situation. The “chatter marks” displayed in many striated ledges in other districts resemble these crescentic cracks in frequently having the form of a crescent, but they have their convex side toward the origin of the ice movement. These Chamberlin regards as the result of a movement in which the gouging agent is not the master of the situation, but is dragged across the rock ledges. The remarkable phases of glacial action on the islands of the western end of Lake Erie and in Marblehead Peninsula have been so well described by Gilbert, Chamberlin, Wright, and others that further remarks concerning them seem unnecessary. Plate XVII furnishes two illustrations of heavy glaciation. The movement across these islands which produced the grooves and strize was perhaps a late one, when the ice had only the Maumee Basin in which to deploy. There are several striated exposures in northern ‘Geology of Ohio, Vol. I, pp. 538, 539. * Geol. Survey Michigan, Vol. VII, 1900, pp. 128-132. *Seventh Ann. Rept. U. S. Geol. Survey, pp. 219, 220. U. S. GEOLOGICAL SURVEY MONOGRAPH XLI PL. XVII ae SE A. GLACIATED SURFACE ON MIDDLE BASS |SLAND, IN LAKE ERIE. B. LARGE GLACIAL GROOVE ON MARBLEHEAD PENINSULA, NEAR LAKESIDE, OHIO. BLANCHARD OR DEFIANCE MORAINE. 609 Ohio which apparently belong in this late series. For example, at South Euclid and near Berea, and in the Sandusky Valley north of Tiffin, the movement was southwestward, corresponding well with that on the islands of Lake Erie, but somewhat out of harmony with the moraines and with the movements a few miles to the south. It is probable, therefore, that in the closing stages of glaciation, after the Scioto and Miami lobes were absorbed, the ice movement assumed more nearly the direction of the longer axis of the Lake Erie Basin than it had at the time these lobes were in existence. Location. ] Bearing. Observer. Newberry Township, Geauga County...-....----.--- Seb0SRE ese aes eae ee Read. Chester Township, Geauga County .-..-----.------. SOB sae ae eee Read. Russell Township, Geauga County ---..-----.-.---- | Sb BO? to 70? Bosses Read. Russell Center, 1 mile southeast of --........-....-- SSS elto bbe wba ay, aaa" Leverett. Bainbridge Township, Geauga County...-..---.---- |} Sire) 10) ee soseoscesaae Whittlesey. Solon Township, Cuyahoga County ...............-| 8. 45° H..._____..__._.. | Whittlesey. Solon Center, 1 WHS MORIN Oh scocasceasunccsesesoce | SP ZO FB ees Rea ees Leverett. Twinsburg, Summit County.............---.------- | Sh SO? st) 4} WD ees osse Leverett. Hudson Township, Summit County .-.-.---.-.-.-.- Sh Gi” 1 OO! IB). seek Read. Boston Ledges, Summit County ..--.-.------------- sh G0? (Wo) 49) 10s oa coe Read. Boston Ledges, Summit County -.--......---------- le WWie (bOME) ao ek a «ae eennehes Read. Rermuinslke, Skormooils Cowlhy 52 sceassdccoossoosee nese Sb HO? to BO Bie soscode Leverett. Independence, Cuyahoga County ...-..-.-..--.---- [S202 STH Ce ete See Nema | Whittlesey. TBiMKS|autom, Wey jaowilelss SOVONIN Cit soasoosanessosoeeessens | Ss iOS) 10? TB) os socseas Leverett. North Linndale, 2 miles southeast of ---.........--- | Sh 7 1@) MOP WY sch. s4 5 | Leverett. iB Creare esteastyOlem ace era c cnaee les ioe nae Sy 222 toss? Witerper eee | Leverett. County line north of Brunswick. ...-..-...-.------- | Se woth BO? 19) 342522 2-o22 Leverett. West Amherst, Lorain County -.....-.-.---....--.. [SS BOQWiec cee eaters Leverett. entice ita Worain Countyeereres ese ne eens eee. | tS OP Tro SI? WY cs cecase Leverett. Birmingham); 2rmilesisounhwotess=ss2=s= = se saee ee Sh USP 110) 7 WY ac sccceas Leverett. Townsend Township, Huron County -...--..---.--- Sao SeWh So teste aeeeees| Read. Sam cus kava (STODSE nya blONS) peas eee eee see Sti (9 Wo) SHO WY ooo eke | Newberry. IPiisio=lseay Wisknael, IMA Iii) o. sees seesee ease cee 9.380? Wires enme ceeee | Newberry. Put-in-Bay Island, Lake Erie -.......-..----.------ [S.LOPr Wi taeaeseseete saan | Newberry. South Bass Island, Lake Erie -....--....----- Sees JOOP: WW Sec oe cele tee | Gilbert. Kell eysiislam dep Wale shiniesne) <2) seesco sean oe se UM WOO WY Soe ecee | Newberry. West Sister Island, Lake Erie...............-.....- Sii80 Caisse a seen tee | Gilbert. West Sister Island, Lake Erie...................--- INFtONS ss see eee emecicee Gilbert. IB ellen eenen ime mete else ciscisiciecneececesecicbee SiiOb 2h Weeet asa migceme Gilbert. Republicn 4ammiles\eastOte= 9s qe 535) 5 sesso seie SsZoeeW eae ageee eich ae | Leverett. Cac, Chemie: Cowan? 2. .eeessssesceacescesesoace S62 5W) sas ouercinc clasevera | Gilbert. MON XLI 39 610 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. List of strive between the Defiance moraine and the west end of Lake Hrie—Continued. Location. Bearing. Observer. Genoa, one-half mile north of........-------------- |S: 609 Wi eo eae nie Winchell. Section 18, Harris Township, Ottawa County -.---.- PASO RAN Uteemeti ns. Winchell. Portage River, west line of Sandusky County --.----- | S.1080 Wie eeseaseeeee Winchell. Section 35, Jackson Township, Sandusky County--. | S500? We St Sie oe eee Winchell. Section 7, Portage Township, Wood County -...---- [S200 29W Pace Ae eee Winchell. Section 12, Freedom Township, Wood County --.---. Se BOLT Wi excel eer eee era Winchell. Section 9, Freedom Township, Wood County ..----- Ss502 Wi ee ee eee Winchell. OtsecowNVood(Countyeeen snes seca eee eee eee Sh (GB) Tho) IS? Wh Sac=secas Winchell. Shahan, JlmKeris| COB, 255 oses cess sesnsnessass0005 Sic002 Wis aateeeeeeaeee Gilbert. Mion clovarelacasiCounbyaeeeseee aes eee enee ee Ba O22 Tee eee eens Gilbert. Hishysiquarry. Wucas) Counbyees assem aes eee 8:00 °NWi eee ee eeeeee Gilbert. Wihitehousesiiicasi County ee seep ese eaeeee nea Ss S0RTWieecee ose seer ae Gilbert. OUTER BORDER PHENOMENA. SMALL GLACIAL LAKES. The position of the Defiance moraine being in large part on the slope toward Lake Erie, the facilities for discharge of glacial waters during’ its production are not likely to have been so good as in the preceding moraines. It is probable that small lakes were formed along the south border of the ice which found discharge either southward across low places on the divide or westward along the front of the ice sheet. One of these small lakes would be the slightly expanded Lake Cuy- ahoga, which had its discharge southward past Akron, as indicated on page 578. Another lake was apparently held in the south part of the Black River drainage basin and found its discharge along a channel leading south- ward from Lodi through the Fort Wayne moraine to Killbuck Creek at an altitude a little more than 900 feet above tide. From the Vermilion River westward there was drainage along the ice margin to Lake Maumee, but the water leading westward from the Vermilion drainage basin was apparently gathered into a narrow lake in the Huron River Basin near New Haven that discharged past Attica to another narrow lake in the Sandusky Basin. The latter discharged west- ward from near Carey to Lake Maumee at Findlay. The line of discharge past Carey is marked by a definite channel brought to notice by Winchell? 1Geology of Ohio, Vol. I, 1873, pp. 626-628; with map of channel. BLANCHARD OR DEFIANCE MORAINE. 611 The chain of lakes and connecting channels just outlined show a decrease in altitude in passing from east to west. The channel in the Vermilion drainage basin is estimated to have an altitude about 950 feet above tide and descends about 25 feet to reach New Haven in the Huron River Basin. The extensive New Haven Marsh, which extends westward from the Huron Basin near New Haven to the head of Honey Creek (an eastern tributary of the Sandusky), near Attica, stands about 925 feet above tide, and probably represents nearly the level of the lake in the Huron Basin. There was a descent of about 100 feet along Honey Creek from this lake to the one in the Sandusky Basin, for the outlet of the latter near Carey is only $15 to 820 feet above tide. The descent along this outlet from Sandusky Lake to Lake Maumee at Findlay was about AO feet in a distance of 15 miles. The head of the outlet of Sandusky Lake is reported by Winchell to carry a deposit of black muck ranging in depth from 4 or 5 feet up to 8 feet or more, which is underlain by a marly or calcareous blue clay. These deposits have probably accumulated since the channel was abandoned RELATION OF THE DEFIANCE MORAINE TO LAKE MAUMEE. Several references have already been made to the beaches and outlet of the glacial Lake Maumee, but its relation to the Defiance moraine has not been clearly stated. As the beaches and outlet are discussed in some detail farther on, only the general relations to the Defiance moraine will now be considered. When the Defiance moraine was traced by Gilbert, some thirty years ago, it had not been determined whether the lake which discharged through the Fort Wayne outlet into the Wabash was held at its high level by the ice sheet or by a land barrier. Gilbert seems at that time to have favored the land-barrier hypothesis and considered the lake entirely postglacial, while Newberry considered the ice dam formed by the retreating ice sheet an adequate cause, and referred it to the closing part of the Glacial epoch." It soon became evident that the land-barrier hypothesis had no foundation in the topography of the region, and attention was directed to the question of the relation of the beaches to the moraines of the great ice sheet. Gilbert took the lead in this investigation and discovered that the beaches do not 1Geology of Ohio, Vol. I, pp. 549-552; Vol. II, pp. 8, 51, 52. 612 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. completely encircle the basin, but terminate in a successive series from higher to lower in passing from northern Ohio eastward into southwestern New York. He did not, however, attempt to map the moraines which were formed subsequent to the Defiance moraine and work out the full correlation. A part of this work has fallen to the present writer, and it is now possible to speak with some assurance concerning the correlations on the south shore of Lake Erie. The correlations on the north are not fully worked out, though studies by Taylor have thrown much light upon them. In an early stage of the investigation the writer supposed that the Defiance moraine was nearly the full correlative of the upper beach of Lake Maumee, and that with the retreat of the ice sheet from that moraine the lake level soon fell a few feet to the Leipsic or second Maumee beach. This interpretation, which was published in 1892,’ was erroneous in that it limited the upper beach to the district outside of the Defiance moraine. It is now known to be developed as far east as Cleveland, and to be identical, from Leipsic eastward to Cleveland, with the beach which in 1892 was sup- posed to be the second Maumee or Leipsic beach; it has not been found east of Cleveland. It has also been traced northward in Michigan to the Imlay outlet, near Imlay City, and may be traced still farther north. The course and known extent of the beach may be seen in Pl. II. These later developments, while indicating that the lake held its highest level long after the Defiance moraine had been formed, do not in the least antagonize the hypothesis that the ice sheet constituted the limiting barrier on the northeast border of the lake. The fading out of the beach near Cleveland and the connection there with a moraine later than the Defiance brings the strongest possible support to that hypothesis, as will be shown farther on. The lowering of the lake level obviously depends upon a change in the lake outlet, and, as in this case, it may have no relation to the withdrawal of the ice sheet from a given moraine. It having been ascertained that the Defiance moraine is not. the -full equivalent of the upper beach of Lake Maumee, the question to be deter- mined is what fraction of the upper lake stage the moraine equals. As Lake Maumee occupied the district outside of the Defiance moraine while the moraine was forming, it may be thought that a comparison of the strength of that part of the beach with the part formed inside the moraine 1Am. Jour. Sci., 3d series, Vol. XLIII, pp. 284-290. 1 BLANCHARD OR DEFIANCE MORAINE. 615 will furnish a ready answer to this question. The solution is, however, not so easy as might be expected, for the beach varies greatly in strength in both districts. It is weak where the descent on the lakeward side is very gradual, and comparatively strong where the descent is rapid. It so happens that in much of the shore outside of the Defiance moraine the lake plain has exceptionally shght descent, often but 5 to 10 feet per mile, while in the part of the shore inside the moraine it is, on the whole, rather rapid. In so far as favorable conditions in one district exceed those in the other a false impression of relative strength is likely to be gained. The impression which the writer has obtained by comparing the portion of the south shore of Lake Maumee outside the Defiance moraine with that inside is that the latter is fully as strong as the former. But upon comparing the northwest shore outside the moraine with that inside there was found to be a decidedly stronger beach outside the moraine and that, too, where slopes appear to be similar. The portion outside seems to have at least double the strength of that inside. The study has not, however, been sufficiently thorough to justify a more precise statement of the relative length of the part of the upper lake stage involved in the deposition of the Defiance moraine. It can only be stated that on the northwest shore it is sufficient to cause a marked contrast between the part of the beach outside and that inside of the moraine. Possibly the part outside required twice the time of that inside, but this seems a rather high estimate. The estimates of relative lengths should be supported by more data than have thus far been collected. INNER BORDER PHENOMENA. The district covered by this description includes, on the east side of the Cuyahoga, only a narrow strip lying between the Defiance and the Cleveland moraine, and on the west side of that river a strip lying between the Defiance moraine and the upper beach of the glacial Lake Maumee. The width of this strip is variable, being 4 to 8 miles from the meridian of Findlay eastward to the Sandusky River, 12 miles on the meridian of Bellevue, a very narrow strip near the meridian of Norwalk, and 15 to 20 miles from the meridian of New London eastward to Berea, beyond which it decreases to a breadth of about 10 miles at the Cuyahoga River and 2 to 3 miles at Chagrin River, east of which it remains narrow. 614 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. TOPOGRAPHY. From Findlay eastward to the west fork of Rocky River this is a nearly plane tract with a decided northward slant, the only prominent exceptions being a small area in northwestern Lorain and eastern Erie counties, cover- ing two to three townships, where occasional sandstone hills rise above the general level. From Rocky River eastward it embraces a hilly district with only a narrow fringe of plane country next to the beach line along its north border. In the district lying west of Rocky River there is some variety in the surface contours, although no part is decidedly morainic. The district between Rocky and Black rivers is exceedingly flat, and so is the narrow tract east of Rocky River between the beach line and the hilly districts, - there being scarcely any knolls so much as 5 feet in height. From Black River westward there are many low swells 3 to 5 feet, and a few 10 feet, in height. They are somewhat irregularly distributed, some sections being thickly dotted with them, while others carry scarcely any. The most conspicuous drift features noted in this district are an esker in Hartland Township, Huron County (described below), and a knoll in the southwest part of the same township, which rises abruptly about 30 feet above the bordering country. There is also a small district south of the Lake Shore and Michigan Southern Railway, in eastern Huron County, where the surface is somewhat uneven, there being valley-like depressions surround- ing island-like knolls whose height is but little above that of the bordering plain. The valleys widen and contract after the fashion of those included among the knolls of the moraine. In the hilly districts the drift is seldom ageregated in knolls, there being only an occasional knoll so much as 10 feet in height. THICKNESS OF THE DRIFT. The thickness of the drift, aside from buried valleys, probably averages no more than 30 feet and may possibly average but 20 feet. In the buried valleys its thickness is much greater, as the rock floor of the larger valleys was probably cut down below the level of Lake Erie, if we may judge from data at Cleveland cited above (p. 595). Remarkably few borings were found which penetrate deeply into the old valleys. Attention has already been called to a line leading from New London northeastward through BLANCHARD OR DEFIANCE MORAINE. 615 Wellington, where numerous wells have penetrated 75 to 110 feet of drift. Aside from this there were but few places found where the drift exceeds 50 feet. One is at W. H. Todd’s, 2 miles north of Florence, in Erie County, where rock is struck at a depth of 77 feet. A mile south of this well is a sandstone hill which rises to a height of 40 to 50 feet above the well mouth. Another is in Hartland Township, Huron County, at a school- house and at the base of the Hartland esker. This well has a depth of 75 feet and does not reach the rock. Around the northern end of the esker the drift has a thickness of only 10 to 20 feet. A gas well in Rocky River valley, at Columbia Center, Lorain County, passed through 40 feet of drift. The well mouth is 20 to 25 feet below the level of the bordering till plain. At Brunswick Center, Medina County, G. B. Babcock has a well 50 feet deep which did not reach rock, but rock comes to the surface just north of the village at a higher level than the well mouth. STRUCTURE OF THE DRIFT. The drift is mainly till, though the valleys, as already indicated, contain considerable silt beneath the till, and there are thin sheets of sand and gravel on the uplands interbedded with the till. It is from these sheets of sand ana gravel that the wells are usually obtained, the abundance or scarcity of good water depending upon their thickness and extent. The till ordinarily contains a large amount of clay, but in the midst of the sandstone hills of northwestern Lorain and eastern Erie counties it is of a sandy nature, furnishing a good illustration of the effect of the local rocks upon the structure. BOWLDERS. The number of bowlders on this inaer border tract is not great, though in certain limited districts they abound. One such district is crossed on the road from Strongsville to Columbia Center. Another is in eastern Seneca County, along the east-west center road in Thompson Township west of the center. Perhaps other similar places occur within the limits of this district, but they have not been noted. THE HARTLAND ESKER. Aside from the beds of assorted material which are interbedded with the till, there are occasional surface deposits of gravel or sand in the form of knolls and ridges, and also in plane tracts. 616 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The only conspicuous gravel ridge observed is the Hartland esker. This ridge lies on a very level till plain in the northeast part of Hartland Township, Huron County, its southern end being near the east-to-west center road, and 14 miles east of Hartland Center, and its length about 2 miles. The trend is nearly due north to south, but the ridge winds slightly, varying 20° or more from a due north-south line. The general height is 10 to 12 feet, but in places a height of 20 feet is attained. The width, including slopes, is only 75 to 125 yards. It is a continuous — ridge, except for a gap near the middle a few yards in width. Two basins were observed on the crest of the ridge, one of which is fully 10 feet in depth and contains a small pond. The northern half of the ridge is sharper and higher and contains coarser material than the southern half. The largest exposure noted in the esker is at a gravel pit in the northern half near the schoolhouse referred to above. It is opened at a place where the ridge makes a sharp curve from a south-southeast course to one west of south. It has been worked back from the outer side of the curve to the inner, the best exposures being at points which show the structure of the inner curve. There is a confused mass of cobble, gravel, and sand, with slight clay admixture, and only indistinct lines of bedding. These, so far as made out, are nearly horizontal. On the outer curve of the ridge the bedding appears to be more distinct than on the inner. Several slight exposures occur between this large pit and the southern end of the ridge. They usually show a thin bed of sandy clay at the surface, which is sparingly interspersed with pebbles, beneath which is gravel of medium coarseness. Residents state that the wells along this portion of the ridge frequently strike a bed of sand which yields some water, after which they enter till near the level of the bordering plain. There is no fan or gravel plain at the south end of this esker, but on the contrary, it terminates abruptly in the till plain. About 2 miles south, however, is found the northern end of the spur of the Defiance moraine described above, which lies along the east side of Vermilion River, and since this spur is composed mainly of gravelly knolls and is so nearly in line with the esker, it is thought that it may have been formed by the same glacial stream which formed the esker, the interval of 2 miles between the esker and the spur having been unfavorable for the production either of an esker or of gravelly knolls. Just how the glacial waters deposited such BLANCHARD OR DEFIANCE MORAINE. 617 ridges and knolls and why the gaps exist are interesting questions which afford room for speculative inquiry but which are not well enough under- stood at present to warrant the rendering of an opinion. THE OLD VALLEY OF ROCKY RIVER. The changes of drainage-in this region, especially in the plane portion of it, have been such that several of the streams are in channels entirely postglacial, draining territory whose preglacial drainage lines are completely filled with drift. Im one conspicuous instance, however, the preglacial course has been abandoned, but not concealed, viz., that of the East Fork of Rocky River. The fact was announced by Newberry’ that the present mouth of Rocky River does not coincide with its ancient mouth, , but comes to the lake shore 2 miles east of it. The river, however, touches its old channel 2 miles above its mouth, one bluff being composed of rock while the other is composed of till. A few years after Newberry’s reports were published, Dr. D. T. Gould, of Berea, Ohio, discovered that the old course of the East Fork of Rocky River may be traced from the point where Newberry left it (2 miles above the mouth of Rocky River), south- ward into Strongsville Township, Cuyahoga County, where it becomes coincident with the present course and continues so to the head of the stream. The present course of the stream is nearly parallel with the ancient one throughout this distance (about 15 miles), lying 1 to 15 miles west of it. The old course is indicated superficially by a shallow, trough- like depression,’ about one-half mile wide and 10 to 40 feet deep, and its existence is confirmed by borings which show that no rock lies near the surface of this depression. The deepest boring (one near the Big Four Railroad) is reported by Gould to have penetrated about 200 feet of drift before reaching rock, showing the rock floor to be nearly as low as the surface of Lake Erie. Along the ancient course, from the vicinity of Berea southward for nearly 15 miles, the Berea grit is wanting for a space of 1 to 15 miles or more, while along the present stream throughout that distance the bed and bluffs are composed of this formation. The present valley is a narrow gorge but afew rods in width, while the ancient one has a width of a mile or more. 1See Gealogy of Ohio, Vol. I, 18738, pp. 171-172; Vol. II, 1875, p. 16. 618 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Gould has published the results of his studies in a Berea newspaper,’ showing in some detail the nature of the evidence bearing upon the question of change of drainage and the manner in which the evidence was brought to his notice. Some of the interesting features along the line of the ancient valley he describes as follows: Extending along the whole eastern border of this village [Berea], and distant from it about a mile, is a chain of what were at one time swamps and small, shallow ponds. These have within a few years been drained, cleared, and brought under cultivation, and to-day are the somewhat famous onion fields of Berea. There are seven of these swamps, each distinct from the other, the divisions in each case being ridges of clay loam of different heights, some being not more than 10 feet and others 20, 30, and in one case nearly 40 feet. The general direction of this chain of swamps is nearly north and south; the direction of the dividing ridges is northeast to southwest. The soil along the crest of these ridges is very noticeably sandy, while the general country everywhere east and west of them has a stiff clay soil. , With the exception of one swamp the drainage is from one to the other through gaps in these ridges, which have been broken through by the contained water in each, into a general reservoir near the center of a swamp muck larger than all the others combined. This reservoir or pond is Lake Abram, and the reclaimed marsh around this pond and also the detached marshes constitute the Berea onion district. This chain of marshes is 24 miles in length. The cross ridges mentioned by Gould, which separate the basins, are composed in the main of ordinary till, though there are places where gravel may be obtained from them. They are evidently glacial deposits, and the basins also date from the glacial period. One basin was observed about one-half mile south of Lake Abram, which is situated on the slope nearly up to the top of the bluff-like border of the trough. At the southern end of the chain of swamps this old channel is completely filled, so that its altitude is fully as high as the bordering plain and slightly above the level of the bluffs of the present stream. The stream, no doubt has taken its- present course because of lower altitude, or at least of less obstruction to its course there than along its old route. It is not improbable that the peculiar features which this old valley displays were present in other deeply filled valleys of the drift-covered region, especially those in hilly districts, and may represent the form of channel in which many of the post- glacial streams began their work. It is certain that many of the channels occupied by postglacial streams, when following their preglacial courses, 1The Berea Advertiser, April 16 and 30, 1886. CLEVELAND MORAINE. 619 vary remarkably in width. The amount of postglacial erosion may there- fore be much less than the size would indicate, a portion of the channel having never been filled. SECTION IV. MORAINES OF THE ERIE LOBE. CLEVELAND MORAINE. The Cleveland moraine is the next one later than the Defiance. As a land-laid moraine it appears to be developed no farther west in Ohio than the southwestern part of the city of Cleveland, but its continuation as a water-laid moraine may be traced at points west from Cleveland. Possi- bly it will be found near a line recently suggested by Taylor, a short distance back from the shore of Lake Erie from Cleveland to Toledo, and thence northward into Michigan; it would then perhaps be more appropri- ately termed the Toledo moraine, a name suggested by Taylor.’ Neither Taylor nor the writer has, however, found conclusive evidence of a moraine along the portion of the line between Cleveland and Toledo, nor for some distance north from Toledo. This being the case, it seems preferable to withhold the name Toledo and apply the name Cleveland, the latter being a prominent city at the southwestern end of the well-defined land-laid por- tion. This land-laid portion has occasionally been called the Newburg moraine, from the part of Cleveland in which it is found, but it seems pref- erable to substitute the name of the well-known city rather than to adopt the name of one of its suburbs. DISTRIBUTION. The westernmost point at which this moraine has been recognized is on the west bluff of Big Creek, opposite North Linndale, near the south- western limits of the city of Cleveland. To the south, west, and north of this place there is a very level surface, on which no morainic features were detected. From North Linndale the course of the moraine is nearly due east along the south side of Big Creek to its junction with the Cuya- hoga in the southeast part of Cleveland. Upon crossing the Cuyahoga into the part of the city known as Newburg, the moraine, as indicated in Pl. XIII, continues eastward through Randall to the valley of Chagrin River below Chagrin Falls. From this valley the moraine swings abruptly 1Bull. Geol. Soc. America, Vol. VIII, 1897, pp. 34, 39; Jour. Geol., Vol. V, 1897, p. 454; Am. Geologist, Vol. XXIV, 1899, p. 15. 620 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. northward, passing through Chester Crossroads to the Hast Chagrin River in the southwest part of Chardon Township. It there swings eastward and passes just north of the village of Chardon to Hampden Center, and thence to the headwaters of the Cuyahoga River in northeastern Geauga County, Ohio. The moraine then makes a detour to the south in crossing the Grand River Basin. For about 10 miles from the head of the Cuyahoga the course is southward along the divide between the Cuyahoga and Grand rivers. It then swings to the southeast and constitutes a portion of the divide between the Grand and Mahoning rivers, passing through Southine- ton and Champion townships, Trumbull County, and coming to Mosquito Creek 2 or 8 miles south of Cortland. It there turns abruptly northward and crosses over the divide between Mosquito and Pymatuning creeks. It first touches the Pymatuning Valley near the line of Trumbull and Ashta- bula counties, and follows the western slope of that valley to the Ohio- Erie divide, about 4 miles northwest of Andover, Ohio. The small glacial tongue encireled by this loop extended but little outside the drainage basin of Grand River. It has a width of about 15 miles at the south end, and perhaps 25 miles at the north, where it became confluent with the main body of the ice sheet. From the Grand River Basin eastward there is a much more complex morainic belt than to the west, and possibly more time was occupied in its formation than in that of the Cleveland moraine. Between Pymatuning Creek and the Ohio-Pennsylvania line there are three somewhat distinct ridges or members, each from 1 to 2 miles wide. The southernmost passes in an eastward course through West Williamsfield and Williamsfield Center, and after crossing the State line enters the Shenango Valley near the north edge of Jamestown, Pa. The middle member leaves Pymatuning Creek 3 or 4 miles farther north than the southern one, and, bearing south of east across southwestern Andover and northeastern Williamsfield townships, becomes merged with the southern member just east of the State line. The northern member passes from the head of Pymatuning Creek north of east across Leon Township, entering Pennsylvania near Pennline, at the northwest end of Pymatuning Swamp. ‘ No well-defined continuation of the southern and middle members was found on the uplands east of the Shenango, between that stream and ce i cel IES RE ES EA Ce ee CLEVELAND MORAINE. 621 Crooked Creek, and nowhere east from it are more than two members developed. Drift knolls abound opposite Hartstown, on the east side of Crooked Creek, near the head of the stream. They apparently correspond in age to those in the Shenango Valley at Jamestown. There is a nearly continuous line of knolls from Hartstown northwest to Pennline, along the east side of Pymatuning Swamp, at a right angle to the general trend of the moraine and in about the same direction that the ice moved. It is probably a con- necting link between the southern and northern members of the morainie system. At the time the earliest member of this series was forming the ice sheet apparently stood at Hartstown, on the valley of Crooked Creek; at Jamestown, on the Shenango, and near the line of Ashtabula and Trumbull counties, Ohio, on the Pymatuning. These points mark the southern border of the features in these valleys. At the time the latest member was forming the ice sheet apparently stood at the head of Pymatuning Creek, in eastern Ohio, and at the northwest end of Pymatuning Swamp, in western Penn- sylvania, and the knolls along this swamp appear to have been formed in connection with the retreat of the ice sheet from Hartstown to Pennline, i. e., from the southeast to the northwest end of the swamp. The upland between the Pymatuning Swamp and the valley in which Conneaut Creek and Conneaut Lake are situated has scarcely any drift knolls worthy of note, but along the Conneaut Valley there is a line of drift knolls about as long as that on the Pymatuning Swamp, 10 to 12 miles. The southern end is east of Conneaut Lake, and the northern end near Conneautville, Pa. The formation of this line apparently occupied an interval of time similar to that between the formation of the southern and northern members of the moraine in the valleys west from here, the south- ern end having been deposited when the ice stood at Hartstown and James- town, Pa., and the northern when it stood at Pennline, Pa. On the uplands between the Conneaut Valley and the Cussewago, two feeble moraines were observed, one passing from the southern end of Conneaut Lake north of east into the Cussewago Valley, at the bend 3 or 4 miles west of Meadville, the other passing from near Conneautville to the Cussewago Valley at Crossingville. The Cussewago Valley has drift knolls along its eastern side throughout the interval between Crossingville and tlie bend of the creek, while the western slope is nearly free from drift knolls. 622 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Between Cussewago and French Creek valleys drift knolls occur, both isolated and in groups, but not forming well-defined belts. In French Creek Valley drift knolls set in near Saegerstown and occupy it as far as the bend west of Cambridge, a distance of 7 or 8 miles. These probably represent only the outer member, for French Creek has here a northeast-to- southwest course corresponding with the general direction of the ice margin- The inner member is apparently represented on Conneautee Creek, a few miles north of Cambridge, near McLane, and on Le Boeuf Creek at Water- ford, there being strongly morainic topography in the valleys at these villages, and a well-defined moraine-headed terrace at Waterford. The two members of this morainic belt are more distinctly outlined east from here than they are to the west, and are accordingly traced separately. The outer member follows the southeast side of French Creek from Cambridge to Le Boeuf and then passes up Kast French Creek and rises to the uplands. It passes 2 or 3 miles north of Beaver Dam, and enters New York at the extreme southwest corner of the State. In New York it has a northeastward course for several miles, crossing the Western New York and Pennsylvania Railway north of Panama station, and rising onto the uplands between the head of French Creek and Lake Chautauqua, where it attains an altitude about 1,800 feet above tide. The moraine is not well developed on the slope toward Lake Chautauqua, but seems to find its continuation in a sharp cluster of knolls at Jamestown, N. Y., at the south- east end of the lake. The inner member passes from Waterford, Pa., northeast into New York, crossing the valley of Lake Pleasant at and above the lake, and the north branch of French Creek north of Lowville, Pa., and in western New York it again crosses this creek near its head at Findley Lake. From the north end of Findley Lake its course is slightly north of east past Sherman, N. Y., to the narrows of Lake Chautauqua. There are occasional developments of morainic topography between these two belts, so that in some of the valleys of Erie County, Pa., and Chautauqua County, N. Y., they are nearly connected, but on the uplands they are distinctly separate moraines. Some uncertainty is felt concerning the position of the ice margin for a distance 30 miles east from Lake Chautauqua at the time the Cleveland morainic belt was forming. It is a much more broken region than that CLEVELAND MORAINE. 623 west of Lake Chautauqua, there being a difference of more than 700 feet in the altitude of ridges and valleys. The altitude of the high points on a dividing ridge between Cassadaga and Conewango creeks, in northwestern Gerry, eastern Charlotte, and western Cherry Creek townships, in Chau- tauqua County, is 2,040 to 2,100 feet, as shown by the Cherry Creek topographic sheet, while the broad valleys of Cassadaga Creek on the west and of Conewango Creek on the east of this elevated strip are below the 1,300-foot contour. As both of these valleys are open to the north, the ice sheet was free to extend into them from the Lake Erie Basin. There is a strong probability that it extended down Cassadaga Valley to the mouth of the creek and down Conewango Valley to the vicinity of Kennedy; but it probably fell short several miles of reaching as far south on the inter- vening uplands and also on the high uplands between Cassadaga Valley and Lake Chautauqua. The entire valley of Cassadaga Creek and the part of Conewango Creek above Kennedy have broad bottoms standing only a few feet above the creek beds, portions of which are still subject to overflow. Along the borders of each of these valleys, and also on the borders of the valley in which Lake Chautauqua lies, there are accumulations of gravelly, partially assorted drift which rise 40 to 75 feet above the broad bottoms. They are slightly undulatory and in places carry shallow basins. The topography, structure, and position of these deposits seem best explained on the hypo- thesis that the valleys were filled by tongues of ice at the time they were accumulating. The hypothesis that these benches are remnants of a filling which once extended entirely across the valleys was considered and found to be untenable, for such an erosion as it would call for is greatly out of proportion to the erosion farther down these drainage lines. The hypothesis that the benches represent the borders of a lake was also considered and found to be unsatisfactory. The deposits are evidently to a large extent glacial. The water action which they display seems to be such as might occur in connection with drainage along the border of ice tongues, and not such as would occur on the shore of a narrow lake. The basins and the low swells on these benches give them a striking resemblance to the head of glacial terraces. An examination of the part of the Conewango below Kennedy shows the valley to be occupied by a pitted gravel plain which stands at about the same height as these benches. This pitted gravel 624 GLACIAL EORMATIONS OF ERIE AND OHIO BASINS. plain leads past the southern end of Cassadaga Valley and connects with a valley that leads down the Lake Chautauqua outlet from the moraine at Jamestown. Concerning the position of the ice margin on the intervening uplands, but little has been ascertained. On the divide between Lake Chautauqua and Cassadaga Creek the drift surface is generally free from knolls. East of Cassadaga Creek there are notable drift accumulations in Mill Creek Valley, from its mouth near Sinclairville up nearly to its source, a distance of 5 or 6 miles. This constitutes apparently a natural line of continuation for the inner member, which was traced to the narrows of Lake Chautauqua, There seems to be no moraine on the high divide to the east of Mill Creek, but east of the divide along Farrington Hollow for about 3 miles northwest from Cherry Creek village, there are conspicuous drift knolls. The lower course of West Conewango Creek, near Hamlet, is also choked by drift knolls. Those in Farrington Hollow may constitute the line of continuation of the inner member. On the east side of the main Cone- wango Valley, drift knolls are conspicuous on the lower course of Dry Brook, near Rutledge. They are also numerous north of Leon, where they have filled an old valley which may have been the former line of discharge for Mad Creek. But aside from these two places there are few knolls along this side of the Conewango Valley. At the head of the Conewango Valley there is a well-defined moraine, but it belongs to a later morainic system than that under discussion. Between Conewango Creek and the South Fork of Cattaraugus Creek there is a high upland, with an altitude 1,900 to 2,000 feet or more, and on this upland drift knolls are comparatively rare. But a well-defined moraine sets in near Maples post-office, about 6 miles east of Cattaraugus village, which seems likely to be the continuation of the Cleveland morainic belt, for it lies a short distance outside the morainie system which farther west is known to be the next one younger than the Cleveland belt. Its general course is indicated on the glacial map, Pl. I, but a more definite outline will be here presented. From Maples northeastward to the meridian of Machias, a distance of nearly 20 miles, this moraine lies near to and in places constitutes the divide between southern tributaries of Cattaraugus Creek and the headwaters of Great Valley and Ischua creeks, which discharge to the Allegheny River. —— CLEVELAND MORAINE. 625 It passes about 3 miles south of the village of Ashford Hollow, 1 to 2 miles south of the village of West Valley, and 2 to 3 miles north of Machias. From near the head of Ischua Creek, about 4 miles southwest of Machias, another moraine leads eastward, passing just south of Machias, and continuing about 3 miles beyond that village. It there becomes obscure, but seems to be continued in a belt that sets in 4 or 5 miles farther east, near Fairview, and leads southeastward past Rushford to the Genesee Valley at Caneadea. Whether this moraine is a member of the same system as that to which the Cleveland belongs is not determined. It may be a correlative of an earlier moraine, but its close association with the supposed Cleveland moraine in the few miles in which it is well developed seems to justify its consideration in connection with that moraine. From Machias eastward to the Genesee the two moraines are separated by a space of but 4 to 8 miles. Returning to the meridian of Machias, we find that the northern or supposed Cleveland moraine takes an eastward course to Clear Creek (a southern tributary of Cattaraugus Creek) at Sandusky. It there swings northeastward and rises to the elevated divide between the head of Catta- raugus Creek and Wiscoy Creek, a western tributary of Genesee River. On this divide it turns southeastward, but extends a spur northward along the divide to the next morainic system. The village of Eagle stands near the outer border of the moraine at the place where it turns to the southeast. The moraine is strong for about 3 miles east of Eagle. It is then poorly defined for a couple of miles. It becomes strong again in Cold Creek Valley, in northeastern Centerville Township, and leads down the south side of that valley to the Genesee, coming to that river between the villages of Houghton and Fillmore. RANGE IN ALTITUDE. The course of the Cleveland morainic belt bemg across a hilly region, there are frequent fluctuations in altitude. In many cases the moraine makes a rise of 200 to 300 feet within a space of 1 to 2 miles, and occasionally an even greater rise in an equally short distance. The following table presents the principal fluctuations. MON XLI——40 626 GLACIAL FORMATIONS. OF ERIE AND OHIO BASINS. Table showing range in altitude of the Cleveland moraine. : Feet above tide. Wiesternarennatnt sm eaieN Or tlie lel © ees ee eae a 800-825 NeariRand alll Obi geese ce aietetyee ae sce Me ohm ones ie fee Cs Me ene ee RO 1, 000-1, 050 Chagrin g Valle yr saan Soe SE ERR care = SASS pao a Sa Eee ee 900-950 Near Chard one seston eset ee cet eee Nee ee oe Ne Ac ee Ee ee ae 1, 100-1, 200 Jaticdnlenarelet yest On Catnacl IRGr a6 sae ssasaaeassnasdusacacoases saconcesbccces-enesssose 1, 200-1, 325 GrandiRiversVialleysesssenssojees nuke a otal e aaa eee 1 ae a ee 915-940 Divide between Mosquito and Pymatuning creeks ...-....-.2..----2.------------------ 1, 100-1, 150 eymatumin oeValll yess 2 le yale eee ae ye 8S ake Us oes a See cer bee ee a eee eee 940-1, 000 ide Detweeny ey marin oa dys ea 2 Ope a aes ses a eee 1, 075-1, 191 Andover geodetic:statiomtns: 222 ss saa 5. Feo Oks ae aes Be ee i a eee il, ight Shenango) Valley trom Jamestown to State Mine ——--—- = 7-225 = eon see ee 972-1, 020 JEVAME MIO MSN NODS oot ose a dene oo Boba dem ocerenue pas sanodaac sR So ee ee 1, 020-1, 050 Divide between Pymatuning Swamp and Conneaut Valley -...-...-----..----..--.----- 1, 100-1, 225 Wonmeam titalce wee sa yete te hse Oe oie Ph 1 oes 1M se ae epee 1, 082 Mivid eynorthyotmalre se. Rene) sees, ote CE we ee cs Oe elec a ea 1, 100 Wicksonib ung ase s eee tee an ae ak ie ee aed a) epee eee es 995 Connesgutwilll eres Beaten seeis aioe See eee ace 8 fae Saas ce aCe es oe ee ee 920 Highlands between Conneaut and Cussewago valleys..-...--.---.---...--------------- 1, 175-1, 450 @ussewarouVialll eyed eee ans cme sae ceek ete ois Meni apnoea eee en 1, 075-1, 150 GCirashke eG! @oG SMe lees! (Woe) 25 coe cacec coos sce esessesseScoussecannaccsenssasue 1, 095. Highlands between Cussewago and French creeks......------------------------------- 1, 300-1, 500 Morainejat| Conmesutees Valleys. cesses — mae so. 6 soe eee ee ene eee aes 1, 275 Ridge between Conneautee and Le Boeuf valleys. _...-..-..-.....--.-+.--:----!--..-.. 1, 400 Moraine at Le Boeut Valley (Waterford station) --......-.-----..-..--.2.------------- 1, 193° Eughlandsimearsouthwesticomenot New York 5-2. 2.2- ss.5 2225 /2e= shee eee esse eee ee 1, 700 Walle yaneary Panama, station: se) 2 4)=\-i2)c\-c)2\iainin slo =) -)efsic wee elma eee eee ee meets 1, 550. JEbielnlenals Wrest OH Wellies CloeiinRNOG IE) - 6 5 ogeeboe oder see soso cmecmoscssesceseseceecone 1, 800 Whale! Chautauquaksoscs see Mc heas 1g 2 i \3 = \ 8 eRe 1) 2) F Wes |e 1 13 H| OP Ik 5 x Al "os 6.4 Mua oO © 4 os © A =| me as (a) z W oO Ww ai Ss 2 ] 0 3 n z ee re Pee eI \é 3 WWE 2 ¢ o a is ; A WW oO q L 4 le} Zz | —? JULIUS BIEN & CO LITH NY Roads Se i ile _ = 4 U.S. GEOLOGICAL SURVEY = = ss —e ¥ 7 e MONOGRAPH XLI PL_XVIII PLEISTOCENE MAP “OF PART OF THE GIRARD AND ERIE » PENNSYLVANIA QUADRANGLES By FrankLeverett Scale 2 4 5 Miles = sai s: =| Ye 1 4 5 Kilometers =r ——=t Contour interval 100 ft, 1900 LEGEND ered LakeWhitllesey Moraines i Non-morainic drift Lake Warren Line of glacial drainage Beaches discharging westwat Lake Maumee SLL Roads ‘ Recent alluvium UUUUS BIEN SCO. LITH NY bax oe ey ie gee bec tate fmt a =) } Te " Diath ¢ H i oo Pi sh mm e / AN ea! ava a “ih aera ie Niet I 1 F ts iit ni . } ih , a a i . Y 7. t ay hued ( b f v7 ¥ aif 1 % ih . ‘ v 3 " pit 4 i 3 i, ‘ j “ ; he Ke * . b i , ‘ . } “? . " f =f 2 D LAKE ESCARPMENT MORAINES. 653 miles distant on the north. From the bend of Ashtabula Creek at East Plymouth the Painesville moraine follows up the south side of the creek to Kelloggsville, where it crosses to the north side. The Euclid moraine lies a short distance south, near the base of the rock escarpment. East from Kellogesville, the valley of Ashtabula Creek lies between the two moraines to their junction at the head of the creek. A third ridge sets in at Ashtabula, causing the great oxbow bend of Ashtabula Creek, and leads eastward through Kingsville, where it crosses Conneaut Creek, and continues into Pennsylvania along the north side of that stream. It is separated from the Painesville moraine only by the valley of Conneaut Creek. The course of each of the moraines of this system in western Erie County, Pa., is shown in Pl. XVIII. The Euclid and Painesville moraines become united at the head of Ashtabula Creek, about 6 miles east of the State line, and the united moraine crosses Conneaut Creek 1 to 2 miles north of Albion, just south of the great bend of the creek. From Conneaut Creek it follows the base of the escarpment northeastward to Elk Creek at Sterrettania, crossing Little Elk Creek near its mouth. Upon passing to the north side of Elk Creek near Sterrettania it becomes difficult in places to separate this moraine from the Ashtabula moraine, but generally a narrow sag or valley lies between the two. Mill Creek and Walnut Creek each occupy this sag for a few miles. The Ashtabula moraine follows the north bluff of Conneaut Creek eastward to the great bend at Lexington. It there turns northeastward, passing just west of the village of Lockport (Platea station), and crosses to Elk Creek 1 to 2 miles above Girard. Upon crossing Elk Creek it turns eastward and, as above noted, is separated from the Painesville moraine by only a narrow valley-like depression. This depression apparently furnished a line of westward escape for glacial waters. The fourth, or Girard, moraine is well defmed and distinct from moraines outside of it for only a few miles in western Erie County, Pa. The western end is immediately north of Girard; but it may perhaps continue as a low water-laid moraine westward along Elk Creek to the shore of Lake Erie. The contours of the topographic sheet have suggested such a continuation. Between Cross station and Girard a range of knolls and ridges 654 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. appears which is somewhat distinct from the Ashtabula moraine. It lies mainly north of the Girard and Lexington wagon road and occupies a width of scarcely one-half mile. On the outer (south) border there is a narrow gravel plain that appears to be an outwash from the moraine. This was at first thought to be a probable continuation of the Girard moraine, but an inspection of Pl. XVIII will make clear that it fits in better with the Ashtabula moraine. From Girard eastward to Swanville the Girard moraine consists of a narrow, nearly continuous till ridge, having only a few knolls associated with it. It hes north of the Girard and Erie wagon road most of the way to Fairview and south of that road from Fairview to Walnut Creek Valley, opposite Swanville. Upon crossing Walnut Creek it becomes much stronger and remains conspicuous to its junction with the morainic belt outside of it near West Mill Creek station. From the vicinity of Erie, Pa., eastward to the north end of Lake Chau- tauqua, in New York, there is a single prominent moraine | to 3 miles in width. It follows the north side of Walnut Creek about to the meridian of Erie, and there crosses Mill Creek and follows its north side past Belle Valley, its inner border extending down to the south edge of the city of Erie. It crosses Sixmile Creek south of the village of Harbourcreek, and Sixteenmile Creek just below (west of) Grahamville. It enters New York at the bend of T'wentymile Creek and follows the north side of the west- flowing portion of that creek across Ripley Township to its source in western Westfield Township, Chautauqua County, N. Y. It comes to Chautauqua Creek 3 miles south of Westfield, and nearly opposite the mouth of Little Chautauqua Creek. Throughout much of the distance from Krie to Westfield its inner border is within 1 to 2 miles south of the railway lines, and for a short distance between Northeast, Pa., and the New York line it extends slightly north of the railways. The inner border is on the whole less definite and regular than the outer, and knolls and ridges occur sparingly for a mile or two north of the main belt. An instance is found at Northeast, Pa., where there is a series of knolls and short ridges 10 to 20 feet high, standing nearly 2 miles north of the main moraine. These and other similar short ridges along the inner border of the main belt seem scarcely prominent enough to merit separate name and description. The course of this morainic system from Lake Chautauqua to Cat- \ 7 ; ee t+ Wee, Be] —AasapTYMEYeT — SeyOwag —-aBeureMP TEND YUpparepns-oneyd AMER, IFIP OnuTeOYy SS fy QON3931 OO61 1249) Das upeU S77 Joes OOLIPAAOjUr an0}U0H SUuaLaMOIM Ss © TZ Se sau > DCAM AAT MNVU AG MHOA MAN ‘SATONVUGVAO MAGHO UAATIS UNV MAWHO AVA MYIMNOG HO Luvd JO daVW ANSAOO.LSIATA XIX 1d 11X HdVYUDONOW ASZAYUNS 1VW91901049 SN JULIUS BIEN 8 CO.LITH NY LF. v Van Buren U.S.GEOLOGICAL SURVEY PLEISTOCENE MAP OF PART OF DUNKIRK, CHERRY CREEK AND SILVER CREEK QUADRANGLES, NEW YORK BY FRANK LEVERETT Scale o x = ° 4 icce = S rn = > = 3 HILOMETERS Contour intervall00 feet Datum is mean sea level. Es LEGEND a ese Morainie drift Mainly plane-surfaceddrift Glacialdrainage § Beaches LakeWhitllesey Lake Warren Alluvial jit Roads a . LAKE ESCARPMENT MORAINES. 655 taraugus Creek is shown in Pl. XIX. In the valley-like depression at the north end of Lake Chautauqua two distinct moraines are found. An outer weak one extends from Little Chautauqua Creek southeastward to within 2 miles of the head of Lake Chautauqua, and there turns abruptly northward along the west side of Inlet Creek and joins the main belt east of Prospect. The main belt leads northeastward along the north side of Little Chautau- qua Creek to its source, and there becoming united with the outer belt, continues through the south part of Portland Township to the valley-like depression in which Bear Lake stands, where it again separates from the outer belt. The outer belt, which here also is weak, leads eastward to Bear Lake, and then returns northward to join the inner or main belt on the high divide between Bear Lake Valley and Cassadaga Creek. -The inner belt leads directly northeast across Bear Lake Valley, passing about a mile north of the lake. The united belt swings around the north end of the high divide between Bear Lake and Cassadaga Creek, and takes a south- ward course into the Cassadaga Valley at Upper Cassadaga Lake. From Cassadaga Valley two moraines lead eastward. A weak outer one passes from Cassadaga Village northeastward to Arkwright, while a strong inner one leads from Upper Cassadaga Lake to the same point, a portion of its course being along the north side of the westward-flowing part of Canadaway Creek. The combined belt leads eastward from Arkwright past Arkwright Summit to the valley or depression in which West Mud Lake lies, and includes that lake in its outer border. It then makes an abrupt northward turn along the face of the hills east of West Mud Lake, and crosses over to the valley-like depression in which Kast Mud Lake lies. In this depres- sion there was less lobation of the ice margin than in similar valleys to the west, the course of the moraine being eastward across the valley and the uplands east of it to Slab Creek, a headwater tributary of the Conewango, and thence over another ridge south of Perrysburg to the broad valley of the Conewango, which afforded the old line of discharge for the Upper Allegheny. In crossing this valley the moraine takes a northeastward course through Dayton to South Cattaraugus Creek, coming to that stream about midway between Gowanda and Cattaraugus. It is very ill defined east of this creek for 3 or 4 miles, but seems to follow the east bluff northward nearly to the 656 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. main Cattaraugus Creek. From that pomt a weak outer belt makes a detour southward in crossing the old valley of South Cattaraugus Creek and returns northward along the east side of the valley to the main Catta- raugus Creek. A stronger belt sets in on the north side of Cattaraugus Creek opposite the old valley and thence leads northeastward along the divide between northern tributaries of Cattaraugus Creek and streams which flow directly toward Lake Erie. Indeed the moraine to a large degree constitutes the divide from this pot up to the head of Cattaraugus Creek, in western Wyoming County. At the head of Cattaraugus Creek there is a reentrant between the lobe that extended westward into the Lake Erie Basin and one that extended southward up the Genesee. Between these lobes an interlobate moraine was formed which occupies the high divide west of the Genesee and extends northward from Wethersfield and Java townships in southwestern Wyoming County to Bennington Township in the northwest corner of the county, a distance of about 15 miles. From the east side of this interlobate moraine a strong moraine leads southeastward to the Genesee River, having a width of 6 or 8 miles in Wethersfield, Gainesville, Pike, Castile, and Genesee Falls townships, Wyoming County, and coming to the river in the vicinity of Portage Falls. The writer has not traced its course beyond the Genesee, but it is supposed to be continued around the southern ends of the Finger lakes of western New York. For a short distance outside the ridged and hummocky part of this morainic system in eastern Erie County, Pa., and in Chautauqua County, N. Y., there are often large numbers of bowlders, which it is thought may have been deposited by the ice sheet at about the time the moraine was forming, the moraine being a submarginal and the bowlders a. strictly marginal deposit. The bowlders are very conspicuous just outside some of the reentrants in the moraine, suggesting that the ice border may have passed more directly over the ridges which stand in these reentrants than the border of the morainic ridges would indicate, and also have reached an ultitude somewhat higher. The bowlders are, however, conspicuous only for a mile or so beyond the morainic ridges, and to altitudes 100 to 150 feet above them. Eo LAKE ESCARPMENT MORAINES. 657 RANGE IN ALTITUDE. The outer or south border of this morainic system is, throughout much of its course, much higher than the inner border, because of its situation on the face of an escarpment. he difference is only about 100 feet in the Ohio portion, but in Erie County, Pa., it reaches 400 feet, and in Chautauqua County, N. Y., fully 600 feet. In Ohio the altitude of the entire system shows scarcely 200 feet variation, the lowest parts being about 775 feet above tide, and the highest scarcely 950 feet. Indeed, it lies mainly between the 800- and 900-foot contours. There is but little rise shown in crossing the Girard, Pa., quadrangle, but in the southwest part of the Erie quadrangle, north of Sterrettania, an altitude of 1,000 feet is reached, and 1,000 to 1,100 feet is maintained along the crest of the morainic belt in the central and eastern parts of the quad- rangle. Between the Erie quadrangle and the New York line the crest of the moraine rises to about 1,200 feet, and near the Westfield geodetic station reaches an altitude of 1,480 feet In the valley-like depression at the head of Lake Chautauqua the outer border of the moraine stands between 1,340 and 1,400 feet. On the divide between Chautauqua and Bear lakes it rises slightly above the 1,500-foot contour, but drops in the Bear Lake depression to 1,325 feet. Northeast of Bear Lake it again rises to about 1,500 feet, and then drops to about 1,310 feet in the Cassadaga Valley. Near Arkwright it makes a still greater rise, and appears on a hill north of the village that rises to the 1,740-foot contour. In the valley east of Arkwright, near West Mud Lake, the altitude falls to about 1,400 feet, some knolls being found between the 1,380- and 1,400- foot contours. On the uplands between Kast and West Mud lakes an altitude of 1,680 feet is reached. Around East Mud Lake morainic knolls appear down to the 1,340-foot contour, but the crest north of the lake is about 1,400 feet in its lowest part. Between East Mud Creek and Slab Creek Valley the moraine rises to the 1,560-foot contour, but drops 200 feet in Slab Creek Valley, its crest being just above the 1,360-foot contour. On the uplands between Slab Creek and the Conewango Valley it rises to about the 1,600-foot contour. In Conewango Valley the crest is not far from the 1,400-foot contour, but the outer face extends down to about 1,340 feet. It rises east of South Cattaraugus Creek to about 1,650 feet, 42 MON XLI 658 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. but drops to less than 1,400 feet on the borders of the main Cattaraugus Valley. In the portion which follows the divide north of Cattaraugus Creek the altitude ranges between 1,400 and 1,800 feet in crossing the sags and ridges, there being a variation similar to that in the portion between Lake Chautauqua and the Conewango Valley. As this district has not been covered by the topographic survey, only general statements can be made. Near the head of Cattaraugus Creek, in the interlobate belt, a still greater altitude is attained, some points being nearly 2,000 feet. Between the interlobate belt and the Genesee the moraine descends several hundred feet, the altitude in the vicinity of Portage Falls being between 1,150 and 1,350 feet. The original level of the crest of the moraine in the Genesee seems to have been fully 1,300 feet. From the data just given it seems probable that the ice sheet had greater thickness in the eastern portion of the Lake Erie Basin at the time it was forming this morainic system than in the central or western portions. This seems due to its having had at that time an axial movement westward into the Lake Erie Basin. The eastern portion, being nearer the center of dispersion, would naturally carry a thicker sheet of ice than the more remote western portion. It may not be possible to compute the thickness definitely, but a rude approximation may perhaps be reached by considermg the altitude and position of the moraine. The moraine-covered hill near Arkwright, 1,740 feet above tide, is but 3 miles distant from the base of the steep escarpment, which stands 900 feet lower, or only 840 feet, but 7 miles distant from the shore of Lake Erie at Dunkirk, where the altitude of the lake bed is less than 570 feet, and 24 miles distant from the axis or deepest part of the Lake Erie Basin, where the altitude is only 380 feet. Were the ice sheet no higher in the midst of the lake basin than this moraine-covered hill, its thickness opposite Arkwright and Dunkirk would have been nearly 1,400 feet. But it is probable that the ice margin rose considerably above this moraine-covered hill, and that there was a gradual ascent from the margin northward to the midst of the lake basin. The thickness of the ice sheet, probably reached fully 2,000 feet in the midst of the lake basin north of Dunkirk. If the ice sheet had had a similar thickness opposite the north end of the Grand River Basin, there should have been a decided oe LAKE ESCARPMENT MORAINES. 659 protrusion into the basin. But instead this morainic system passes the basin with scarcely a mile of southward deflection. It is strikingly in contrast with the Cleveland, or next earlier morainic belt, which has a loop extending southward 20 to 25 miles into the basin. It may be objected that the movement toward the border of the basin was comparatively weak, the main movement being along the axis. This objection is, however, only another way of stating that the ice sheet was too thin in this part of the lake basin to have a strong movement. It is doubtful if its thickness was half that of the portion in the eastern end of the basin. RELIEF. Along its outer border this morainic system usually shows a relief of 20 to 40 and occasionally 60 feet; but the country to the south rises rapidly and soon reaches an altitude much above the morainic crest. The relief is best shown where the moraine crosses valleys, such as the Cassadaga, Chautauqua, and Conewango, but it is in many places conspicuous along the face of the escarpment. Between the members of this morainic system there are valley-like sags, above which the ridges rise to heights of 20 to 40 feet or more, there being nearly as much relief as on the outer border of the system. The sags afford convenient lmes for streams to follow, and the peculiar winding courses and sharp deflections of the creeks on the south border of the Lake Erie Basin in northwestern Pennsylvania and northeastern Ohio are in large part due to the controlling influence of the sags. TOPOGRAPHY. This morainic system, like the earlier ones, presents considerable variation in topographic expression, ranging from a comparatively smooth ridge with only gentle undulations to intricate hummocky tracts inclosing basins that hold ponds and small lakes. Between these types is the well-defined ridge that carries sharp hummocks and has its surface indented with basins. ‘There is also some contrast between different moraines of this system, the Euclid moraine having, on the whole, less strength of expression than the other moraines. In the detailed discussion which follows, the Euclid is first considered, after which the other moraines follow in turn from the outer toward the inner part of the morainic system. 660 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. From Euclid eastward into Lake County there are only a few low swells and a very faint ridge to mark the position of the moraine, the largest swells being scarcely 10 feet in height. Near the southwest corner of Lake County a more distinct ridge appears, which presents a relief of 10 to 25 feet, and has swells 5 to 15 feet in height along its crest and on its slopes. There are also a few knolls scattered over the plain on the south border of the ridge. These features continue through to Chagrin River, a distance of 3 or 4 miles. East of Chagrin River, along the north side of East Chagrin River, there is a ridge 10 to 20 feet in height with a breadth of a mile or less. Its surface is very gently undulating, with swells but 5 to 10 feet in height. An old channel follows the south border of this ridge from the bend of Grand River south of Painesville westward to East Chagrin River, which seems to have been the line of discharge for glacial waters into Lake Maumee. In this channel, about 3 miles southwest of Painesville, there is an outlying ridge that trends northeast to southwest in harmony with the main ridge and rises nearly 50 feet above the level of the channel in which it stands. The portion of the Euclid moraine which lies along the south side of Grand River presents a series of loosely connected knolls and short ridges, 10 to 20 feet in height, covering a belt only one-half mile to a mile in width. There does not seem to be a definite basement ridge, such as appears in portions of the moraine to the east and west. From the Grand River Valley eastward into Pennsylvania the Euclid moraine consists of a faintly outlined ridge with a relief of but 10 to 20 feet, yet this is sufficient to hold Griggs Creek in a westward course along its outer border from source to mouth and to cause Mill Creek to turn west- ward into Grand River. In eastern Ashtabula County, Ohio, it causes a tributary of Ashtabula Creek to flow westward on its outer border, while in western Hrie County, Pa., it causes a tributary of Conneaut Creek to turn abruptly eastward. As above noted, this moraine has not been recog- nized farther east than the northward-flowing part of Conneaut Creek, in Erie County, Pa. Returning to Painesville and taking up the description of the Paines- ville moraine, we find a somewhat sharp ridge, 2U to 40 feet in height, and from a half mile or less to fully a mile in width. Its crest as well as slopes carries swells and sags, with oscillations of 10 to 25 feet or more. LAKE ESCARPMENT MORAINES. | 661 Throughout its course, from Painesville eastward into Pennsylvania, it displays much greater strength than the Euclid moraine. Its influence upon drainage is a notable feature, and one showing its almost perfect con- tinuity. Grand River is made to take a westward course for about 20 miles along its outer border from the bend near Austinburg to the bend at Painesville, thus greatly increasing its distance to Lake Erie. The head- water part of Ashtabula Creek, from its source westward to Kellogegsville, Ohio, also has its course determined by this morainic ridge, and is prevented from flowing directly north to Lake Erie. After combining with the Euclid moraine in western Erie County, Pa., there is but little change in the topography from that presented by the Painesville moraine west of the point of union. There is usually a well- defined crest and a sharply undulating surface, on which the knolls are 10 to 25 feet or more in height. The part of the moraine between Conneaut Creek and Elk Creek, as may be seen by reference to Pl. XVIII, holds small drainage lines between it and the base of the rock escarpment to the south, one line leading northeastward into Little Elk Creek, and the other southwestward into Temple Creek, a tributary of Conneaut Creek. Between these is another stream which finds a gap in the moraine through which it passes northward into Elk Creek. Little Elk Creek takes advant- age of a similar gap near its mouth; but an eastern tributary of Little Elk Creek is turned westward between this moraine and the base of the escarp- ment. Elk Creek owes its southwestward deflection of 3 or 4 miles, near Sterrettania, to the presence of this moraine on its north side. The Ashtabula moraine differs but little in strength and in topographic expression from the Painesville moraine. Its width is one-half mile to a mile or more, and its crest stands 30 to 60 feet or more above the bordering sag on the south and the plain on the north. The outer or south face is much more abrupt than the inner. It is sharply undulating, and where strongest it has knolls 20 to 40 feet in height. The weakest part is immediately west of Kingsville, where for a couple of miles it rises but little above the old lake bottom, and has perhaps been worn down to some extent by the waves. The portion along the north side of Conneaut Creek from Kingsville, Ohio, eastward to Lexington, Pa., is exceptionally strong, its height beng 40 to 60 feet above the creek bluff. Immediately east of Lexington it is interrupted by a narrow gap through which Crooked Creek 662 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. finds a passage, while at Kingsville it affords a wider gap for Conneaut Creek to turn north toward the lake. From Conneaut Creek to Elk Creek the moraine, though having a well-defined crest, carries gentler swells than in the neighboring portions to the west and the east. From Elk Creek eastward to its junction with the Painesville moraine it presents a series of sharp knolls distributed over the slopes and along the crest of a prominent basement ridge. Parts of the ridge stand 60 to 80 feet above the sag on the south, which is drained by Brandy Run. Along the south side of Walnut Creek from near Sterrettania up to Kearsarge there is an intricate assemblage of knolls and sags without so well defined a basement ridge as appears to the west, where the moraines are more distinct. The largest knolls are 30 to 40 feet in height and are rather sharp. A similar confused assemblage of knolls continues across the interval between Walnut Creek and Mill Creek to the point of connection with the Girard moraine at the bend of Mill Creek south of Erie. Walnut Creek owes its deflection from the base of the escarpment westward to Kearsarge to the presence of this morainic system between Kearsarge and Mill Creek. Otherwise the headwater portion would have continued north- ward to Mill Creek and thence through the midst of the city of Erie into the lake, as may be seen by reference to Plate X VIII. In the range of sharp knolls which leads from Cross Station toward Girard the highest points rise about. 70 feet above the Maumee beach on- the north slope, but are seldom as much as 30 feet higher than the gravel plaim on the south or outer face. In places the knolls barely reach the level of the gravel plain. In the western part of the Girard moraine there is a gently undu- lating ridge with swells only 10 to 12 feet high, and a relief of 15 to 20 feet above the plain on its outer or south border. This weak phase con- tinues to Walnut Creek Valley. at Swanville; but from Walnut Creek eastward to Mill Creek, a distance of 9 miles, this moraine is about as strong as and is similar in topography to the best developed parts of the — Painesville and Ashtabula moraines. It is fully a mile in average width and consists of a well-defined basement ridge on whose crest and slopes knolls 10 to 40 feet in height appear. The variations in the strength of the Girard moraine are clearly brought out in Pl. XVIII. LAKE ESCARPMENT MORAINES. 663 From the bend of Mill Creek south of Erie, Pa., eastward nearly to the north end of Lake Chautauqua, N. Y., this morainie system, as above noted, is combined into a single strong belt. Along its south border there is often a somewhat sharp ridge forming the crest line of the belt and . standing 20 to 30 feet or more above the immediate border. Where the moraine crosses Sixmile Creek there is a small tract of level land lying between it and the escarpment to the south. A similar low plain at Sixteen- mile Creek is traversed by the creek for a mile or more near Grahamsyille. In western Chautauqua County, N. Y., there is a similar narrow plain several miles in length which has been utilized by Twentymile Creek in its westward course. From this ridge northward down the face of the escarpment the drift knolls are distributed singly or in groups. They are often so closely ageregated as to give the face of the escarpment a hummocky appearance, but in places are scattermg. The lower part of the escarpment generally has fewer knolls than the upper part. From the New York line eastward to the Westfield geodetic station numerous shallow basins were found among low swells along or near the crest of the moraine. Such basins are less numerous, though not rare, im Erie County, Pa. The outer moraine in the depression at the head of Lake Chautauqua is a gently undulating till ridge, with swells scarcely 10 feet in height, among which there are numerous saucer-like depressions. At the south border it stands only 8 or 10 feet above a gravel plain that leads down to Lake Chautauqua, being near the 1,340-foot contour, but the crest in places reaches the 1,400-foot contour. It is not certain, however, that this relief of 60 feet is entirely due to drift accumulations; possibly the crest follows in part a rock ridge. The topography of the outer moraine in the Bear Lake Valley is somewhat different from that in the Chautauqua, there bemg only scattering knolls without a well-defined basement ridge. The outer of the two moraines which lead from the Cassadaga Valley toward Arkwright consists of a gently undulating till ridge which, for a couple of miles northeast from Cassadaga village, forms a divide between a southward-flowing and a westward-flowing tributary of Cassadaga Creek, as indicated in Pl. XIX. The inner or main moraine from the head of Lake Chautauqua eastward 664 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. presents topography similar to that toward the west, there being in places a narrow ridge scarcely an eighth mile in width and 30 to 40 feet or more in height forming the crest, while numerous hummocks and basins appear on its inner border for about a mile north from the crest. Such a sharp-crested ridge is a conspicuous feature for 2 or 3 miles in the part of the moraine immediately west and north of Bear Lake, as may be seen by reference to the Dunkirk topographic sheet (see Pl. XIX). Just outside this sharp moraine is a smooth gravel plain. On the slopes north and northwest from the upper Cassadaga Lake there are a few drift knolls 20 to 40 feet or more in height, among which are numerous small ones only 5 to 10 feet high. In Cassadaga Valley a gravelly tract occurs around the upper and lower lake, which carries a few low knolls and presents apparently a gradation from the moraine into a plain that sets in south of the lower lake. On the high ridge near Arkwright the moraine has a hummocky surface, with numerous knolls 10 to 15 feet and a few 20 or 25 feet in height. This topography extends down the slope eastward to West Mud Lake. The valley below West Mud Lake carries a smooth gravel plain, but near the lake it becomes full of basins, the largest of which is occupied by the lake. They extend up to the morame which forms the divide north | of the lake, and which presents a sharply ridged surface. North from the morainic crest sharp knolls occur for a mile or more. Many of the knolls are small, being only 10 to 15 feet in height and covering only an acre or two. There are basins among them that occupy only a few square rods, yet are several feet in depth. The hummocky topography leads eastward over the ridge to East Mud Lake, where the moraine presents features similar to those around West Mud Lake, there being a gradation from the gravel plain south of the lake through basins in and around it to the sharp-crested moraine that passes it on the north. The basins on the border of the lake are 8 to 10 feet deep and only a few acres in extent, but the lake itself occupies a basin nearly an eighth of a mile across. From East Mud Lake eastward to Perrysburg knolls 20 to 30 feet high are quite numerous and are arranged in chains with trend in line with the moraine, or nearly east to west. The tendency to an east-to-west ridging becomes still more conspicuous in the area extending from Perrysburg LAKE ESCARPMENT MORAINES. 665 southeastward into the Conewango Valley. The ridges are in some cases 30 to 40 feet high and a half mile or more in length. There are also numerous conical knolls 10 to 20 feet high, among which are shallow basins. At the south border of the moraine there is a gradual transition to a gravel plain that leads down to the Conewango Swamp, near South Dayton. A similar transition is found in Slab Creek Valley west of Perrysburg. This strong moraine, as above noted, dies out at the west bluff of South Cattaraugus Creek, about 5 miles south of Gowanda, there being only scat- tering drift knolls on the east side of that valley. But upon crossing over the ridge to the old valley, about 3 miles northeast, the moraine again appears, though its ridges and swells are of a more subdued type than in districts to the west. The swells are only 10 to 15 feet high and have very gentle slopes, while the crest is a barely perceptible ridge. On the north side of Cattaraugus Creek between the creek and Collins Center there is a topography similar to that in the Conewango Valley near Dayton. The ridges and knolls are 20 to 30 feet high and among them are sloughs and saucer-like depressions. ‘There is but little change in topog- raphy in passing northeastward over the high ridge north of Mortons Corners to Woodward Hollow (Wyandale post-office), though the knolls are sharper on the elevated tract than on the lower ground. Knolls 20 or 25 feet high may be seen distinctly for a distance of 2 miles, their slopes are so abrupt. Among the knolls are basins with abrupt rims instead of the saucer-like depressions noted near Collins Center. In the valley both north and south of Woodward Hollow there are sharp knolls, 10 to 25 feet or more in height, among which basins are inclosed, but the tendency to ridging is not so pronounced as to the west, The east slope of the valley also presents a hummocky surface through the entire width of the belt, which is here nearly 3 miles. _ Farther east, on the meridian of Springville and eastward past East Concord, the moraine grades on the south into a gravel plain which leads westward some distance down Cattaraugus Creek. Low gravelly swells appear at the junction of the plain with the moraine. There is considerable ervavel outwash along the moraine from Springville up to the head of Cat- taraugus Creek, setting in near the level of the crest of the moraine and sloping southward. North of the crest the moraine is in places lower than the gravel plain and yet carries sharp knolls and basins. The knolls extend 666 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. north along the valleys some distance farther than on the mtervening ridges, giving the appearance of spurs. They are perhaps the lines of subglacial drainage, many of the knolls being gravelly and a few having the form of eskers. The interlobate portion of this morainic system in western Wyoming County presents in its southern part a very sharp knob-and-basin topography, scarcely an acre of the surface being plane. The knolls rise usually but 20 to 30 feet above the basins, and there are many very small, sharp hammocks only 5 to 10 feet in height. Upon passing northward in the interlobate belt the knolls become more scattering and among them are areas of considerable extent which have a nearly plane surface. The knolls are, however, in some cases rather large, some of them being 40 to 50 feet in height. The portion of this morainie system between the interlobate tract and the Genesee River also presents a sharp knob-and-basin topography, with knolls 10 to 30 feet or more in height inclosing numerous small basins. There is some tendency to aggregation in belts that trend northwest to southeast in line with the trend of the system, but this tendency is scarcely so marked as in the district west of the interlobate tract. There are also strips a mile or so in width in the midst of this system in which knolls are rather rare. These suggest intermorainic tracts, but they are not continued far enough to cause a separation of the system into distinct moraines. — STRUCTURE OF THE DRIFT. In the gently undulating morainic ridges from Euclid, Ohio, eastward into Pennsylvania there is a clayey till similar to that found in the plains farther west, and but few gravel knolls occur. The coarse material becomes more conspicuous as the moraine rises along the escarpment in Hrie County, Pa., and Chautauqua County, N. Y., while on some of the high ridges farther east the stones are so abundant as to give the moraine a gravelly appearance. The outer belt in the valley-like depressions at the head of Lake Chautauqua and at Cassadaga and Bear lakes carries a more clayey till than the inner or main belt. There is also a very clayey till in the old Upper Allegheny or Conewango Valley and the old course of South Catta- raugus Creek. But from the crossing of Cattaraugus Creek near Collins Center eastward to the interlobate moraine the till is very stony and gravel LAKE ESCARPMENT MORAINES. 667 knolls abound. Gravel knolls are more conspicuous in the valley-like depressions than on the ridges, both in the district north from Cattaraugus Creek and that west from it in Chautauqua County, N. Y. The interlobate moraine carries a large number of gravel knolls, and the till knolls contain a large amount of coarse material. The depressions among the knolls have, on the whole, a coarser drift than is usually found in the portion west of the interlobate, where a compact till predominates. The portion of this morainic system between the interlobe and the Genesee River has about the same structure as the interlobe, there being a large number of gravel knolls and a rather stony drift in the till knolls. Surface bowlders are common all along the morainie system, but are especially abundant in the New York portion. They are largely granitic rocks, though in many places Canadian crystallines are represented. Parts of this morainic system have been classed with the beaches by early writers. This confusion appears to have arisen mainly from the imperfect knowledge of the phases of structure which a moraine may pre- sent, especially the stony phase, though in one of the instances above cited a ridge of clayey till is called a beach. In Read’s “Profile section from Lake Erie to Grand River,”’ the southernmost of the four ridges there shown is the Painesville moraine and is described as a riage of bowlder clay. The beaches are narrow ridges only a few rods wide, while the moraine has a width of one-half mile or more. The beaches are composed of assorted material, the moraine of till, with occasional developments of gravelly knolls In places in Ashtabula County the moraine and beach are so closely associated that beach sand appears on the ‘moraine, but through much of its course in Ashtabula County, as well as elsewhere, the moraine is free from beach deposits and from evidences of wave action. The following description by Read, taken from the report on Ashtabula County,? will make it evident that a glacial ridge rather than beach is described: The old ‘‘lake ridges” and terraces are well defined in the county, and railroad excavations have afforded unusual facilities for studying their character. The outer or southern ridge, where exposed by railroad cuts, is shown to be a ridge or wall of compact unstratified clay, composed largely of the local rocks, but with many frag- 1T. C. White: Second Geol. Survey Pennsylvania, Rept. Q*, pp. 38,39. M. C. Read: Geology of Ohio, Vol. I, 1873, pp. 488-490, 516-518; Vol. II, 1875, pp. 60-63. 2 Geology of Ohio, Vol. I, p. 518. 3 Geology of Ohio, Vol. I, p. 488. 668 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. ments of granite and other metamorphic rocks, not rounded by the action of wayes but in irregular forms, ground, polished, and marked with strie and scratches on all sides. On page 489 the following section is presented by Read, and with it a few remarks on the drift clays of the Painesville moraine, exposed on the bluff of Ashtabula Creek: Section of the Painesville moraine at the bluff of Ashtabula Creek. Feet. ysan dy sloamrss sae vei s Soe shah 2 em acina saeinneie Se = aaa taleiale eee ete eee a eee ee eee epee 1-2 2, Veallony Gly, waka tacyenmners) Oi (NEN Ae one eco oe cep soebo se Se ceocos coos esos ac ohesseacce 10 3. Blue clay, with fragments of shale’and bowlders. _------- ~~~ <= 2-222 oo oon 14 A Rimeysand: local on castes Se ein cists smo eoe ee seater ssc ieee SoS c ea RES eae ee ee ete 0-3 bs Coarse sravel, coarsestiat botbomd . <2 52-22 sani = joisiewin cise oe se ee eee Ee EEE eeeee 10 GaeB lnevclay-wathybowdders=se—- posse cee ace nee see sea eee eee eee ee eee ae 50 7. Erie shale in place. The yellow and blue clays are wholly unstratified, composed of the débris of the Erie shales, with numerous fragments of granite rocks. The coarse gravel in the middle of the section is of similar fragments, with the clay washed out of it. The mass bears no resemblance to the shingle of a water-washed beach, the gravel not being polished and rounded into pebbles, but apparently the result of a mass of mud ‘pushed up into a position where drainage has carried off the softer and more liquid materials. The local bed of sand (4 above) is stratified, indicating a temporary local space of open water apparently soon closed up, and the ice pushing the unstratified clay above it. This ridge with its mass unstratified and without rounded, water-worn pebbles, can not be the slow accumulations ot a water-washed beach, nor can the materials have been deposited in any way which permitted them to fall through water which would sort and stratify them. In Read’s descriptions of the ‘‘south ridge” in Lake County, the upper beach line and the moraine are not clearly distinguished. The “south ridge” in Willoughby Township is the Euclid moraine, and in the eastern part of Lake County is the Painesville moraine, but what is termed the south ridge at Painesville is the Belmore beach. It is remarked concerning the moraine in Willoughby Township that “the southern lake ridge here, and in a large part of the county, is mostly composed of unstratified clays, but is irregular and not well defined.” Concerning the Belmore beach at Painesville, the following remarks and section are presented :* At Painesville the south ridge is in places largely composed of coarse, stratified gravel, but it has been modified by subsequent action. The following isa section from ‘Geology of Ohio, Vol. I, 1873, pp. 516-517. LAKE ESCARPMENT MORAINES. 669 a cut made by the Painesville and Youngstown Railroad on the north bank of the river: Section of Belmore beach south of Painesville. Feet Coarserrave Sanath out, distimGin tec clita oye see ees ee eee en ee een 12 MIC RSA Cie Ck OT AVE merase teers an IA Scr a oe eS Sean ee Ss Sate a ee ne eee eee 4 Coarse gravel obliquely stratified, changing below to fine grayel with irregular waved lines of S ULeL bit CaUL OM Mires py tele eter ierdlal ai AiS ia a a laictehe oh cee St SR hk od Se Ad me ai ie RO eR 6-12 In the above section the upper 16 feet constitutes the beach proper. The lower part of the section is an earlier formation of glacial age. The gravel is cemented with lime and contains much calcareous sand and rock flour produced by glacial grinding. The obliquely stratified gravel lies below the level of the base of the inner slope of the beach, and is probably no more closely related to the beach gravels above it than is the till which so often underlies beach gravels, the beach gravels in both cases being produced at a later period by the waves of the lake, while the underlying gravels or the till were produced by glacial agencies. The following description of the moraine east of Painesville is given by Read:* The bluff of the river is 250 feet above the lake. An irregular clay ridge, half a mile north of the bluff and about 5 miles from the lake, is here the most southern well-defined lake beach. It is 260 feet above the lake, and composed of bowlder clay, with a surface somewhat irregular from the effects of erosion, but gently sloping to the sandy ridge on which Madison village stands, the surface generally becoming sandy as this ridge is approached. Thus it appears from the descriptions that the ‘‘south ridge” when a moraine is composed of bowlder clay, and when a beach, of sand and eravel. It is, however, but fair to call attention to the fact that Read appears to have held at one time the view that the till ridge is a moraine, even though in his description he calls it a lake ridge. Newberry states? that Read had regarded this ridge as a moraine, but that he (Newberry) cousidered it a clay terrace which had been cut by the lake. The chief geologist of the Ohio survey thus appears to have been influential in turn- ing his subordinate from a correct to an erroneous interpretation. OUTER BORDER DRAINAGE. The lines of escape of glacial waters on the outer border of this morainic system are very plainly indicated along much of the border. 1Geology of Ohio, Vol. I, 1873, p. 518. *Thid., Vol. II, 1875, pp. 60-61. 670 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. From the Conneaut Valley, in western Pennsylvania, westward to the terminus of the moranic system near Euclid, Ohio, there are well-defined channels between it and the rock escarpment, one of which is outside the Euclid moraine and others between the moraines. ‘These channels are still utilized in large part by small westward-flowimg streams which after following the line of glacial discharge for a few miles now turn northward through gaps in the moraines. Between these streams there are short sec- tions of the glacial channel not utilized by the present drainage. Perhaps the most conspicuous abandoned part leads from the bend of the Grand River south of Painesville westward to East Chagrin River near Kirtland, and this has a length of but 5 or 6 miles. The interval between Ashtabula Creek, south of Kellogsville, and the head of Griggs Creek is scarcely 2 miles, and there is a similar interval between Chagrin River and Euclid Creek. In each of these places there is a well-defined abandoned channel. From western Chautauqua County, N. Y., westward to Conneaut Creek Valley the waters no doubt found passages along the face of the escarp- ment either outside or just within the edge of the ice sheet, but sufficient attention has not been given to the channels to determine their full courses and connections. From the Chautauqua Valley eastward to the Conewango there are, as already indicated, moraine-headed terraces in each of the valleys dis- charging southward that contain a gravel outwash from the ice sheet and were evidently lines of vigorous discharge. Some of these terraces have their heads at the brow of the escarpment overlooking Lake’ Erie (see Pl. XIX), and yet lead directly away from the lake to the Allegheny River and thence through the Ohio and Mississippi to the Gulf of Mexico. In the headwater portion of Cattaraugus Creek there appears to have been a vigorous movement of the waters along the front of the ice sheet, such as would call for adequate outlet to the west. Fairchild has recently determined that there was a discharge from the South Cattaraugus past Persia Siding to the Conewango at an altitude but little above 1,300 feet above tide. Fairchild has also found evidence that the discharge shifted from this channel to channels leading westward from Gowanda along the face of the escarpment as the ice melted back. His studies are still in progress (in 1900) and promise to brmg out an interesting drainage history. The drainage from the part of the morainic system in the vicinity of LAKE ESCARPMENT MORAINES. 671 the Genesee River seems to have been southeastward to the Canisteo River, a tributary of the Susquehanna, through the Burns-Arkport channel, brought to notice by Fairchild.’ An outline of this line of discharge, given by Fairchild, is as follows. ? When the ice uncovered the region of Portageville the Genesee waters found an avenue of escape, 150 feet lower than Cuba, over the morainic dam east of Portageville and filled the Upper Nunda (Kishawa) Valley to the height of the 8 : pp SEN ) gs col north of Swains. Overflowing by the Swains-Canaseraga channel into the Dansyille Lake, the water ultimately escaped by the Poags Hole col, past the sites of Burns and Hornellsville, to the Susquehanna. INNER BORDER PHENOMENA. From the western terminus, near Euclid, Ohio, eastward to the vicinity of Dunkirk, N. Y., there is a narrow plain lying between this morainic system and Lake Erie. It slopes rapidly from the base of the escarpment, or from the inner border of the morainic system, toward the lake. The greater part of it has been under lake water and well-defined beaches, descriptions of which appear in Chapters XV and XVI, mark the different levels which the lake water has held. Over much of this lake plain rock is within a few feet of the surface, but there are filled valleys crossing the pla in which the drift is very thick. Their courses are in some cases entirely concealed, and generally are rendered quite obscure by the drift fillimg. The bluff of the lake often shows places where valleys come in whose courses across the lake plain are entirely concealed. The lake and stream bluffs and the well borings show the drift to be largely till. The coarse pebbles are scarcely so numerous as in the moraine and in places are rare, but, as a rule, this till differs little from the clayey till which covers the plains to the west of Lake Erie. In the intervals between the beaches there is a surprisingly small amount of sand or other wave-washed material, till being usually found within a few inches or at most but a few feet of the surface. The material covering the rock is there- fore largely glacial. Upon passing eastward from Dunkirk the Gowanda moraine soon appears and lies within a few miles north of this morainic system from that 'Glacial lakes of western New York, by H. L. Fairchild: Bull. Geol. Soc. America, Vol. VI, 1895, pp. 358-359. Also Glacial Gen_see lakes: ibid, Vol. VII, 1896, pp. 438-440, pls. 19 and 20. *Tbid., p. 439. 672 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. place eastward to the interlobate moraine in western Wyoming County. The portion of the Gowanda moraine west of Cattaraugus Creek lies along the south border of the lake plain near the base of the escarpment, and is separated from the morainic system under discussion only by a narrow strip, in places a mile or less in width, along the face of the escarpment; but from the point where it crosses Cattaraugus Creek, at Gowanda, northeast- ward to the interlobate moraine, the Gowanda moraine lies a few miles north of the inner border of this morainic system. This strip between the moraines, although involving the same succession of ridges and valleys that are crossed by the moraines, is strikingly different from the morainic strips. The slopes and crests of the ridges are nearly free from drift swells and the valley bottoms are smooth and open. The drift is also perceptibly thinner on the ridges than in the morainic strips. 5 East from the interlobate moraine there is, for some distance north from this morainic system, a somewhat hilly region with comparatively few drift knolls and a much thinner deposit of drift than appears in the moraine. The knolls do not seem to be arranged in such definite belts as in the Gowanda and Hamburg moraines which connect with the western side of the interlobe, yet their deposition probably extends over the time occupied in the production of each of these moraines. RELATION TO LAKE MAUMEE. The Lake Escarpment morainic system was apparently formed during the lower stage of Lake Maumee while it stood at the level of the Leipsic beach. That beach, as indicated on pp. 734-738, can be traced with some certainty as far east as the vicinity of Girard, Pa., though it is a compara- tively weak beach from Cleveland, Ohio, eastward. Farther east than Girard there are only faint and rather uncertain indications of wave action at the Leipsic level. The ice sheet appears to have persisted there until the lake had found a lower outlet and begun to form the Belmore beach. SECTION V. MORAINES OF WESTERN NEW YORK SOUTH OF LAKE ONTARIO. There are several short moraines in western New York between the Lake Escarpment system and the shore of Lake Ontario, two of which, the Gowanda and Hamburg, connect at the east with the interlobate moraine which extends northward from the Lake Escarpment system to northwestern GOWANDA MORAINE. 673 Wyoming County, while the remainder continue eastward past the north end of this interlobate moraine, in part as distinct ridges and in part coa- lesced. While they may have been formed in nearly as close succession as the several moraines of the Lake Escarpment system, they are on the whole more distinct from each other than those moraines, and should not perhaps be grouped as a single system. In the present discussion each morainic ridge receives a name, and the several ridges are considered in turn, beginning with the southernmost. GOWANDA MORAINE. DISTRIBUTION. The westernmost appearance of the Gowanda moraine, so far as recog- nized, is in a chain of knolls which lies along the base of the escarpment in Sheridan Township, Chautauqua County, N. Y., from near Sheridan east- ward to Walnut Creek at Forestville. On the east side of Walnut Creek it widens out to a strip a mile or more in width, which occupies the entire space between the Belmore beach and the base of the escarpment from Hanover Center eastward to the valley of Cattaraugus Creek at Gowanda. An isolated morainic tract, covering about 2 square miles,.appears on the north side of Cattaraugus Creek, 3 to 5 miles east of Irvig, as indicated im Pl. XIX. It stands below the level of the Forest beach, yet it presents a sharp knob-and-basin topography. Its relation to the Gowanda moraine is not understood. After crossing Cattaraugus Creek near Gowanda the moraine turns northward, following nearly the base of the escarpment past Lawton at an altitude but little above the level of the Belmore beach. Northeast of Law- ton it crosses over the ridge that lies between Cattaraugus and Kighteen- mile creeks, passing 2 or 3 miles east of North Collins and coming to Eighteenmile Creek Valley at Clarksburg. Thence its course is northeast- ward over another ridge to the east branch of HKighteenmile Creek at Boston Center. — It continues northeastward over a prominent ridge between East Eighteenmile and West Cazenovia creeks, and comes to the valley of the latter creek at West Falls. Thence its course is more nearly east across a ridge in southern Aurora Township, Erie County, to Hast Cazenovia Creek, at and north of the village of South Wales. It is not so well defined MON XLI 43 674 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. farther east, but seems to continue across Wales Township, Erie County, to the interlobate moraine in Sheldon Township, Wyoming County. The general width of this moraine is only about a mile and it is often considerably narrower. Its narrowest portions are usually the best defined, for the moraine is so weak that when spread over a width of more than a mile it becomes difficult to map its limits. RANGE IN ALTITUDE. The portion of the Gowanda moraine west of Cattaraugus Creek has a range of only about 100 feet in altitude, the lowest points being near the level of the Belmore beach, 840 to 850 feet above tide, and the highest about 950 feet. From Cattaraugus Creek northward past Lawton it remains at similar low altitudes, but in crossing the ridge east of North Col- lins it rises to about 1,300 feet. In each of the branches of Eighteenmile Creek its altitude 1s not far from 1,000 feet, but on the ridge between it is fully 1,300 feet. Farther east it fluctuates between about 1,100 feet in the valleys and 1,500 feet or more on the ridges, and is fully 1,500 feet at its junction with the interlobate tract in Sheldon Township, Wyoming County. TOPOGRAPHY. This moraine throughout its course consists largely of small swells, 10 to 15 feet high, which are separated by sags and winding, poorly drained depressions. Occasionally knolls 25 to 40 feet or more in height are found, and on the whole the portions in valleys carry larger knolls than the por- tions on ridges. Where the moraine is narrowed to about a half-mile the knolls are usually very closely aggregated and the expression is strong; but where it spreads out to a width of more than a mile the knolls become more scattering and the expression correspondingly weak. In the portion from South Wales eastward, as noted above, the knolls are very scattered and it becomes difficult in places to determine the limits of the moraine. STRUCTURE OF THE DRIFT. In the portion of the moraine west of Cattaraugus Creek, and also on the ridges farther east, the Gowanda moraine consists mainly of till. Wells often pass from a yellow into a blue till at 8 or 10 feet. The till is clayey in the low tract west from Cattaraugus Creek, but on the high tracts GOWANDA MORAINE. 675 it contains less clay and is thickly set with small fragments of the shaly sandstone of that region. In the valleys of Kighteenmile and Cazenovia creeks there are heavy deposits of silt and fine sand which were apparently laid down in water. These are capped by a few feet of stony material, some of which is assorted. The knolls and ridges which constitute the moraine proper carry consid- erable gravelly material. In railway cuttings north of Gowanda beds of gravel are exposed beneath the till, the till bemg in places only 6 to 8 feet thick. The gravel shows discordant stratification, some beds being horizontal and others having a sharp inclination. -'The gravel is only a local phase, for it passes horizontally into unmodified till within a space of a few rods. A bank of till 100 feet in height is exposed on the west side of Catta- raugus Creek about a mile west of Gowanda. It is of blue color and clayey, yet much of it is thickly set with stones, there being only a small part in which pebbleless clay appears. The coarse fragments are largely -of local shaly sandstone, but limestone pebbles are not rare, and there are not a few Canadian crystallines. This till was probably deposited while the ice sheet stood farther south than the Gowanda moraine, and may, therefore, not form a part of that moraine. It is capped by a few feet of gravel which was deposited as a delta in connection with the Belmore beach, its altitude being about the same as that of the beach. The Gowanda moraine carries a remarkably large number of surface bowlders. These serve to indicate its limits in places where the topographic expression is weak. They are largely granitic rocks, though many other Canadian crystallines are represented. The bowlders do not seem to be so numerous beneath the surface; at least there are but few exposed in the banks or bluffs of the streams and they are seldom struck in the excavation of wells. OUTER BORDER DRAINAGE. The position of the ice margin at the time this moraine was forming was very unfavorable for such a southward discharge of glacial waters as took place in connection with the deposition of earlier moraines. South- ward discharge could have been accomplished only by a ponding of waters south of the ice margin to sufficient height to raise the water surface to the level of the passes across the divide. This would demand lakes about 400 676 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. feet deep in much of the portion west of Cattaraugus Creek, while in the portion east a depth of 200 feet or more would be required simply to carry the water southward to the creek. The conditions were far more favorable for westward discharge from Cattaraugus Creek along the face of the escarpment than across these passes, and there is not wanting evidence of such a discharge. As to the drainage of the region that lies north of Cattaraugus Creek less has been determined. It is not known whether the waters were ponded sufficiently to throw the drainage into Cattaraugus Creek or had lower lines of discharge along or beneath the ice margin. Strong indications of a westward discharge from the western part of the moraine are found on the slope of the northward projecting part of the escarpment east of Forestville. A well-defined channel or scourway leads across from Silver Creek to Walnut Creek, and is utilized by the Erie Railway for a couple of miles about midway between Smith Mills and Forestville, as indicated in Pl. XIX. It stands between the 920- and 940- foot contours, and is therefore 80 feet or more above the level of the Belmore beach. It harmonizes well, however, with a delta on Walnut Creek at the village of Forestville, which stands between 900 and 920 feet. There are some indications of stream action along the base of the escarpment for 3 or 4 miles west of Walnut Creek, which seem referable to glacial drainage, while the ice margin occupied the district immediately north of the escarp- ment. The level of Lake Whittlesey was probably reached within a few miles west of Walnut Creek. These channels are now (season of 1900) ‘under investigation by Fairchild. Between Smith Mills and Cattaraugus Creek the writer noted short sections of an east-west channel and also shelves or terraces leading across divides between streams that now discharge northward; but the full relations of these channels and terraces to the glacial drainage were not determined. The writer also noted what appears to have been a line of glacial drainage across the projecting part of the escarpment near Smith Mills at a still higher level than the channel above noted, there being a conspicuous terrace at and west of the railway station at about 1,000 feet. This terrace may be mainly a rock shelf whose origin is independent of the glacial drainage, but its smoothness suggests the action of a current It contrasts strikingly with the irregular surface of the slope above this level. HAMBURG MORAINE. 677 INNER BORDER PHENOMENA. From the western terminus eastward to Cattaraugus Creek this moraine is followed closely by the Belmore beach, but farther east the beach bears away from the moraine, its course bemg through the low country, while the moraine rises to somewhat elevated country. The Hamburg moraine, which leads eastward from the village of Hamburg, lies, throughout its course, only a few miles north of the Gowanda, but is entirely distinct from it. Between the two moraines there is a strip in which the drift shows but little aggregation in knolls and is on the whole a thinner deposit than on either moraine. The most conspicuous development of morainic topography is near the mouth of Cattaraugus Creek, as indicated above. On some of the high ridges the drift is so thin that shallow ditches reach the rock, which in places is touched by the plow. In the valleys the drift is very thick, there being nearly as much as on the bordering moraines. Bowlders are much less conspicuous on this tract than on the Gowanda moraine, but otherwise the drift is not strikingly different in the two situations. The beaches and attendant lake features are discussed farther on. We therefore pass directly to the Hamburg moraine. HAMBURG MORAINE. DISTRIBUTION. The Hamburg moraine has not been recognized west of the village of Hamburg, N. Y., which is situated 10 miles south of the city of Buffalo. It seems probable, however, that the ice margin extended westward from Hamburg along the north side of Eighteenmile Creek to Lake Erie. Pos- sibly the somewhat indirect westward course of the creek will prove to be due to the presence, along its north side, of a water-laid morainic ridge so broad and low as to be scarcely perceptible and yet of sufficient relief to prevent the stream from taking the more direct course northwestward into Lake Erie. At Hamburg a distinct till ridge appears near the level of the upper beach of the Lake Warren series and leads northeastward to Orchard Park, where it is crossed by the Belmore beach. From Orchard Park the course is eastward across Cazenovia Creek to the north edge of East Aurora, and thence to Buffalo Creek, the outer border in Buffalo Creek Valley being at Porterville, and the inner border near East Elma. In the 15 miles from 678 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Hampurg to Buffalo Creek the moraine increases from less than a mile to fully 3 miles in width. East from Buffalo Creek it becomes still wider, and in eastern Marilla Township has two somewhat distinct members, one of which passes south of Williston, and the other north. The Hamburg moraine connects with the interlobate moraine of the Lake Escarpment system in the northwestern part of Wyoming County. Its length from Hamburg to the interlobate moraine is scarcely 25 miles, and if extended westward to Lake Erie it would not much exceed 30 miles. RANGE IN ALTITUDE. The crest of the moraine at Hamburg stands 825 feet above tide. It rises to about 875 feet at Orchard Park, and to fully 1,000 feet between Orchard Park and Cazenovia Creek. Between Cazenovia and Buffalo creeks its outer border stands 925 to 950 feet above tide, but the highest points in the midst of the moraine are probably above 1,000 feet. From Buffalo Creek eastward the inner border rises from about 950 feet to nearly 1,000 feet, and the northern, or mner, member has a crest reaching 1,000 feet near the meridian of Williston, and becoming still higher at its junction with the interlobate moraine. The inner member reaches about 1,100 feet on the meridian of Williston, and perhaps 1,200 feet at its junction with the interlobate moraine. TOPOGRAPHY. The greater part of the moraine consists of sharp knolls 20 to 50 feet in height, which, together with inclosed basins and winding sloughs, give it very strong expression. The most inconspicuous part is the crest and outer slope of the western portion, from near Orchard Park to Hamburg, where only gentle swells 5 to 10 feet in height occur. The sharp knolls are usually closely aggregated, but in Marilla Township the outer member consists of scattered knolls of considerable prominence, among which are nearly plane tracts which occupy more ground than the knolls. The inner member, as far west as Marilla, has closely aggregated sharp knolls. But from Marilla to East Elma there is a pitted gravel plain with basins 10 to 20 feet or more in depth, which often cover several acres each. The width ot this strip is a mile or more, and its length about 3 miles. It stands very near the level of the Belmore beach, and was apparently formed in the water. HAMBURG MORAINE. 679 On the inner slope of the moraine near Orchard Park the lake waves connected with the Belmore beach have formed a marked terrace from which the knolls have been cut away and the depressions filled, but west- ward from Orchard Park down the slope toward the upper beach of the Lake Warren series, the knolls and basins seem to have been modified but little by lake waves. The moraine appears to have extended but little north of the beach, though a few drift knolls were observed a mile or so north of it along the valley of Rush Creek. A small part of the moraine, about 2 miles southwest of Orchard Park, stands as an island above the level of the Belmore beach. It covers only about 40 acres, and the road from Abbotts Corners to Ellicott passes directly over it. Wave action is very clear on its north and west face, but the south and east are scarcely at all wave-cut. These and other features attending the lake occupancy are more fully discussed in connection with the beaches. STRUCTURE OF THE DRIFT. This moraine contains a remarkably large amount of gravelly material along much of its course. There is, however, from Hamburg nearly to Orchard Park, a ridge of compact clayey till forming the crest of the moraine. There is also much compact till on the high parts of the moraine between Cazenovia and Buffalo creeks. Gravelly knolls abound on the inner slope from near Hamburg to Orchard Park immediately north of the till ridge just mentioned, while from Orchard Park to Cazenovia Creek the crest, as well as slopes, is largely a gravelly material. There is an abandoned valley, probably of preglacial age, leading from Cazenovia Creek at East Aurora to Buffalo Creek at East Elma, and this is filled with sharp gravelly knolls and ridges, which are markedly in contrast with the gentile till swells on the higher part of the moraine north of this old valley. From Buffalo Creek eastward nearly all the knolls appear to contain gravel, while the low or gently undulating tracts among them carry a rather stony till. OUTER BORDER DRAINAGE. The line of escape for glacial waters at the time this moraine was forming was evidently westward into the glacial lake which was bordered by the Belmore beach (Lake Whittlesey). There is a well-defined channel leading from the head of Little Buffalo Creek, in southeastern Marilla 680 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Township, in a course south of west along the outer border of the Hamburg moraine to Buffalo Creek, just below Wales Center. Its altitude is fully 100 feet above the present bed of Buffalo Creek at Wales Center, or not far from 1,000 feet above tide. Upon reaching Buffalo Creek, the stream seems to have passed down the valley about two miles, or nearly to Portersville, and then turned westward along the face of the upland that. separates Buffalo Creek from the abandoned valley leading in from East Aurora. It soon entered that abandoned valley and followed it in a course south of west through East Aurora to Cazenovia Creek. Its altitude near the railway station in East Aurora is about the same as the station—925 feet. Its precise course for 2 or 3 miles west from Cazenovia Creek has not been determined, but it seems to have kept along the creek far enough to pass the elevated upland west of East Aurora, and to have then taken a south- westward course along the outer border of the moraine. Evidence that it took this course is found in a channel, now abandoned, whose south bluff is well defined, being cut into the face of the escarpment south of the meraine, but whose north border is vague. The east-west road leading from Kast Aurora to Deuels Corners descends into this channel about 2 miles east of Deuels Corners and keeps in it for about a mile toward the corners, when low shale hills set in. The channel passes between these hills and the higher land to the south, and has for a short distance a well-defined bluff on each side. West of the shale hills it enters the old lake at an altitude about 875 feet above tide, thus making a fall of 50 feet in the 6 or 7 miles west from East Aurora. The actual fall of the stream was, however, some- what less, for northeastward differential uplift, as shown in the neighboring beaches, has materially affected that region. The channel just described is but one-fourth to one-half mile wade and its blufis seldom exceed 30 feet in height. It seems rather small to have carried the full drainage from the melting ice sheet, and suggests the inter- pretation that part of the water may have worked westward into the lake beneath the edge of the ice sheet. | Between the two members of the moraine in eastern Marilla Township there is a small channel which leads westward past Williston to the pitted gravel plain south of Marilla. This was apparently formed by a glacial stream, for it is out of harmony with the present drainage and is largely an abandoned channel. MARILLA MORAINE. 681 There is still another channel which seems to have been formed just before the ice sheet withdrew from this moraine. It lies on the north slope of the inner member, but is limited on the north by a chain of drift knolls that separates it from a lower channel. Each of the channels passes across from Cayuga Creek to Little Buffalo Creek. The one under discussion seems to be in harmony with the Belmore beach and apparently connected with Lake Whittlesey at Marilla. The lower channel to the north seems to be connected with the upper beach of the Lake Warren series and is therefore of later date than this moraine. MARILLA MORAINE. DISTRIBUTION. The Marilla moraine appears to set in on the east side of Little Buffalo Creek immediately north of the village of Marilla in eastern Erie County, N. Y. If it continues farther west, it is either too faint to be easily recog- nized or is combined with the Hamburg moraine. From Marilla eastward into Genesee County it is a well-defined ridge separated by only a narrow, valley-like lowland from the Hamburg moraine. Its outer border passes just north of the corners of Wyoming, Genesee, and Erie counties, while its inner border passes from Erie into Genesee County immediately east of the — village of Alden. The Marilla moraine does not, like the Hamburg, connect with the interlobate moraine of the Lake Escarpment system, but passes the north end of the interlobate spur and continues eastward to Tonawanda Creek Valley south of Batavia, near which it passes beneath or becomes combined with the Batavia moraine. For several miles before reaching Tonawanda Creek it is combined with the Alden moraine, which farther west lies 1 to 3 miles north of it. The moraine is generally between 1 and 2 miles wide. Its course throughout is from south of west to north of east and is remarkably direct. RANGE IN ALTITUDE. This moraine shows remarkably little range in altitude compared with moraines to the south. Its altitude near Marilla is about 900 feet on the crest and 875 feet on the inner border; at the line of Erie and Genesee counties the crest is about 1,000 feet; from this county line eastward to 682 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Tonawanda Creek the crest generally stands between 950 and 1,000 feet, while the inner border in places extends down to less than 900 feet. TOPOGRAPHY. Along this moraine there is generally a definite ridging in line with the trend of the moraine. In places two or more parallel ridges appear in close succession, but quite as often there is a single main ridge, on the inner slope of which there may be subordinate ridges. The relief of the ridges seldom exceeds 40 feet, and is generally 30 feet or less. The undulations range from low, gentle swells to rather sharp knolls West from the Erie-Genesee county line the crest is in places nearly free from swells, and there are very few sharp knolls; but in Genesee County the surface is generally sharply undulating, with knolls 15 to 30 feet in height, which cover but a few acres each. The knolls are also more closely associated in Genesee than in Erie County. There are only a few well- defined basins, but winding sloughs are common among the knolls. There is a small esker situated in this moraine in the northeast part of Darien Township, Genesee County. It is less than a half mile long and only 50 to 75 feet wide, yet it rises generally to a height of fully 15 feet. The trend is nearly north to south, though the esker is slightly winding. Tt terminates at the south in a small gravel delta, which stands about as high as the crest of the ridge. This delta rises abruptly above low ground on the east, but is continued toward the west in a gravel plain which is at nearly the same level as the delta, and which is probably an outwash from the portion of the ice sheet immediately west of the esker, it being on the south border of the moraine. STRUCTURE OF THE DRIFT. The Marilla moraine carries much less gravel than the Hamburg, there being only an occasional knoll in which gravel is known to occur. The surface of the moraine, both on knolls and in depressions, is a rather clayey till, liberally strewn with bowlders. Large limestone slabs, gathered from the formations which outcrop between this moraine and Lake Ontario, are conspicuous both on the surface and in the midst of the till. Such slabs are rare on moraines outside of this one, but are common on those which lie between it and the lake. MARILLA MORAINE. 683 RELATION TO LAKE WHITTLESEY This moraine seems to have been formed nearly at the time when the lake level dropped from the Belmore beach to the Forest, and marks, therefore, the closing part of the existence of Lake Whittlesey. Taylor and the writer, after tracing the Belmore beach to Marilla, searched in vain for its continuation on the north slope of the Marilla moraine. That slope appears not to be modified by lake waves at the level of the Belmore beach. This matter is considered more fully in connection with the discussion of the Belmore beach. OUTER BORDER DRAINAGE. Along the south border of the western portion of the moraine, from southwestern Darien Township, in Genesee County, to the end of the moraine, near Marilla, there is an open valley occupied in part by an eastern tributary of Cayuga Creek, in part by Little Buffalo Creek, and in part abandoned. It shows a perceptible westward descent, and was evidently utilized by the glacial waters in their escape to the lake, if it was not opened by them. The width ranges from about one-fourth mile up to over one-half mile. The banks are usually low, being seldom more than 30 feet in height. At Marilla it is a few feet lower than the Belmore beach, and the valley continues descending westward till it reaches the level of the Forest beach, where an extensive delta is found that covers the interval between Little Buffalo and Buffalo creeks. It seems evident that by the time this channel was fully opened the lake level had dropped to the Forest beach and Lake Warren had succeeded Lake Whittlesey in the Erie Basin. From the head of the eastern tributary of Cayuga Creek, just referred to, eastward to Tonawanda Creek the line or lines of escape for glacial waters have not been clearly worked out. There are scourways among the glacial ridges and knolls in northern Darien Township which appear to mark lines of discharge, and which may, by detailed study, be found to form a connected system. These may, however, have been opened at the time the ice sheet was forming the Alden moraine, which, as above noted, is combined with the Hamburg from Darien Township eastward. This being the case, they do not throw light on the earlier part of the drainage. From eastern Darien Township eastward to Tonawanda Creek there is a sag or valley along the outer border of the moraine, which received some 684 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. outwash, but which may not have been excavated by glacial waters. The esker delta noted above lies in this sag, and its form seems to indicate that it was built up in a body of still water or in a stream with very sluggish current The gravelly outwash to the west of the esker delta and the delta itself indicate that currents of considerable strength were issuing from the ice sheet; but these were, perhaps, forced out by hydrostatic pressure into a body of water which had but little current. ALDEN MORAINE. DISTRIBUTION. The Alden moraine has been recognized no farther west than Alden Center, in eastern Erie County, N. Y. It appears as a well-defined ridge imniediately east of Alden Center on the east bluff of Ellicott Creek and just back of the lower or Forest-Crittenden beach of Lake Warren. It takes a course north of east into Genesee County, and, as above noted, becomes united with the Marilla moraine about 3 miles east of the county line. Its inner border at the west end is south of the Lackawanna Railroad, but the moraine soon crosses to the north side of that railroad and lies near the Lehigh Valley and New York Central railroads. For 2 or 3 miles in northern Darien and southern Pembroke townships, Genesee County, it extends slightly beyond (north of) the New York Central Railroad, but with this exception it lies south of that railroad to the valley of Tonawanda Creek in Batavia. ‘The Batavia moraine there comes in from the northwest and overrides or combines with the Alden moraine, and it has not been recognized between Batavia and the eastern limits of our district, the Genesee River. RANGE IN ALTITUDE. This moraine, like the Marilla, presents but little range in altitude; the western end, near Alden Center, stands about 850 feet above tide, and there are but few points between that place and Batavia that rise above 950 feet. TOPOGRAPHY. The greater part of this moraine is very similar in contour to the Marilla moraine, there being generally a definite ridging from east to west in line with the moraine. The ridges are not continuous for long distances, so that drainage lines find frequent gaps through which to pass northward. ALDEN MORAINE. 685 The knolls that are associated with the ridges are often quite sharp, but are only 10 to 30 feet in height. At the western end of the moraine there are numerous small basins bordered by gently undulating gravelly tracts. The appearance is some- what similar to that of the pitted gravel plains found as an outwash from the ice sheet. The outwash seems to have been directly into lake water, for the pitted plain stands at about the level of the beach of Lake Warren. STRUCTURE OF THE DRIFT. In structure the Alden moraine is similar to the Marilla, the greater part of the drift bemg a clayey till. Limestone pebbles and also large blocks are conspicuous ingredients of the till, and surface bowlders are numerous. OUTER BORDER DRAINAGE. It is probable that the glacial drainage from the vicinity of Tonawanda Creek to the western terminus of the moraine was westward. For a few miles it was through narrow channels among the knolls and ridges of the Marilla moraine; but from near Fargo, in Darien Township, Genesee County, westward to Alden Center, there is a plain 1 to 2 miles in width which stands near the level of Lake Warren, and which probably carried a shallow bay into which the glacial waters discharged. RELATION TO LAKE WARREN. To the north and east from this moraine there seems to be but a single beach of Lake Warren, the Lower Forest or Crittenden, while to the south and west there is a more complex system. The moraine seems therefore to correlate with a somewhat lengthy part of the Lake Warren history. This matter is considered more fully in the discussion of the beaches of Lake Warren. PEMBROKE RIDGES. DISTRIBUTION. Under this name is discussed a complex system of sharp gravelly knolls and ridges which leads eastward from the west part of Pembroke Township, in western Genesee County, to the Batavia moraine in western Batavia Township, a distance of about 10 miles. They are in part shown on PI. III. There are usually two, and in places three, ranges of knolls, each trending 686 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. from south of west to north of east. The southern range les only 1 to 2 miles north of the inner border of the Alden moraine. The second range lies 1 to 2 miles farther north. The second range crosses to the north side of Tonawanda Creek near East Pembroke, while the south range lies south of the ereek all the way to the Batavia moraine. There is a short range of knolls south of Indian Falls, which is fully 2 miles north of the second range. A range west of East Pembroke is also somewhat distinct from the second range, and trends from southwest to northeast. These ranges of knolls may find westward continuation toward Buffalo along the Corniferous escarpment, there being a few drift knolls and short ridges scattered along the base of the escarpment from Akron westward, and a few knolls on the escarpment between Akron and Crittenden. These knolls along the base of the escarpment may, however, be incident to the retarding influence of the escarpment upon the ice movement, in which case they may indicate nothing as to the position of the ice margin. RANGE IN ALTITUDE. The highest point in this system of knolls is in a gravel ridge on the north side of Tonawanda Creek, about 2 miles northeast of East Pembroke, which bears some resemblance to an esker. This ridge, as shown by the Medma topographic sheet, rises above the 1,000-foot contour. It is 75 to 100 feet higher than the majority of the knolls in that vicinity, and stands 130 feet above low ground within one-fourth of a mile to the east, north, or west. The crests of the two ranges generally stand between 900 and 950 feet, while the low ground on their borders is about 850 to 875 feet. TOPOGRAPHY. The south range of knolls is in places scarcely one-fourth of a mile in width, though the knolls rise 30 to 50 feet above bordering plane tracts. There are scattering knolls along the north border of this range which are but 10 to 15 feet high. The range has, on the whole, greater continuity than the one north of it, but is not so prominent. The north range contains several knolls 75 feet or more in height and many are 40 to 50 feet. It is so prominent that its course may be seen for several miles at a stretch. Some of the knolls are sharp and conical; others are elongated, though seldom to a greater length than one-fourth of a mile. The large knolls carry hummocks on their slopes and also send out irregular spurs, which add PEMBROKE RIDGES.- 687 to the complexity of the range. The portion on the north side of Tona- wanda Creek lies within the limits of the Medina quadrangle and occupies the interval between the creek and a marshy tract nearly parallel with it a mile or so to the north (see Pl. II). The most prominent group of knolls in this part of the range bears some resemblance to an esker, in that it trends directly across the range and has a sharp, narrow gravel ridge. The ridge has not, however, so smooth a crest and slopes as generally characterize eskers. The north end rises abruptly to a height 130 feet above the bor- dering marsh, but most of the ridge is only 75 to 90 feet above the marsh. It is about a mile in length and is narrow and sharp throughout its course. The knolls around this esker-like ridge are generally but 20 to 30 feet high, being less prominent than in the part of the range farther west, on the south side of ‘Tonawanda Creek. The range standing south of Indian Falls is less than a mile in length and scarcely one-fourth mile in width, but stands nearly 40 feet above bordering tracts on the south and east,and even more above the tract on the north. From this range southward to the main range there is a gently undulating strip strewn with bowlders, that separates the old lake plain on the west from a shallow bay on the east which occupied 3 or 4 square miles. STRUCTURE OF THE DRIFT. - So far as can be ascertained from the surface ditches and shallow excavations, these ranges of knolls are composed of gravelly and sandy material with but little clayey till) They are in striking contrast to the Alden and Marilla moraines, which, as above noted, are composed largely of clayey till, There are numerous surface bowlders, but there seems not to be many bowlders incorporated in the drift. The cause for so much water action in connection with the production of this moraine is not apparent. It does not seem due solely to its having been formed near the level of Lake Warren, for in that case we should expect the Alden and Marilla moraines to show evidence of more water action. OUTER BORDER DRAINAGE. There is a sag along the outer border of the south range extending from its western end at the shore of Lake Warren eastward nearly to Batavia, which affords adequate room for westward discharge of glacial 688 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. waters. It is now utilized for a few miles by Murder Creek. The sag stands but little above the old lake level, and probably was in part occupied by a bay at the level of the lake. There is also a sag between the south and north ranges which would have afforded a line of discharge for glacial waters issumg from the north range. It is now utilized from near Kast Pembroke westward by a tribu- tary of Murder Creek, while Tonawanda Creek utilizes the part east of Kast Pembroke. BATAVIA MORAINE. DISTRIBUTION. The Batavia moraine forms the south member of a rather complex series of moraines, drumlins, and eskers, which occupy the district imme- diately south of Lake Ontario. The writer applied the name Lockport to this south member some years ago,’ but upon further consideration it seems preferable to substitute the name Batavia. The western part is so vague that some uncertainty is felt as to its continuation. The Batavia moraine, from. the Genesee River westward to the Tonawanda swamp in north- western Genesee County, lies just south of the drumlin belt and has a general course slightly north of west. From that swamp westward two lines invite attention: one continues the course north of west to Lockport, passing to the north side of the few drumlins which appear in that region; the other leads south of west along or near the base of the Corniferous escarpment toward Buffalo, keeping south of all the drumlins. The latter course seems to have in its favor a relationship to the drumlins similar to that found farther east. It, however, differs in being not even approxi- mately at a right angle with the trend of the drumlins, but instead is nearly in line with them. So far as morainic features are concerned, there is very little to favor this line, there being only occasional slight ridging and a few knolls and basins; and these, as already indicated, may be incident to the retarding influence of the escarpment upon the ice movement rather than marginal accumulations of a morainic character. While the uncertainty as to this line is great, it should perhaps be held as a possible continuation of the ice margin, especially since the line toward Lockport seems also open to question. ‘Turning to the latter line we find 1Am. Jour. Sci., 3d series, Vol. L, 1895, pp. 13-17. BATAVIA MORAINE. 689 that there is a definite belt of ridges and knolls leading from the Tona- wanda Swamp toward Lockport, which seemed to the writer, while in the field, to be the more probable continuation of the Batavia moraine. The gap at the Tonawanda Swamp, which separates it from that moraine, is less than 2 miles wide, and the ridges on opposite sides of the swam) are about in line with each other, as may be seen by reference to Pl. III. It is found, however, that the north or main ridge of the belt west of the swamp is practically continuous with the Barre moraine, which leads in from the east along the north side of the drumlin belt. This may not oppose the interpretation that the belt constitutes the continuation of both moraines, but it certainly leaves it open to question. The description of the Batavia moraine will consequently be carried eastward only from Tonawanda Swamp, the portion of the morainic system to the west bemg described in connection with the Barre moraine. The Batavia moraine, as shown in PI. III, leads from the southeast border of Tonawanda Swamp southeastward across Alabama Township, Genesee County, passing south of Alabama Center and Smithville and coming to the Corniferous escarpment immediately south of the latter village. On rising to the brow of the Corniferous escarpment it leads toward Batavia and crosses over or becomes combined with the Pembroke, Alden, and Marilla moraines. From Batavia it continues south of east as far as Oatka or Allens Creek, which it crosses 2 to 4 miles south of Leroy. It then takes a course nearly east to the Genesee River, coming to that stream immediately below (north of) the village of Avon. Its farther course was not determined. RANGE IN ALTITUDE. The Tonawanda Swamp is about 620 feet above tide. The altitude increases gradually from the swamp to the Corniferous escarpment, reaching about 780 feet at the base and 900 feet at the brow of the escarpment south of Smithville. The highest points between Smithville and Batavia are about 960 feet, one being at the geodetic station 4 miles west of Batavia, and others between that place and the city. An altitude of 900 to 950 feet prevails for several miles east from Batavia. The moraine then begins to descend toward the Genesee River, and is below 600 feet on the border of that stream. MON XLI——44 690 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. TOPOGRAPHY. . On the east border of Tonawanda Swamp the moraine rises into a stout till ridge 30 to 50 feet in height, which has a well-defined crest and gently undulating surface and is a prominent feature for at least 4 miles Its con- tours are to some extent shown on the topographic map, Pl. IIL. Upon rising to the Corniferous escarpment the moraine breaks up into a series of knolls and short ridges, rather sharp in contour, which inclose basins and winding sloughs. This phase becomes conspicuous at the place where the moraine rises above the level of Lake Warren, though a few knolls and basins appear southwest of Oakfield at a considerably lower level. he northwest side of this till ridge, just discussed, is fully 200 feet below the level of that lake, and is a remarkably strong feature to have been formed in such a depth of water. The contours of the part of this moraine which was formed above the level of Lake Warren are partly brought out by the topographic maps, the course of the moraine being through the northeast part of the Medina quadrangle and the southwest part of the Batavia. It will be observed that the height of the knolls and ridges ranges from 60 feet down to less than 20 feet. Many small knolls less than 10 feet in height are not represented on the maps, and _ this detracts greatly from their expression. The moraine holds its sharp features as far east as the valley of Allens Creek, near Leroy, but within a few miles east from that creek the sharp knolls change to very small swells and the prominent knolls and ridges present smoother slopes than to the west. The ridges are not so long nor so definite as in the district below the Cerniferous escarpment, but they are fully as high. This part of the moraine was also formed in water, for a glacial lake occupied the Genesee Valley at the time it was forming. STRUCTURE OF THE DRIFT. The portion of the Batavia moraine between the Corniferous escarpment and the Tonawanda Swamp contains a large amount of compact till, but the portion on the escarpment carries a loose stony till and also considerable gravel and sand. The gravelly ingredients are more conspicuous from Batavia northwest to the brow of the escarpment than east from that city. The portion of the moraine which stood above the level of Lake Warren carries a large number of surface bowlders, but bowlders are not a con- spicuous feature on the part formed below the level of the lake. DRUMLINS OF WESTERN NEW YORK. 691 WESTERN NEW YORK DRUMLIN BELT. DISTRIBUTION. The extent of the dramlin belt from the Genesee River westward to Niagara River is well shown on the Rochester, Brockport, Albion, Medina, Lockport, and Tonawanda topographic sheets, incorporated in Pl. II, the contours of the oval-shaped hills being a sufficient means for identification. The drumlins are all situated in the district between the Corniferous and Niagara escarpments.’ It will be observed that in the Rochester quadrangle the drumlin belt crosses to the west side of the Genesee below Scottsville, and nearly occupies the interval of 7 miles between Allens Creek and Black Creek; on the Brockport quadrangle the south border lies near Allens Creek, while the north border is 6 to 8 miles farther north, being generally about 2 miles north of Black Creek; in the Albion quadrangle it les mainly in the northern townships of Genesee County (Bergen, Byron, Elba, and Oakfield), but extends southward into Stafford Township, in the vicinity of the New York Cen- tral Railroad; in the Medina sheet it is represented in only a few small drumlins on the south side of Oak Orchard Swamp, in Oakfield and Alabama townships. There is an interval of about 15 miles in which no drumlins occur; but near Raymond, south of Lockport, there is a group of three drumlins; and near Pendleton Center, a few miles farther west, there is a similar group, and still farther west, near Tonawanda, an oceasional low drumlinoid ridge. Where best developed the drumlins occur at intervals of one-half mile to a mile, and there is usually a nearly plane surface among them, but where they are poorly developed the drift among the drumlins is liable to be ageregated in knolls of irregular shape, often bearing no resemblance to drumlins. The drumlins prevail to the exclusion of other drift knolls only in very limited areas. It will be observed that they are most abundant in the northern and eastern parts of Elba Township, Genesee County, and thence eastward along the borders of Black Creek to the Genesee River. In the southern part of the drumlin belt there are many small drift knolls and ridges which do not appear on the topographic sheets, but which tend to give the surface a morainic appearance. The 1A few drumlins near the mouth of Genesee River do not fall in the belt under discussion. 692 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. drumlins near Lockport and farther west stand in a very level region, decidedly in contrast to that found in the drumlin belt to the east. RANGE IN ALTITUDE. Although the drumlins of this belt are all situated in the district between the Niagara and Corniferous escarpments, the belt shows a range of about 300 feet in altitude. They appear at the lowest altitude near the Genesee River, 525 to 550 feet, and at the highest altitude in eastern Elba and northern Stafford townships in the Albion quadrangle, where their crests, in a few instances, rise above the 820-foot contour. It should, perhaps, be explained that there are other drumlins near the shore of Lake Ontario (some of which appear in Pl. III) that are not in the belt under discussion. TOPOGRAPHY. The usual form assumed by the drumlins in this region is an elliptical smooth-surfaced knoll, a mile or less in length and scarcely one-fourth mile in width, but in places they are elongated to 10 or 12 times their width and reach a length of 2 miles or more. They trend in a general northeast- southwest direction, with variations of perhaps 20° on either side of a due northeast-to-southwest line. The northeast end shows a tendency to be more abrupt than the southwest, though a large proportion of the drumlins are very symmetrical. Where the sides are not symmetrical the southeast is usually the more abrupt. The height ranges from 10 or 15 feet up to about 100 feet, but in the majority it is not far from 40 feet. The most prominent drumlins are in northern Elba Township, the one utilized for the Parker geodetic station being about 105 feet above the Oak Orchard Swamp, only one-fourth mile to the north. Two miles farther west a knoll of gravelly constitution and less regular form than the typical drumlin stands 130 feet above the bordering swamp. The knolls and ridges which occur among the drumlins and along the south border of the belt are of various shapes and sizes, as may be seen to some extent in Pl. II]. There are with these knolls and ridges small, nearly plane areas carrying shallow basins. Such areas are usually gravelly, and present the appearance of the pitted outwash plains that border moraines. These pitted plains occur at intervals along the north side of Allens Creek from Scottsville westward to the bend north of DRUMLINS OF WESTERN NEW YORK. 693 Leroy. They are also conspicuous in the vicinity of Oakfield. In general they are near the south border of the drumlin belt, and, together with the neighboring drift knolls and ridges of morainic type, they support the view that the ice margin at one time stood near a line drawn along the southern edge of the drumlin belt. This interpretation is strengthened by the fact that an exceptionally large number of bowlders occur throughout the drumlin belt from the Genesee River westward to the point where it dies out in western Genesee County. They abound among the drumlins as well as on them, and on nearly plane tracts as well as on knolls. STRUCTURE OF THE DRIFT. The drumlins are usually composed of a compact blue till, and it is rare to find assorted material in them. Some of the most prominent ones, however, are known to contain gravel. From the numerous well sections obtained it would appear that the drumlins rarely if ever have a rock nucleus’ In many cases the wells extend far below the base of a drumlin without entering rock. For several miles west from the Genesee River the drumlins carry a coating of fine sand, deposited apparently by lake water after the withdrawal of the ice sheet. In some cases the depth of the sand is several feet, but it is usually only a few inches. The heaviest deposits noted are those lying on the west side of Genesee River, north of Scottsville. The knolls and much of the plane-surfaced drift among the drumlins contain a large amount of gravel with the till. This is especially the case in the southern part of the belt. The presence of gravel is known chiefly from well data, but there are a number of places where gravel pits have been opened. The bowlders are apparently more numerous on the surface than beneath, at least wells seldom encounter them. They are so abundant on the surface as to afford material for many miles of wall fence, and are also piled in large heaps in the fields. The majority are granite rocks, but slabs of limestone are rather common. In size there is considerable variation from place to place, there bemg in some localities only small stones a foot or less in diameter, while im others many large bowlders are present. These variations are probably significant, but like the variations in the underlying drift, the significance is not yet apparent. 694. GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. RELATION TO LAKE WARREN. After forming the Batavia moraine the ice sheet apparently withdrew from the Corniferous escarpment sufficiently to allow the waters of the Genesee glacial lake to enter Lake Warren and take the level of that lake. This blending of the lakes in all probability occurred while the drumlins and their attendant morainic phenomena were being produced, and the connecting portion of the beach of Lake Warren would date from this time. Possibly the lake waters were barred out or were of little effect for a considerable part of the time that the drumlins were form ng, for drumlins were apparently submarginal rather than terminal accumulations of the ice sheet; but the southern portion of the belt, with its morainic knolls and pitted gravel plains, seems to have been nearly coincident with the ice margin for at least part of the time. It is a matter of much significance that these pitted gravel plains appear at levels far below the level of Lake Warren and in positions where it would seem probable that the lake had free access to the ice margin. Those near Oakfield are fully 100 feet below the level of the neighboring part of the beach of Lake Warren, while those along the border of Allens Creek are 150 to 250 feet or more below the beach. There is a gravel plain just west of Scottsville on the north side of Allens Creek which stands between the 580 and 600 foot contours, or about 275 feet below the beach of Lake Warren. This has been extensively opened for gravel in a direction favorable for showing the mode of formation, there being a pit about one-fourth of a mile long extending from north to south across the gravel plain. The bedding shows that it was built by a stream moving southward away from the ice sheet but up the Genesee Valley. The beds were built out from north to south in the form of a delta, the topset and foreset beds being well exposed. The dip of the foreset beds is most abrupt in the middle part of the pit, being 25° to 30° below the horizontal. With the advance of the delta southward the angle of dip decreases to 10° or less. The material is a sandy gravel with many stones 2 or 3 inches in diameter. It is, on the whole, finer and less distinctly assorted than in the outwash gravels formed in situations where the water had free escape. If Lake Warren still persisted the material contained in this delta and other gravelly deposits along the southern border of the drumlin belt seems likely to have been forced out by hydrostatic pressure from the edge of the ice sheet into the bordering lake. EE EEEEEEEOEOOOEOeeEOeeeeeeeee eel eee BARRE MORAINE. 695 Excavations in the pitted plain southwest of Oakfield, near the Fertilizer Works, show till interbedded with gravel and sand in such manner as to suggest either a readvance of the ice to form the till, or the deposition of the gravel beneath the ice margin. The form of the pits or basins seems to favor the view that the ice was present and prevented their being filled with gravel. The gravel deposits of this region, while presenting considerable similarity to the outwash found in localities where there was free discharge for the glacial waters will probably, upon close inspection, reveal through- out their extent features which are compatible with the obstructed drainage due to the presence of the waters of Lake Warren. BARRE MORAINE AND ASSOCIATED ESKERS. DISTRIBUTION. The Barre moraime presents a nearly continuous chain of ridges from the head of Oak Orchard Swamp, near South Barre, in southern Orleans County, westward to Lockport. Its crest passes through the, villages of West Barre, Hast Shelby, Royalton, and MecNalls, in a slightly winding course, as shown on PI. III. From its crest eskers and morainic spurs extend north a mile or two, but the main ridge is only about one-fourth of a mile in width. South from the main ridge in western Orleans County small ridges and knolls are scattered over the interval between the ridge and Oak Orchard Swamp. Knolls and ridges also lie south of the main ridge in Niagara County out to a distance of about 2 miles. Those in Niagara County, as above indicated, may belong to the Batavia moraine. The continuation from Lockport seems to be in a northward course toward Wilson, on the shore of Lake Ontario, there being an exceptionally large number of bowlders in that direction. No sharply outlined ridges or other morainic features were noted, but as the drift here was laid down in a great depth of lake water such ridges could hardly be expected. From South Barre eastward the course of the Barre moraine is rather indefinite. There is, however, a prominent group of knolls in the “New Guinea Settlement” at the head of Oak Orchard Swamp, in southwestern Clarendon Township, which constitutes a natural line of continuation. From this group the course seems to be south of east into northeastern Genesee County, there being more drift knolls in that direction than to the east or northeast. Its continuation in Monroe County seems to be in knolls near the line of Ogden and Riga townships and in the north part of Chili 696 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Township. This belt of knolls is situated immediately north of the north border of the drumlin belt from near the ‘‘New Guinea Settlement” east- ward to the Genesee River, and presents a strikingly different topography, as may be seen by the topographic sheets and to some extent in Pl HI. The number of knolls is greater than in the district to the north, though the latter is by no means free from them. RANGE IN ALTITUDE. The principal variation in altitude is made in rising from the plain north of the Niagara escarpment up to the brow, the altitude near the base being only 400 feet and on the brow about 630 feet. The level of the base of the drift ridges and knolls from the escarpment eastward to Oak Orchard Creek falls between 620 and 650 feet, while the crests of the ridges range from about 630 feet up to 700 feet, the highest points being near West Shelby. From West Shelby to East Shelby the crest stands generally between 650 and 675 feet, but knolls on a spur north of the main ridge near the Ross geodetic station rise above 700 feet. From East Shelby to West Barre the crest is mainly between the 660- and 680-foot contours, but a point on an esker at the Pusel geodetic station, a mile northwest of West Barre, reaches 737 feet. This appears to be the highest point in Orleans County. From West Barre to South Barre the crests of ridges range between 650 and 700 feet, the lowest ridges being situated in the edge of Oak Orchard Swamp. At the border of the sharp drift knolls in the New Guinea Settlement, the swamp stands just below the 640-foot contour, while some of the knolls rise above the 700-foot contour. From this group of knolls eastward to western Monroe County there is but little descent, the altitude being generally between 620 and 650 feet; but from the meridian of Churchville to the Genesee River, a distance of about 12 miles, there is a descent of almost 100 feet, the altitude on the border of the Genesee being but little above the 520-foot contour. . Particular attention is called to the range in altitude because the narrow ridge leading westward from West Barre has been considered a beach of Lake Ontario by many of the residents. The form and structure in places seem to sustain that interpretation. This is especially true of the part between West Barre and West Shelby; but in this part of the ridge there are oscillations of 30 or 40 feet in the level of the crest within a distance of BARRE MORAINE. 697 less than 5 miles, a difference which seems too great to be due to uplift. Uplift here may amount to a foot or more per mile alone a line from south- west to northeast, as shown by measurements on the neighboring portion of the beach of Lake Warren. A variation of 10 to 12 feet may also occur in a shore line, independent of uplift, there beg that amount of variation in the beach of Lake Erie. But if these are combined it would cause scarcely half the variation in altitude which this part of the ridge displays. TOPOGRAPHY. There are few moraines which present greater variations in topography than are displayed by this one. Knobs and basins, smooth till ridges, eskers, drumlioid forms, and nondescript or irregular forms are all present. For a few miles south from Lake Ontario only a few low swells can be detected, but the bowlders which appear in greet numbers seem to indicate the position of the ice margin. They occupy a belt 2 miles or more in width, in which they have been heaped in great piles in the fields and built into stone walls. On the face of the Niagara escarpment for 2 miles east from the eastern edge of the city of Lockport the moraine consists of a series of knolls and basins, which give that part of the escarpment an appearance strikingly in contrast with the smooth face it presents west from Lockport. From the brow of the escarpment about a mile east of the city limits of Lockport a well-defined ridge 15 to 40 feet in height and one-fourth mile or less in width leads eastward past McNalls and Royalton. Its surface is gently undulating, like the till ridges so common on the plains of Ilinois, and, like them, it is composed largely of till. To the north, between this ridge and the escarpment, there is a gently undulating tract thickly strewn with bowlders, while along the brow of the escarpment several knolls 15 to 20 feet high appear. South of the till ridge the surface is nearly plane as far east as the meridian of MeNalls. A system of knolls and ridges there sets in which leads eastward to West Alabama, and which may belong to the Batavia moraine. The ridges are broken by occasional gaps and are some- what disjointed, but are definite for 2 or 3 miles at a stretch, as shown by the topographic map (Pl. III) In form they are similar to the ridge that leads through Royalton, but they are also similar to the till ridge southeast of Tonawanda Swamp in Alabama Township, Genesee County, of which they are, perhaps, the continuation. 698 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The main ridge leads from Royalton eastward to West Shelby, but becomes irregular, and at West Shelby connects with a prominent morainic spur which extends north about 2 miles It also changes in constitution to a mixture of gravel and till. In the spur that leads north from West Shelby there are sharp knolls 20 to 40 feet high, among which basins are inclosea that cover areas of from 1 to 5 acres each. It is a very gravelly belt, but there is usually a thin capping of till thickly set with bowlders About a mile east from the north end of this morainic spur is an isolated sharp ridge of sandy till, on which Ryan geodetic station was placed. The ridge is about one-half mile long and trends north-northeast to south- southwest. Its highest points are about 60 feet above the bordering plain. There are knolls 15 to 30 feet high along its slopes. On the east side of Oak Orchard Creek there is greater complexity than on the west. The main ridge is very definite all the way from the creek to West Barre, but ridges north and south of it are scattered over a nearly plane tract occupying only a small part of the surface. The main ridge in places presents a smooth surface like a beach line and is narrow and low, the height bemg but 10 to 15 feet and width 5G to,75 yards; but usually its surface is more irregular than a beach line, there being variations of 15 to 20 feet in height within short distances. The bulk is also greater on the whole than beaches commonly display, the width being from an eighth to a fourth of a mile and the height from 10 to 40 feet. Of the scattering ridges found south of the main ridge the most prominent is at Edwards geodetic station, its height being about 50 feet. The majority are between 15 and 25 feet in height. These ridges are commonly but an eighth of a mile or less in width and one-half mile to a mile or more in length. The usual trend is from north of east to south of west, being similar to that of the drumlins, but this is the only point of resemblance, the surface being less regular than that of drumlins. They also are largely composed of sand and gravel, while the drumlins are mainly of till. North of the main ridge there are only scattering knolls and low wind- ing ridges for a mile or two east from Oak Orchard Creek. A sharp range of gravelly hills then sets in, which trends northwest to southeast. Its highest points stand 75 to 100 feet above bordering plane tracts and its BARRE MORAINE. 699 surface is very irregular, as may be seen by reference to the topographic map (PI. III). For several miles east from this range of knolls the sur- face is nearly all plane, there being only an occasional low knoll. There is then a sharp ridge with north-south trend, which connects at the south near Kast Shelby with the main ridge. It is about 14 miles long and one- fourth mile or less in width. Its height ranges from 15 to 60 feet. The surface is thickly strewn with bowlders, which add to its morainic expres- sion. his ridge and the range of gravelly bills to the west seem to be morainic spurs rather than eskers; at least they are not so regular in form as eskers. The most prominent ridges of Orleans County are found in the next spur to the east. They cover a track nearly 2 miles in length (from north to south) and a mile or less in width. The main ridge bears some resem- blance to an esker, but there are many irregular-shaped ridges and knolls associated with it. It terminates at the south in a flat-topped tract which stands about 80 feet above the bordering plains and which incloses a deep basin. A marsh lies in the midst of this system of ridges. There is on the west side of the marsh a ridge about 40 feet in height which has a flattened top im which there are shallow basins. On the east side of the marsh is a less regular ridge, which in places presents the form of an esker. From West Barre eastward to the east end of Oak Orchard Swamp the ridges and knolls are similar to those found south of the main ridge to the west from West Barre. They trend east-northeast to west-southwest and are rather narrow and sharp. The height is seldom less than 15 feet and in places reaches 40 feet. | The prominent group of ridges and knolls in the New Guinea settle- ment at the east end of Oak Orchard Swamp is well represented in PI. III. Basins appear on the crests of the ridges, two of which are shown on the map. The ridges rise abruptly 40 to 60 feet above the bordering swamp. From this group of ridges eastward to the Genesee River the knolls are rather scattered and of irregular shape. They contrast strikingly with the regular form of the drumlins to the south, as may be seen by reference to the topographic map. Two ridges in this part of the morame are worthy of notice, one is an esker or gravel ridge near Ogden and the other a sandy ridge near Chili. East and south of Ogden Village there is a narrow gravel ridge 15 to 700 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. 30 feet in height and about 2 miles in length, including small gaps. The northern half has a nearly due north-south trend, but the southern half bears southwestward. The topographic map shows the change im trend but fails to bring out the esker form which it presents. From near Chili northeastward to the bend of Coldwater or Little Black Creek there is a sandy belt about 1 mile wide and 3 miles in length, which has a knob-and-basin topography. Its highest pomts stand about 60 feet above Little Black Creek. The topographic features as well as the sandy material suggest wind action, but bowlders were found embedded in the sand and on its surface, which seem to indicate that the features are only to a minor degree due to the wind. Glacial action seems to have been the main agency. The intricacy of this belt is brought out to a fair degree by the topographic map. South of this sandy belt from Chili eastward to the Genesee River is a gently undulating till tract, with knolls usually but 10 to 15 feet in height, while to the north the surface is even less undulatory and carries scarcely any sand. This sandy belt has about the same trend as the strize of that vicinity, and meets the remainder of the moraine obliquely. It is in a nearly direct line of continuation of the Pinnacle Hills ridge of Rochester, but is separated from it by a gap about 4 miles in width, which is partly occupied by a later moraine. The presence of this moraine is thought to indicate that the Pinnacle Hills ridge was formed later than the Chili sand belt. STRUCTURE OF THE DRIFT. In the Barre moraine, as well as its associated spurs, eskers, ete., there is a large amount of gravel and sand. Indeed, till seems to predominate over assorted material only for a few miles east from Lockport. The ridges there as well as the plains are principally till. Farther east there seems to be considerable till in plane tracts, but the ridges are chiefly gravel. The most prominent ridges are usually thickly strewn with bowlders, but they are not so numerous on the low ridges and on plane tracts. Among the bowlders, which are largely of granitic rocks, there are not a few limestone slabs gathered from the immediate vicinity. The drift is ordinarily so thick along the line of this moraine that wells are obtained without entering rock. There are, however, small areas around Shelby Center and Barre Center as well as farther east where the drift is very thin, so that the rock ledges are within reach of the plow. ALBION MORAINE. 701 RELATION TO LAKE WARREN. The highest poimts on this moraine stand more than 100 feet below the level of the neighboring part of the beach of Lake Warren, while the lowest parts are several hundred feet below the level of that lake. On theoretical grounds the ice sheet appears to have terminated in that lake at the time the Barre moraine was forming. On this assumption its deposits are all water-laid. It seems remarkable that under these conditions assorted material, and especially coarse gravel beds, should form so prominent con- stituents of the drift. There being no line of rapid escape for the waters from the ice margin, it would seem natural for the fine material to be laid down with the coarse, though possibly there was sufficiently vigorous movement of water under the ice to cause much assorting of its deposits and removal of fine material. ALBION MORAINE. DISTRIBUTION. The course of this moraine has been accurately traced only from Albion eastward to Rochester, but it has been crossed on the New York Sentral Railroad, directly south of Knowlesville, and appears from the con- tours of the Medina. topographic sheet to come to the Erie Canal 14 miles west of Knowlesville, and to be continued westward in a series of knolls on the borders of Oak Orchard Creek, 1 to 3 miles north of Medina. From the railway crossing south of Knowlesville to Albion the crest of the moraine is less than a mile south of the New York Central Railroad, and is followed by a ‘“‘ridge road.” The moraine is scarcely one-fourth of a mile in width, but presents a very definite ridge. It is cut through by Sandy Creek near the southeast edge of the city of Albion, but the gap is very narrow, and the ridge continues to the Albion Cemetery, 14 miles east of the city, where it rises into greater prominence. There are minor ridges and small knolls and also basins in Albion and eastward to the cemetery, extending out to a distance of nearly a mile north of the main ridge, but west from Albion such features are rare. At Albion Cemetery there is a knoll standing nearly 100 feet above low ground on the south and 60 to 75 feet above the neighboring parts of the moraine. Toward the east the moraine continues with sharp ridges and 702 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. knolls as far as the west border of Murray Township, 2 miles. It is then vague for about a mile, but reappears on the brow of the Niagara escarp- ment near a schoolhouse. About one-fourth mile east of the schoolhouse a gap about one-fourth mile wide sets in, but this gap is bridged by a reef of bowlders. East of this gap for about 2 miles the ridge. lies just south of an east-west road and is very sharp and narrow. About 14 miles west of Holley the moraine makes a southward jog to Clarendon, and thence passes in a nearly east course into Monroe County. Tn this deflection it passes around an esker that les between Holley and Clarendon. The moraine becomes more complex on passing east from Clarendon, its ridges and knolls being scattered over a belt 1 to 2 miles wide, lying mainly south of the Erie Canal. The main ridge, however, is along the southern border, and is, as a rule, definite and nearly continuous. It passes through Lake View Cemetery, 15 miles south of Brockport. There are drift knolls and ridges in Brockport and eastward from there to Spencer- port in sufficient number to give a morainic aspect to the surface. From Adams Basin, 2 miles west of Spencerport, a morainic spur extends north nearly 2 miles, occupying a width of about a mile, but the moraine presents a definite east-west ridge opposite the south end of this spur, which passes about one-half mile south of Adams Basin and Spencer- port. There are drift knolls around Spencerport and for a mile or more east and north, but the moraine takes a southeastward course into Gates Township, its crest passing just south of West Gates and crossing the main line of the New York Central Railroad a mile southwest of Gates. It con- tinues south of east to the Genesee River in the south part of Rochester, upon crossing which it connects directly with the west end of the Pinnacle Hills ridge. The Pinnacle Hills ridge is thought by Fairchild to be a marginal moraine, but to the writer it appears more like a spur extending back from the inner border of the moraine. A low till ridge, which leads from its western end southward toward Ridgeland, is thought to mark the continua- tion of the Albion moraine. As this lies beyond the field allotted for inves- tigation, its course was not traced farther than Ridgeland. The relation of strie to this ridge is discussed farther on (p. 709). ALBION MORAINE. 703 RANGE IN ALTITUDE. The altitude of the crest of the moraine is only about 540 feet at the Erie Canal west of Knowlesville, while the altitude of knolls farther west in the northern part of the Medina quadrangle is from 540 to 550 feet. The altitude gradually increases eastward, the 600-foot contour being reached in the western part of Albion Township and the 620-foot contour 2 miles southwest of Albion. The cemetery hill east of Albion rises above the 680-foot contour, but neighboring portions of the crest are scarcely 640 feet, and it stands near the 640-foot contour for several miles to the east. About 3 miles southwest of Brockport the crest rises above the 660-foot - contour, and immediately south of the village it passes the 680-foot con- tour. A knoll here appears, which rises above the 720-foot contour, but the general elevation for a mile is about 680 feet. Between Brockport and Spencerport the altitude decreases to about 600 feet, and from that village southeastward into Gates Township only the prominent knolls rise above that contour. At the crossing of the main line of the New York Central Railroad southwest of Gates it is barely 580 feet, and few points from there eastward to the Buffalo, Rochester and Pittsburg Railroad rise to this contour, while at the bluffs of the Genesee the altitude is only about 560 feet, and from the river southward to Ridgeland it is between 560 and 580 feet. The Pinnacle Hills ridge varies greatly in altitude, its northeastern end at Brighton being barely 500 feet, while the highest point rises above the 740-foot contour. Much of the crest stands above the 600-foot contour. Between Albion and Brockport, where the crest of the moraine is highest, morainic knolls and ridges abound along the face of the Niagara escarpment down about to the level of the Erie Canal, 510 feet, but are rare north of the canal except in the spur near Adams Basin, where they extend about 2 miles north of the canal. The highest points on this spur are about 560 feet and the lowest about 460 feet. TOPOGRAPHY. The main ridge throughout much of its course has an abrupt outer border relief of 20 to 30 feet, and is more nearly continuous than any ridges in neighboring moraines. There are, aside from the large knolls which occasionally appear along the crest, numerous small knolls and gentle swells alony the crest and on the slopes. The knolls and ridges which lie 704 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. north of the main ridge are ordinarily but 10 to 20 feet in height, and the ridging is far less conspicuous than in the main ridge. The sharply ridged parts of this inner border are confined chiefly to the esker near Holley, the spur near Adams Basin, and the Pinnacle Hills ridge in Rochester. : The Holley esker sets in about a mile southwest of that village and extends southwestward to within one-half mile of Clarendon, its length being about 14 miles. It is a nearly continuous ridge, though it varies greatly in height, there being hummocks on it. One of these hummocks rises 40 feet above the adjacent parts of the ridge, while others rise 15 feet or more. The ridge is in places very sharp, in one place its width being only 30 or 40 yards and its height 20 to 30 feet. Along each side of the ridge gravelly knolls abound, which rise 10 to 20 feet above the marshy tract in which the esker lies. These knolls also extend around the southern end of the ridge, being numerous at Clarendon and for a short distance south and east of the village. The spur near Adams Basin does not carry a definite esker ridge, but consists of irregular-shaped knolls, which are often grouped into small clusters. The intricacy of contours is only faintly portrayed on the topo- graphic map (Pl. IIT). The Pinnacle Hills ridge, which received the attention of many geolo- gists attending the Rochester Meeting of the Association for Advancement of Science, in 1892, has since been described by Upham? and by Fairchild.’ With a width of but one-eighth to one-half mile, including slopes, and a height of 50 to 240 feet, it constitutes a very conspicuous drift feature. It does not present the form of a typical esker, though it was put in this category by Upham. Its topography is more like that of a very sharp moraine, and the name kame-moraine given by Fairchild seems highly applicable. The following description of the topography is taken from Fairchild’s paper just cited: The Pinnacle Hills extend from the village of Brighton to the Genesee River, a distance of 4 miles, with a general direction of west 15° south. The belt of hills has a linear form with a distinct curvature of large radius, the convexity facing south- ward. The range, however, is not continuous or uniform, but consists of groups of 1Kskers near Rochester, N. Y., by Warren Upham: Proc. Rochester Acad. Science, Vol. II, 1893, pp. 181-200. *The kame-moraine at Rochester, N. Y., by H. L. Fairchild: Am. Geologist, Vol. XVI, 1895, pp. 39-51; with map. ————————— ALBION MORAINE. 705 irreeular hills and knolls, three main divisions being easily recognized. The first large group extends from Brighton to Monroe avenue. This group is subdivided by a deep cut, the western mass being known as Cobbs Hill, with a summit height of 663 feet above tide. The sag which was cut by Monroe avenue originally had an elevation of 560 feet. The second large group lies between Monroe avenue and a sag or depression one-fourth of a mile west of South Clinton street (Pinnacle avenue). This group is the most distinct and compact, and contains the highest point in the whole range, called the *‘ Pinnacle,” which name has been extended to cover the whole series of hills. The altitude of this summit is 749 feet, or about 240 feet above the surrounding plain. The third group may be regarded as including all the western part of the hill range, which is lower than the eastern part, much broader and less definite. This includes in succession, westwardly, the knolls east of South Goodman street; Highland Park, between Goodman street and South avenue; the ‘‘ Warner tract,” lying between South and Mount Hope avenues; Mount Hope Cemetery, lying west of Mount Hope avenue; and the low point running into a bend of the Genesee River. The highest points in this area are the knoll on which is built the memorial pavilion near the reservoir, 650 feet, and the summits in the cemetery, 650 to 670 feet. The eastern portion of the range consists of a series of overlapping ridges or elongated mounds having their longest diameters parallel in general with the trend of the range. Only at the ** Pinnacle ” is the cross section a single ridge, and this part is better described as an elongated, irregular mound. The width of the belt at Cobbs Hill is but little less than one-half mile, and here the crests of the southern and northern series of ridges or mounds are but one-fourth mile apart. At South Good- man street the two series of ridges are one-eighth of a mile apart. The western third of the range, or the portion beyond South Goodman street, is very different, there being, instead of east-west ridges, a broader irregular aggregation of mounds with a larger number of inclosed basins. The crest line is very irregular, nowhere level for any distance, and varying 100 to 180 feet in height between the groups of hills. The northern slopes of the range are irregular, with spurs, and hillocks and deep ravines, and over the eastern half of the range are usually as steep as the material will rest, 25° to 30°. The southern slopes are more smooth and uniform, commonly with gentle inclination to the southern plain into which they blend. The irregularity of the hills is great in both Jongitudinal and transverse sections. The only feature of evident system is the linear arrangement of the series, taken as a whole. A striking feature which has not been sufficiently noted is the frequent occur- rence of *‘ kettle holes” and basins. A better example of mound and basin topography might not be desired than is found in Mount Hope Cemetery. Beautiful examples of ‘‘ kettle holes” are seen here; also in the Warner tract; also east of South Good- man street, and east of Cobbs Hill. The only ponds or swamps are found east of South Goodman street, where one pond occurs, lying at the base of the hills, and one large oval basin has been filled with peat to a depth of at least 6 feet. There is a small ridged and knolly drift tract on the inner border of the moraine in the west part of Rochester to which Fairchild, in the paper just MON XLI——45 706 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. cited, has applied the name “Lincoln Park kame area.” It consists of a series of low gravel and sand knolls distributed in a belt 13 miles long from north to south and less than one-half mile wide. The largest are but 20 to 30 feet in height and from 200 yards to about one-fourth mile in length. These knolls are recognized by Fairchild to be inside the frontal moraine. STRUCTURE OF THE DRIFT. The main ridge of the Albion moraine apparently contains a much larger percentage of till than is found in the moraines outside of it. It is a clayey till, thickly set with small stones, and bears a close resemblance to the ordinary till of the plains to the west of Lake Erie. Its surface is liberally strewn with bowlders and so is the inner slope of the moraine. The small knolls and ridges on the inner slope also contain much till, but the large knolls are in many instances composed chiefly of sand and gravel. Fairchild has given a detailed description of several sections in the Pinnacle Hills ridge from which it appears that the north slope and crest earry a large amount of till, but the south slope and basal portion of the ridge are composed chiefly of gravel and sand. The dip of the beds is not westward, or lengthwise of the range of hills, nor is it from the crest toward each border, as is common in eskers. In general it is southward and east of south, or across the trend line. The southward dip is found to be most pronounced in the gravels upon the north side of the range, and there is an approach to horizontality in passing toward the south flank. There are many local exceptions, but these have seemed to Fairchild to be in large part due to disturbances by ice thrust, to which should probably be added disturbances from settling of the beds. Large blocks of Lockport (Niagara) limestone abound on the surface and in the till of the Pinnacle Hills ridge. Their altitude reaches more than 200 feet above the outcrops of this limestone in the districts to the north, and yet they seem to be derived from that district within a distance of 5 miles. In the esker near Holley there are two gravel pits near its northeast end. The bedding is imperfect in the surface portion to a depth of several feet, there being earthy or clayey material commingled with sand and gravel. Below this depth the bedding is distinct, but it is variable, for the beds ALBION MORAINE. 707 arch and dip at various angles. They, however, show a tendency to slope with the surface from the crest toward each side of the ridge. A surprising feature in these gravel pits is the very large percentage of Medina sandstoue fragments. By actual count they constitute about 90 per cent of the pebbles. The sand also must contain a large amount of rock fragments of the same formation, for it has the pink tinge characteristic of the sandstone and shales. The till of this moraine occasionally presents a pink tinge because of the presence of the Medina shales, but ordinarily it has a blue cast and the coarse fragments seem to consist more largely of limestone than of sandstone. The granitic and other crystalline rocks of distant derivation do not consti- tute a prominent part of the till, but are very abundant on the surface. RELATION TO LAKE WARREN. Until this moraine has been traced farther east its relations to Lake Warren can only be conjectured. It was probably formed near the close of the existence of that lake, for the waters must have fallen to a lower level as soon as the ice sheet uncovered the Mohawk outlet. Possibly the outlet was opened and the lake level lowered before the moraine was formed. INNER BORDER PHENOMENA. Between the Albion moraine and Lake Ontario there is a plain sloping gradually toward the lake, as may be seen by Pl. III. It is traversed by the Iroquois beach, which lies 1 to 4 miles north from the inner border of the moraine, from the Genesee westward to Oak Orchard Creek. Above the level of this beach drift swells are not uncommon, but below it they are very rare. There are, however, just west of the mouth of the Genesee, a few small drumlins, standing only 50 to 75 feet above the level of Lake Ontario, or more than 100 feet below the level of the Iroquois beach. The drift is usually thin throughout this plain, a depth of 50 feet being rare. It has been noted by Gilbert’ that the divides between the drainage lines usually carry a smaller amount of drift than the sags through which the streams have their courses. This, as Gilbert announced, is a matter of some significance, in that it shows that the drainage is not controlled by ridges of drift, but instead by furrows in the rock. He considers these furrows immense glacial groves, as indicated more fully below (p. 709). 1 Bull. Geol. Soc. America, Vol. X, 1899, pp. 126-129. 708 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. In addition to the furrowing just mentioned, Gilbert has discovered an interesting dislocation of the Medina shale at Thirtymile Point, which he attributes to glacial thrust.’ GLACIAL STRIZ. Numerous observations of glacial strize have been made by the writer and by others on the Corniferous escarpment from Batavia westward, and on the Niagara escarpment from Rochester westward to the Niagara River, all of which have a bearing west of south. They vary, however, from S. 5° W. to 8. 60° W. A similar variation in trend is found in the drumlins which appear between these escarpments and which are thought to indicate the direction of ice movement. On the uplands south of the Corniferous escarpment two observations of strizee were made in western Wyoming County which bear east of south, one being 8. 20° E., and the other 8. 30° to 35° E. They are near the point of connection of the Gowanda moraine with the interlobate belt, the one with bearing 8. 20° E., being 13 miles west of North Sheldon, while the one with bearing 8S. 30° E., is 2 miles southwest of Sheldon Center. The diversity in the bearing of the strize in the low country lying between Lakes Ontario and Erie and of those on the uplands to the south, may simply indicate a difference in the direction of movement of ice in the axial and the peripheral portions. A southwestward axial movement is to be inferred from the fact that in the late stage of glaciation the ice sheet moved from the Lake Ontario into the Lake Erie basin; but the margin need not partake of this movement, for in crowding against the uplands on the south of these basins it would be liable to move in a southeastward direction. There is a possibility, however, that the striz on the uplands of Wyoming County were formed at a much earlier date than those on lower land to the north and northwest, and that at the time they were formed the ice sheet had a general southeastward movement across the lake basins, its thickness being so great that the basins then had little influence upon its course. Irving P. Bishop, of the New York survey, has brought to notice several instances of striation on the bed and bluffs of Niagara River near Buffalo, which show that the channel had nearly its present depth prior to the. close of the Glacial epoch.” A photograph of a striated ledge at the 1Loe. cit., pp. 1381-134. *Fifteenth Ann. Rept. New York Geol. Survey, 1895, pp. 325, 326, 392 GLACIAL STRIA. 709 Lehigh coal sheds, about 6 miles east of Buffalo, accompanies Bishop's report. Several acres were stripped of drift to expose the rock, which was used as a floor for the sheds. The surface, though in places slightly undulating, is well polished, and sharp grooves are numerous. Gilbert’s recent studies of glacial sculpture in western New York have brought to light numerous exposures of glaciated ledges, about fifteen of which are along the brow and face of the Niagara escarpment between Lockport and the Niagara River. Evidence has also been found that the shales to the north have been furrowed by the ice on a grand scale, the furrows being in some cases at least 40 feet in depth and hundreds of feet in width. These great furrows have a southwestward trend or bearing ‘similar to that of the strize on the hard rocks of the region. Fairchild has found, near Rochester, two sets of striz, an older, main set with a bearing 8. 40° to 60° W., and a later, light striation, hardly more than a polishing, with a bearing S. 5° to 15° W. on the west side of the Genesee, while they are slightly east of south on the east side of the river. He considers the latter set of similar age to the Albion moraine and calls attention to the fact that their direction is about perpendicular to the are of the moraine. It is not certain, however, that such a phase of striation might not accompany the production of a spur since the ice is liable to be to some extent lobed on each side of a spur and to have more or less move- ment toward it. The movement in connection with the Pinnacle Hills ridge would naturally be stronger toward the north side than toward the south, since the main body of ice stood on that side, and probably had a movement southward as well as westward. 1Bull. Geol. Soc. America, Vol. X, 1899, pp. 121-180. CREASE An EB in Sov ie THE GLACIAL LAKE MAUMEE. INTRODUCTORY. / Lake Maumee is the first and highest of a series of large, definitely outlined glacial lakes which occupied the Huron-Erie basin. This lake, as noted in the discussion of the Fort Wayne and Defiance moraines, was preceded by a few small, disconnected lakes which lay between the ice margin and the divide south of Lake Erie, and which found outlets at several points across the divide at levels somewhat higher than the Fort Wayne outlet. Lake Maumee was limited on the south and west by a land barrier, but its limits on the north and east were determined by the retreating ice sheet. The Defiance moraine marks the position which the ice sheet held during a large part of the lake’s existence (see Pl. XX). With the melting back of the ice the lake expanded its area to the limits shown in Pl. XXI. The outlet past Fort Wayne was the lowest available point on the bordering rim at the beginning of the lake’s existence, but later, the ice having melted away from another poimt equally low near Imlay, Mich., the lake for a brief time seems to have had two outlets. With the further withdrawal of the ice a still lower outlet became available, and with the change of outlet and lowering of level this lake’s history closed and that of its successor, Lake Whittlesey, had its beginning. The latter in turn was succeeded by a lake with still different outlet and lower level, and these changes were continued, as will be described in the discussion which follows. Lake Maumee will here include the uppermost two beaches of the Huron-Erie basin with the two outlets, the Fort Wayne and the Imlay, for it now appears probable that the former outlet continued in operation after the latter was opened. The beaches will be called the first Maumee and the second Maumee, these names being more readily understood than any other of the several names which have been applied. The name Lake 710 MICHIGAN MASON LAI 40 VAN BUREN 4) BERRIEN 2 CASS. 43 ST.JOSEPH 44 BRANCH 45 HILLSDALE 46 LENAWEE 4&1 MONROE INDIANA 1 LAPORTE 8 KOSCIUSKO 9 MARSHALL 10 STARKE WELLS 17 HUNTINGTON: 18 WABASH 19 MIAM( 50 RIPLEY 5] OEARBORN 52 SWITZERLAND. 53 JEFFERSON SCOTT 55 WASHINGTON 56 CLARK FLOYD 58 HARRISON | WILLIAMS {0 LORAIN L) ERIE 12 SANDUSKY 13 Woop: 14 HENRY 15 DEFIANCE 16 PAULDING. 17 PUTNAM 18 HANCOCK 22 SUMMIT 23 PORTAGE 24 MAHONING 25 COLUMBIANA 26 STARK 27 WAYNE 28 ASHLAND 29 RICHLAND: 33 VAN WERT 34 MERCER 35 AUGLAIZE 36 HARDIN 37 MARION 38 MoRRow 32 KNOX 40 HOLMES 4) COSHOCTON 42 TUSCARAWAS 43 CARROLL 44 HARRISON 45 JEFFERSON 50 DELAWARE 51 UNION S2 LOGAN 53 SHELBY 54 DARKE 55 MIAMI 56 CHAMPAIGN 57 CLARK 58 MADISON 59 FRANKLIN 60 PICKAWAY. 61 FAIRFIELD. 62 PERRY 63 MORGAN 64 NOBLE 65 MONROE 86 WASHINGTON 67 ATHENS: 68 HOCKING 69 VINTON 77 CLINTON 7B HIGHLAND 19 PIKE 80 JACKSON Bi MEIGS B2 GALLIA @3 LAWRENCE 84 SCIOTO 87 CLERMONT 88 HAMILTON KENTUCKY IDG SGN —-Owetousun— 7 36 37 NEW YORK AE SON[OCSIM SLEW PENDLETON GRANT. GALLATIN COT. FRANKLIN. SHELBY JEFFERSON ARK MONTGOMERY JEFFERSON EWS SENEC: 7 CHENANGO: CORTLAND TOMPKINS. SCHUYLER CATTARAUGUS. CHAUTAUQUA ON NORTHUMBERLAND MONTOUR COLUMBIA WASHINGTON GREENE POCAHONTAS. GREENBRIER U.S. GEOLOGICAL SURVEY ee as MONOGRAPH XLI PL. oD ae Wad MAP OF THE | FIRST LAKE MAUMEE AND CONTEMPORARY GLACIATION BY FRANK LEVERETT 1901 Bite 7 io s . SES ESR GAS SIRS ISS 22 Sy iS oly he 46 =Ias TEE YG mee aI } Scale 0 10 20 40 40 50 too Miles == So == : = 106 10 20 3040 _50 100 Kilometers Contour interval 500 feet Datum ts nean sea level LEGEND” | \ | Glacial lakes and drainage a Iee covered Previously glaciated, border incomplete east of longitude 78° Unglaciated Determined borders of glacial lakes or of ice Conjectured borders of glacial lakes or of ice a =) jo JULIUS BIEN SCO LITH NY bert sae U.S. GEOLOGICAL SURVEY MICHIGAN KENTUCKY ete wee i 5 5 Correct. 3 eters 3 ae 3 Simm 2 ee eg § Bis siete oie 3 Bron § ne 3 ker pees gat ie gine inns 12 MERRYSO iz TRIMBLE 13 Bet 12 Stonah 2 eee 13 Senay VS MOnTEADE 13 OWEN 1S uote 12 Gaon ie gener I Ropenaon 18 Tuscol 18 FLEMING 1p SAMivac lo CARTE! 33 src 29 BOYD 2 ecen 3 evmence a ae Bee Bauayere 3 gar ann % Benoa 3 aie #3 Siena 3 thw 8 Boris, 32 Prana Pe Bit an 32 Surrentson 3a inc, 3) BULLITT 32 UVINOSTON 32 SPENCER 3 Uitearon 33 tran eye 3k Gear 2m eae, fc 36 Wasimeynw 34 Slarreoueny 3 cana 33 NEWYORK Rcesthe NEWYORK | | | et eA Oy Ce 1 vinnie | JErrenson | ews Sem 3 ONEIDA 22 sateen 2 Binet 45 WILLSOALE 5 caYuo) frets sae 44 LENice + YAS 2 eels INDIANA 2 Bains 3 ine yuspome 17 -SENESEE wr, I ro isperert—3 Winaavon Pee, © 12 onan APES ae $8 18 Sees § abate 16 Sree 2 Mots Ia wadlean S yseauere 1B tunanuo 8 anne exams, 8 Serene it puben H PMIUR eee, ie 12 Sn a 1s Abas F Oeehina 13 oe 23 Sreueete 17 HUNTINGTON 27 ALLEGANY Va Gana 3 Betenttous 15 Misa 3 EANauauR 21 CARROLL o ii Sonar PENNSYLVANIA 2 Gaaer 1 ene Beton Hanne oe 5 teen tron 4 OTTER wm niooe Se brawn ahagrono moe GE crane B Linen 2 Sete 2 son Hear 3 Beate, 8 roouino 3 teeny 12 eiveran 3 Wie 1) EAERDN Sele Tet ee 12 Foness MANION, 13 Geneon 3 Uae 12 LER ap Moneys Siencen 28 anetar 13 Uoinence \ 2 mai 18 eiiten 4) Paverre 20 CLARION RES 45 Union 31 GERFENSON > AS Oey 3 deans x 45 Geearun 3 cevren WINING $3 BeMulowew 52 UNION \S Zo srown 25 NORTHUMBERLAND RY WS x : 48 JACKSON 28 NONTO! ‘ yy Seats Calulat 30 RIP 26 LWWZERNE ’ 3 Satins, 2 Mana no 52 itelana ‘53 JEFFERSON Si al cien 2 geo 3 gener HS EeNncton 3s Aeteeneny 33 Ean 3 SuS tnt uno # tte 34 Sbenser 3 iaaiison 32 FANE 3 Uxbiterox OHIO 38 GREENE E ies ; apa . A | pugaee— WESTVIRGINIA | [7 =e ENS 2 Ss [? iS pe ok j ih, TE CSin4 Heart Pas BeOS NW nee so, wat io 3 Hie ica 7 TRUMBULL 3 we geet | aekteee, § Eating He cs ie “a pote a SN MAP OF THE ERI 9 TAYLOR = < g RC : : | 12 SANOUSKY 10 HARRISON e : K ay : NS : . 13 wooo: TL DOOORIDGE - = i y ( : ; 5 eo é i : : ; i 1h MeVerng y aN 3} H 5 y -— ‘ i A tre peas 1B Beals cnefénjaines | et Re aaiee ASB S “AKI MAUMEE H é 7 3 = & < 3 ayy .) pees Gages = errs : lek | EAN | % : 1B HANCOCK 16 WiRT Zi a} ct : ks eae ie. i Ake epee {9-2 Ueno NS Se ¢ \ AND | re é | 21 MEDINA 19 Lewis , SS tht ; : | o ? a ; : Veal RR 5 Y | "MPORARY GLACIA’ zens, ae ‘ ‘\ : seiner Aire, 2 eee es | “— 25 COLUMBIANA 23 RANDOLPH gi ee a ae ee x + Hq ts reals N \ . \ FRANK LEVERETYT 26 ASHLAND 26 JACKSON $ ¥ % RI i . ~ Sy | Bata, a ee : : : Mi Giakeon |B putnan Po H hey if OY \ sa a Mat WERT ey cays \ : : ‘ . : Slt. = Mae = i S —_ eee 10H, Milometers Contour inte 5 re arval 500 feet Datancis ti sean sea level te aetoie Has 3 Mt | gial , p i ashe 1% \ ig ais ' Cha . | Ave \ ra , SS us im . LEGEND Glacial lakes and drainage j lee covered 1 Previously glaciate pder ) enst of longitude open" EN i SNS) ye NS Unglaciated 14 PREBLI i é if : ' Ss ; : S \ S . -~__—_ ster i SGASS N f= Determined borders of glacial lakes or of ice 4 eA St | Approximate borders of glacial lakes or of ice ‘i iN } Conjectured borders of glacial lakes or of ice fe AE + AB HAMILTON 85° 2 e 78° a ae AED 7 +e JUUUS BIEN SCO LITH 1 ¥ pilots Se Oe i Lee dee OUTLETS OF LAKE MAUMEE. ui Maumee was first applied in 1888 by C. R. Dryer, of the Indiana Geological Survey, in an official report on the “Geology of Allen County, Indiana,” which includes a discussion of the western ends of the beaches and the Fort Wayne outlet." FORT WAYNE OUTLET OR WABASH-ERIE CHANNEL. The former extension of lake waters to Fort Wayne was known as long ago as 1840, for Bela Hubbard makes reference to such an extension in a State report published that year. It is probable, also, that the outlet to the Wabash was recognized at that time, but the outlet seems to have received its first careful examination by Gilbert about thirty years later, during his investigation of the Maumee Valley for the Ohio Geological Survey. He called attention to it in 1871° and again in his official report published in 1873.4 The outlet was very briefly described in each pub- lication and no name was applied to it. The first name which it appears to have received in print was that applied by Dryer in his report above mentioned, where it is called the Wabash-Erie channel. This name, how- ever, seems not to have met with such favor as the name Fort Wayne outlet, which, though later introduced into the literature, has for several years been in use among geologists, and is now quite common in print. The term “Fort Wayne outlet” has the advantage also of being in harmony with the nomenclature adopted for the other (Imlay) outlet, both being from towns situated near the points where the outlets led away from the old lake, and both being termed outlets. As indicated by Gilbert, the lake which formed the upper Maumee beach discharged southwestward into the Wabash River. The outlet begins about 2 miles west of New Haven, where the north and south shores cease converging and turn westward in parallel courses to form the bluffs of the stream. On reaching the Wabash the outlet has a length of fully 80 miles, but the enlargement due to the accession of the lake waters extends down the Wabash many miles farther. The width ranges from 1 mile up to 1Sixteenth Ann. Rept. Geol. Survey Indiana, 1888, pp. 107-126. *Third Ann. Rept. of Dr. Douglas Houghton, pp. 102-111. Published as house document No. 8, Detroit, 1840. 5On certain glacial and postglacial phenomena of the Maumee Valley, by G. K. Gilbert: Am. Jour. Sci., 3d series, Vol. I, 1871, pp. 339-345; see also a brief notice in Rept. Geol. Survey Ohio, 1870, Columbus, 1871, p. 488. *Report on the surface geology of the Maumee Valley, ete. Geology of Ohio, Vol. I, 1873, pp. 590-551. 712 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. nearly 3 miles, the least width beimg m the city of Fort Wayne, where it passes through the Fort Wayne moraine, and the greatest width, 2 to 5 miles, being west of the city. The bluffs range in height from 15 or 20 feet up to about 75 feet, the highest part of the bluffs being near Aboit, at the place where the outlet cuts through the Wabash moraine. The bluffs in Fort Wayne, where the outlet crosses the Fort Wayne moraine, are scarcely 50 feet in height. The bed of the outlet in Fort Wayne stands about 755 feet above tide, or 182 feet above Lake Erie, and the head near New Haven seems to be but a foot or two higher. From Fort Wayne to Lewis’s ford, 3 miles east of Huntington, there appears to be a fall of but 11 feet, though the distance is nearly 25 miles. At this ford a ledge of limestone forms a barrier which was influential in causing the low rate of fall. Between this ledge and the junction with the Wabash River there is a fall of 45 feet in the present drainage line, Little River, and the lake outlet probably had nearly that amount of fall, for Little River has done scarcely any cutting in the bed of the outlet. The blufis of the outlet are abrupt throughout the entire distance from the head to its junction with the Wabash and far down the Wabash Valley, showing clearly the work of a vigorous stream. Parts of the bed are strewn with bowlders and cobblestones, also indicating an old scourway. The northwest part of the city of Fort Wayne stands on sucha stony part of the bed. Between Fort Wayne and the ledge at Lewis’s ford the bed is occupied by an extensive growth of peaty material, beneath which there is fine sand. This part had apparently been scoured out somewhat below its present level during the most vigorous stage of the excavation and was then filled in as the strength of the flow declined. The outlet is also partially filled near its head by a delta of sand formed at the mouth of Sixmile Creek. Dryer estimates the average height of this delta to be about 10 feet above adjacent parts of the lake bottom,’ and considers it the product of a stream that has passed from the St. Marys River Valley northward through the Sixmile Creek channel. This stream is reported to be still operative at exceptionally high stages of water in St. Marys River, though the main current passes around by Fort Wayne to the head of the Maumee River. 1Sixteenth Ann. Rept. Geol. Survey Indiana, 1888, p. 113. OUTLETS OF LAKE MAUMEE. Galley SIXMILE CREEK CHANNEL. This channel, which was brought to notice by Dryer,’ has been discussed in connection with the Fort Wayne moraine, its course being southward from New Haven to the St. Marys River, through the Fort Wayne moraine, and thence westward to the Fort Wayne outlet. It is much smaller than the Fort Wayne outlet, being only about one-fourth mile in width. Although its bottom has a level 40 to 60 feet below neighboring parts of the moraine,: its immediate banks are scarcely more than 15 feet in height. The channel is now drained northward by Sixmile Creek from within 2 miles of St. Marys River; but it seems to have been opened, or at least utilized, by waters of Lake Maumee discharging southward. The beach south of the lake turns up this channel on each side just as the north and south beaches turn westward into the Fort Wayne outlet. Furthermore, the recurved portion on the east side of Sixmile channel has been opened for gravel, and its bedding shows that it was formed by a southward-flowing stream. This line of discharge for Lake Maumee found its continuation down the St. Marys Valley but a short distance, for it left the river and passed directly west to join the Fort Wayne outlet about 6 miles southwest of Fort Wayne. The course is plainly marked by a channel about the same size as that along Sixmile Creek. This channel was probably utilized only during the highest stage of Lake Maumee, for its summit is apparently a little higher than the second beach. The deposit of sand found near the north end of the channel may, as suggested by Dryer, represent, in part at least, the delta of the St. Marys River, formed after the lake level had become lower. IMLAY OUTLET. The headward part of the Imlay outlet, as described by Taylor,” is only about one-third of a mile wide at its narrowest place, averaging somewhat less than half a mile in width, and ‘‘does not give evidence of a very rapid or powerfully flowing current, if the sediments remaining on its bottom are taken as an indication, for it is floored mainly by sandy beds of gravel and not by bowlders and cobble.” These gravel beds are found chiefly along the borders of the valley and stand 6 to 15 feet above the swamp which ‘Sixteenth Ann. Rept. Geol. Survey Indiana, 1888, p. 112. 2 Bull. Geol. Soc. America, Vol. VIII, 1897, pp. 37-39. 714 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. occupies its axis. In this narrow portion, which extends through parts of Goodland, Burnside, and North Branch townships, in Lapeer County, the banks are steep, as is also the west bank southward through Imlay Town- ship. But below the village of North Branch the width is seldom less than a mile, and there are fewer places where the bordering bank is sufficiently steep to suggest cutting by the current. Taylor argued in his paper that the narrowness of the Imlay outlet, as compared with that at Fort Wayne, seems to show that the former never carried the whole discharge from Lake Maumee, but that the Fort Wayne outlet also probably continued active. In a recent letter, however, he points out that a newly found fragment of the beach at the southwest corner of section 3 of Goodland Township overlooks the col and stands 20 to 25 feet above it. From this fact he suggests that the capacity of the narrow part of the outlet may have been largely compensated by the rather unusual depth of the water passing through it, and that there may have been after all little, if any, water left to flow out past Fort Wayne. The fact that the lower reaches of the Imlay outlet, as lately seen in Clin- ton and western Shiawassee counties, have an average width of a mile, thus comparing favorably with the width of the Fort Wayne outlet, gives some added strength to this view. Still, so far as could be made out from the faint features of the second beach near the head of the Fort Wayne outlet, it seems probable that this outlet did, in fact, continue to carry off some part of the discharge after the Imlay outlet had opened. MAUMEE BEACHES, FROM THE FORT WAYNE TO THE IMLAY OUTLET. Before a discussion of these beaches is begun a few explanatory state- ments seem necessary concerning the difficulty of discriminating between the first and second beaches. The strength of neither beach is great, except in places favorable for strong wave action. Where the lake plain inside of a beach slopes at the rate of 15 or 20 feet to the mile a well- defined ridge of wave-washed material or a cut bank may be expected, but where it becomes reduced to 10 feet or less per mile it can with difficulty be discerned, even though the surface, as stated by Gilbert, is remarkably adapted to receive the impress of the waves. In the case of the Maumee beaches conditions of slope are in places favorable for the strong develop- ment of both beaches, in places for but one, and in places for neither. As U.S. GEOLOGICAL SURVEY +09 Thy U} i“ 44 ! yy MICHIGAN MASON OCEANA MONTCALM 15 OWEN: GRATIOT 16 HARRISON SAGINAW 17 ROBERTSON N2O0G 506 RGN —SeeseuUsun— 3 5 3 te NICHOLAS KENT 26 BOURBON OTTAWA. 27 Scot FRANKLIN SHELBY EATON 30 JEFFERSON BOLLTT 3 LIVINGSTON 32 SPENCER OAKLAND 33 ANDERSON MACOMB 34 WOODFORD 35 WAYNE 35 FAYETTE CLARK 3F SkcKSON 37 MONTGOMERY 38 CALHOUN 39 KALAMAZCO Bal KACAMBZ Od NEW YORK. 41 BERRIEN JEFFERSON 2 BGbU yRNNRBN BERS Sooo ooH = > E i a 3 Zz 19 i ASS. 43 ST.JOSEPH 41 MONROE INDIANA 1 LAPORTE 2 ST.JOSEPH BOING RGN -Owosousun— * & 2 8 CHENANGO 10 STARKE 20 CORTLAND I PULASKI 21 TOMPKINS. 12 FULTON 22 SCHUYLER 13 WHITLEY 23 14 ALLEN 24 15 ADAMS z= 16 WELLS: MH 27 i) 17 HUNTINGTON WABASH CARROLL earls ENNSYLVANIA. GRANT BLACKFORD JAY RANDOLPH i 2 3 zi 8 6 BRADFORD. TIPTON. 7 SUSQUEHANNA 9 Cy 1 2 3 Ss Es Zz a MARION 14 6 17 18 9 20 21 22 24 ON 5 NORTHUMBERLAND JACKSON 26 MONTOUR, 27 COLUMBIA 29 30 31 2 33 rs SWITZERLAND 18 19 20 21 22 23 24 25 26 27 28 29 30 at 32 33 34 35 36 37 3e MOR 33 40 4 42 43 4 45 45 47 48 49 50 Si 52 53 JEFFERSON 54 55 56 57, 58 § HARRISON 36 OHIO 38 sce WEST VIRGINIA 3 LUCAS ' 4 OTTAWA 2 5 LAKE 3 6 ASHTABULA 4 7 TRUMBULL 5 8 GEAUGA 6 9 CUYAHOGA * 10 LORAIN 6 i) ERIE 9 12 SANDUSKY 10 13 OD {1 DODDRIDGE 14 HENRY 12 TYLER, 15 DEFIANCE 13 RITCHIE 16 PAULDING {4 PLEASANTS 17 PUTNAM, ts WOOD 1B HANCOCK 16 WIRT 19 SENECA 17 CALHOUN 20 HURON 18 GILMER 2) MEDINA Ig LEWIS 22 SUMMIT 20 UPSHUR 23 PORTAGE 21 BARBOUR 24 MAHONING 22 TUCKER 25 COLUMBIANA 23: RANDOLPH 26 STARK 24 27 WAYNE 25 28 ASHLAND 26 29 RICHLAND 27 30 CRAWFORD 26 31 WYANDOT 23 32 ALLEN 30 33 VAN WERT 31 34 MERCER 32 NICHOLAS 35 AUGLAIZE 33 WEBSTER 36 HARDIN 34 POCAHONTAS 37 MARION 35 GREENBRIER 38 MORROW 36 39 KNOX 37 40 HOLMES 36 4| COSHOCTON 33 42 TUSCARAWAS 43 CARROLL 60 PICKAWAY B 62 PERRY: i 4 B \ é pIpeto . . 68 HOCKING 77 CLINTON GALLIA LAWRENCE SCIOTO ADAMS. BROWN CLERMONT 88 HAMILTON on -ove Scone omt~ Sous MONOGRAPH XLI MAU MEE AT ITS GREATEST EXTENT WITH CONTEMPORARY GLACIATION BY PRANK LEVERETYT AND PRANK B. TAYLOR 1901 Seale io 0 10 20 80 40 50 100 Kilometers SS $ Contour imterval 500 feet Datum ts mean sea level NOTE Lt ts probable that Lake Maumee had a double outlet lor buta brief period. . The Imlay outlet may at the last have carried all the drainage. as the Wabash outlet did at first. The position of he south and west shores of the lake ts based upon Leveretts work and that of earlier students. everett has traced the contemporary moraine trom Girard Pas eastward to the Genesee River, beyond which tts course ts based upon Chamberlins map wthe Third Annual leport of the United States Geological Survey. The time of the change in the Genesee glactal lake from the Allegheny to the Susquehanna drainage may not have been strictly coincident with the lowering of Lake Maumee to the level of Lake Whittlesey. : The position of the twce margin in Canada and Michigan, and the course of the Intajs outlet, are based tn the main upon Taylors studies. The insitar tract within the tee field in Canada was perhaps covered by a take in tts southern part 0 10 20 30 40 50 100 Miles: —_ L a —_ it 78° HES JULIUS BIEN & CO.LITH NY LEGEND Glacial lakes and drainage Ice covered Previously glaciated.border incomplete eastof longitude7S” Unglaciated ones Determined borders of flacial lakes or of ice [ore Stell eal ae borders of ial lakes or of ice Conjectured borders of glacial lakes ot of ice i MICHIGAN 10 FRABELLA 1h MECOSTA {z HEWAYGO S HENDRICKS 33 Nonaan 38 Uoumson to SHELBY 49 Rusk 36 os 3, fantieon OHIO 1 WILLIAMS 86 BROWN 87 CLERMONT 88 HAMILTON, MONOGRAPH XLI PL.XXI PAS POT ae LAKE MAUMEE AT ITS GREATEST EXTENT WITH CONTEMPORARY GLACIATION — BY PRANK LEVERETT AND =H FRANK B. TAYLOR 100 Miles ——4 10 0 0 20 804050. too Kilometers Contour interval 500 feet Datumnis mean sea level NOTE It ts probable that Lake Maumee had a double outlet for buta brief period as the Wabash outlet did at tirst The position of Qe south and west shores of the lake is based upon Leveretts work and that ofeariver students. Leverett has traced the contemporary moraine thom Girard Pu, eastward lo the Genesee River beyond which tts course ts based upon Chamberlins map uttre Third Annual Report or the Un tted States Geological Survey: The time of the change in the Genesee glaciallake trom the Allegheny to the Susquehanna drainaye may not have been i sirictly coincident with the lowering of Lake Maumee to the | level of Lake Whittlesey. | the posttion of the tve margin in Canada and Michigan and the course of the Imlay outlet, are based tn He main upon Taylors studies The insular tract within the ice fteld in Canada was perhaps covered by a lake in tts southern part The Imlay outlet may at the last have carried all thedrainage ial JULIUS BIEN BCO.LITH HY Previously glaciated. border ete enstoflongitudeys” Determined borders of lacial lakes orof ice Approximate borders of glacial lakes or of ice Conjoctured bordors of Slacial lakes of of ice Pat fo ip BEACHES OF LAKE MAUMEE. 715 the beaches differ but a few feet in altitude (10 to 25 feet), and as topo- graphic maps of the region they traverse have not been made, it will easily be seen that some uncertainty in identification is likely to be felt at points where but one beach is present. It is now known that considerable error of identification has appeared in publications already made by the writer as well as by others. Portions of what was supposed to be the first beach have, upon further examination, proved to belong to the second beach, the first beach having been found in faint form outside of and above the level of the second beach. The first beach has also in one case been taken for the second, and this has led the writer to a serious error of interpretation in the part of the lake border in Ohio between Findlay and Cleveland.’ Rail- way altitudes have been pressed into service wherever obtainable, and these, together with a reexamination of much of the shore since the first publica- tion (in 1892), enable the writer to correct some errors and to understand more fully the difficulties of correlation. The Maumee beaches have been traced eastward from the Fort Wayne outlet to their termini on the south border of the Lake Erie Basin, as described below. They have been traced northward no farther than the Imlay outlet, m Lapeer County, Mich. On the west border of the lake only incidental notice was taken of the second beach, the writer’s attention being concentrated on the determination of the extent of the lake and the position and character of its highest shore. It was found that the border of the lake is usually marked by a cut bank or a gravelly ridge, and that the surface inside the lake border is perceptibly smoother than that outside. There are, however, a few places where the waters were too shallow to permit strong wave action, and at such places the margin can be only approximately determined. The extent of the lake is indicated in Pl. XXI, but as the scale of the map is small and the variations in the beach are of considerable interest, a somewhat detailed outline of the position and character of the beach will be given. DETAILED DESCRIPTION. At the point where the upper beach turns into the Fort Wayne outlet, - 14 miles northwest of New Haven, Ind., it stands 15 to 20 feet above the floor of the outlet and several feet above the plain back of it. It presents a 1Am. Jour. Sci., 3d series, Vol. XLIII, 1892, pp. 287, 291-296. 716 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. single strong ridge from that point northeastward about to St. Peter’s Church, 2 miles north of New Haven. It there assumes a complicated form, with three ridges more or less definite and of about the same height. The middle ridge is on the whole stronger than the outer and inner. These continue nearly 2 miles, to the western edge of Milan Township. The second beach is present much of the way to Milan Township, and stands about 15 feet lower than the first or upper beach. It is much weaker than the upper beach, probably because of the shallow depth of the lake in front of it. From western Milan Township to Maysville, a distance of 7 miles, the upper beach is rather fragmentary or disconnected, and stands only 5 to 10 feet above the lake plain on its inner border. A common feature in this part of the shore is an overlap of ridges at the point of entry of streams into the old lake, a bar having been extended southward on the east or lakeward side of nearly every stream from the point where it entered the lake. These streams enter at intervals of about a half mile, and the bars extend south so far as to cause much of the shore to be lined with them. At Maysville (Harlan post-office) a strong beach sets in, 150 to 200 yards wide and 10 or 12 feet high. It is bordered on the inner slope by a weak ridge or offshore bar, standing about 10 feet below its crest and 8 or 10 feet above the plain to the southeast. There are also some marks of wave action and a weak shore line to be seen on the tract immediately outside this strong beach, but this soon becomes merged with the main ridge upon passing east. The beach is well developed, largely as a gravel ridge, from Maysville to the State line, a distance of 8 miles, and the offshore bar is found to accompany it, for short distances, at frequent intervals. The beach is ordinarily 50 to 75 yards wide, and stands several feet above the lake plain on its inner border. It shows some overlapping at streams, but not to so marked a degree as in the district southwest of Maysville. From near the State line of Indiana and Ohio to Hicksville, Ohio, a distance of 2 miles, there is scarcely a trace of the shore, as the water was probably too shallow for wave action; but immediately back of Hicksville a cut bank appears, which is distinctly developed for several miles. In the village of Hicksville the second beach is well defined, but is not so marked a feature as the cut bank of the upper shore line. To one passing northeast from Hicksville along the Hicksville and Bryan pike the upper beach is in plain view, though at a distance of BEACHES OF LAKE MAUMEE. CAG. one-fourth to one-half mile or more from the road, the cut bank being often 15 feet or more m height. The second beach, though lying near the pike, is developed for only short distances and is difficult to trace. About 25 miles from Hicksville a gravel ridge sets in that is 60 to 80 yards or more wide and 6 to 8 feet high. This follows the Bryan pike northeast one-half mile to the Six Points Church, and seems to be the upper beach. From the church northeastward to Lost Creek there are two well- defined gravel ridges, differing a few feet in altitude, but scarcely so much as the usual difference between the first and second beaches. The upper ridge lies north of the pike much of the way to Lost Creek, while the lower lies along or near it. The pike turns north after crossing the creek and comes to the upper beach about a mile from the creek bridge. The beach is exceptionally strong for a mile or more along the east side of Lost Creek, its breadth bemg about 150 yards and its relief 15 feet or more above the plain on its inner or southeast border, and several feet above the plain on its outer border. The lower of these two ridges is poorly developed from Lost Creek to Farmers Center, but from there northward to Bryan there is a rather definite ridge, which has the altitude of the second beach. The upper beach crosses Dry Creek at its bend 3 miles southwest of Williams Center, and for nearly 2 miles above this point lies along the east side of the stream, causing it to take a southwestward course. It consists of a gravel ridge 100 to 200 yards in width and 10 to 15 feet in height. The ridge continues prominent and carries a large amount of gravel as far as Williams Center, but from there to Bryan gravel appears only in patches and the shore is mainly a cut bank. It passes about a mile west and a mile north of the court-house at Bryan, while the second beach passes through the court-house block. From Bryan the upper beach, a cut bank, bears north of east to Beaver Creek, crossing that stream just above Pulaski. The second beach, a gravel ridge, bears northeast and crosses the creek about a mile below Pulaski, after which it follows up the east side of its valley to the village. About a mile above Pulaski the upper beach takes the form of a gravel ridge and maintains it much of the way to West Unity. It stands usually 10 to 15 feet above the inner border plain, and 3 to 6 feet or more aboye the tract west of it. It passes through the north part of West Unity and has been opened extensively for gravel immediately east of the railway station. 718 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. From West Unity northeastward past Fayette into Michigan the upper beach lies but a few miles west of the Defiance moraine, and parts of that moraine rose above the lake level. It seems to have been protected to a great degree from wave action, and the beach is not so strong as farther south. Near Adrian traces of a vigorous stream, which was discharged south- ward, were found, as shown by the bedding of its gravel deposits. It pro- duced a remarkable amount of erosion considering the fact that it was flowing near the lake level. The west part of the city of Adrian stands on the scourway of this stream, its path being indicated by a level bowlder- strewn surface bordered on the west by a definite bank or bluff. Immedi- ately south of the Lake Shore and Michigan Southern Railway a deposit of gravel sets in on this old stream bed and extends for 4 miles to the southwest, or nearly to the village of Sand Creek. The stream seems to have entered Lake Maumee near this village, for southwest of Sand Creek, along the west side of the Defiance moraine there is a sandy ridge at a level corresponding to the upper beach of Lake Maumee. It appears north of Black Creek near Packer, and south of Black Creek from near Bimo to the vicinity of the State line, passing about a mile east of Morenci. It is a low ridge only 38 to 5 feet high, but is perhaps as strong as could be expected along a narrow bay. The west border of the bay can be traced easily from Sand Creek southwestward by a cut bank. At the time the stream was operating, the ice sheet seems to have occupied the Defiance moraine, so that Lake Maumee extended but little north of the Ohio-Michigan State line. The production of this moraine, however, as already indicated, occupied only a part of the time when Lake Maumee was forming its upper beach. The beach has been found farther - north on the inner border of that moraine. The southernmost point on the inner slope of the northern limb of the Defiance moraine at which the upper beach has been identified is near Fairfield, Mich., 6 miles south of Adrian, but there are probably traces of it farther south in the midst of the sand area of northern Fulton County, Ohio, for parts of that area rise 20 feet or more above the level of the upper beach of Lake Maumee. The second beach is well developed at many points both on the east and west borders of that sand area, as indicated below. About a mile southwest of Fairfield a gravel ridge sets in which leads BEACHES OF LAKE MAUMEE. 719 northeastward through the north part of the village, and which furnished the site for the Fairfield geodetic station. It is 100 yards or more in width, and stands in places 10 to 15 feet above the plain on its inner border. The second beach lies within one-fourth of a mile south of it and leads through the south part of Fairfield. It is traceable beyond the southwest terminus of the upper ridge. Both ridges are developed for a short distance from Fairfield along the inner border of the Defiance moraine, which there runs nearly west to east. About 2 miles east of Fairfield the Defiance moraine swings abruptly to the north and becomes broken up into knolls and sloughs which are wave worn only at a few exposed points. The second beach, however, lies near the border between the moraine and the plain and is better developed. The upper beach seems to be definite at but few points in the next 15 miles to the north, though more or less smoothing of the surface of knolls and slight terracing may be traced all along the inner slope of the Defiance moraine. The second beach is much better defined, and lies near the border between the moraine and the plain. In northeastern Lenawee County, between Ridgeway and Macon, two ridges appear above the Belmore which seem to differ about 15 feet in altitude. The lower is about 35 feet and the higher 50 feet, by aneroid, above the Belmore beach at Ridgeway. The lower ridge is rather weak, but the higher one is strong and is maintained distinctly for a distance of fully 3 miles. It contains a sandy gravel and stands 5 to 10 feet above border tracts. On the west side there is a swamp, covering much of sections 18 and 19, Macon Township, and extending back to the border of the moraine. This, in all probability, was covered by lake water, the ridge in that case being at the place where the water became so shallow as to cause the waves to break. This ridge terminates near the bluff of a small stream about a half mile southeast of Macon. From the north end of the swamp, near Macon, the beach continues northward, along the border of the Defiance moraine, into Washtenaw County, being largely a cut bank, though gravelly ridges appear where small streams led down from the moraine to the lake plain. The beach turns eastward in section 22, Saline Township, Washtenaw County, and passes through the central part of section 23 and north part of section 24, to Saline River, in the south part of section 13, bemg much of 720 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the way a well-defined gravel ridge. Hast from the rive: the beach con- tinues in a course north of east through York Township, traversing sections 18, 17, 16, 15, 14, 11, 12, and 1, and presenting throughout much of its course a well-defined gravel ridge 6 to 10 feet high and 50 to 100 yards or more in width. In section 12, York Township, the beach turns northward and enters Ypsilanti Township near its southwest corner. For about 3 miles it presents a well-defined sandy ridge, passing in a direct course slightly east of north to the north part of section 20, where it terminates abruptly. But another ridge sets in outside this ridge and pursues a winding course northward through the western part of Ypsilanti Township, passing near the western limits of the city of Ypsilanti and coming to Huron River in the northwest part of section 5. About a mile east of this ridge, and at a slightly lower level, there are faint ridges of sand running through the southwest part of the city and along or near Summit Street nearly to the State Normal grounds in the northwest part. On the north side of Huron River there is a promi- nent sand bar setting in at Highland Cemetery nearly opposite the ridge at the Normal grounds. This bar trends east of north about a mile and connects with a beach leading in from the west which forms the contin- uation of the western or main ridge found south of the river. This beach can be traced westward across sections 33 and 32, Superior Township, nearly to the Huron River, and to within less than a mile of the end of the beach south of the river. The Huron River does not present a definite terrace at the level of this beach. This is due perhaps to the fact that the stream for a considerable period had its discharge southward from Ann Arbor to Saline River. Possibly the diversion to the present course did not occur until after Lake Maumee began to form this beach. From the point where the bar connects with the beach in the west part of section 33, the beach takes a north-northeast course into Wayne County, passing through sections 34, 27, 22, 23, 14, and 12, Superior Township, and entering Wayne County in the northwest part of section 7, Canton Township. It consists usually of a low, gravelly ridge 3 to 6 feet in height, but there are frequent gaps where it is poorly developed or has the form of a cut bank. The beach presents simply a cut bank for several miles after crossing into Wayne County, but from section 28, Plymouth Township, northeastward to West Rouge River, near Waterford, it usually consists of a low, gravelly Eee BEACHES OF LAKE MAUMEE. (all ridge. On the east side of Rouge River there is a conspicuous delta across which low bars pass northeastward, converging into a definite beach line. At the border of the river they are spread over a space nearly one-half mile in width. The beach enters Oakland County near the southwest corner of Farm- imgton Township and takes a somewhat direct course across that township, passing through the northwestern part of Farmington village and leaving the township in the northeastern part of section 12. It usually forms a definite gravel ridge 3 to 6 feet high, and 30 to 50 yards or more in width. It les along the inner border of a sharply morainic tract. 'To the east of it there is a rapid descent to the Belmore beach, but the surface is remarkably smooth. Immediately northeast of the point where the beach leaves Farmington Township there was a bay-like extension up to and beyond the village of Franklin, and in this the beach is not clearly defined. East of Franklin the shore follows the imer border of the moraine, and is usually in the form of a cut bank, as far east as the meridian of Birmingham. The second beach runs parallel with it, scarcely one-half mile distant, and presents usually a gravel ridge. Near Birmingham there is considerable complexity caused by a till ridge and morainic hills which appear along the borders of East Rouge River. The till ridge at Birmingham is barely high enough to catch the second beach on its crest. Northeastward along the till ridge, however, it soon rises to the level of the upper beach, but the indications of wave action at that level are exceedingly faint, even where conditions seem favorable for the development of a beach. The lowering of the lake to the level of the second beach seems to have followed closely the withdrawal of the ice from this till ridge and the opening of the Imlay outlet. Indeed, it is probable that the opening of this outlet is the main cause for the lowering of the lake. The second beach from Birmingham northward to the Imlay outlet is usually a gravelly ridge. It is exceptionally strong at Romeo and in the vicinity of Almont. It lies along the inner face of the till ridge just noted, from near Birmingham to Romeo. Farther north it traverses a tract of weak and interrupted till ridges. Its course is, however, somewhat direct from Romeo past Almont to Imlay. Near Almont it lies along the crest of a small till ridge that passes just east of the village. MON XLI——46 722 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. The writer has not attempted to trace the beach beyond the Imlay outlet. That region is under investigation (season of 1900) by Taylor. The portion of the second beach which appears on the border of the Defiance moraine in northern Fulton County, Ohio, and southern Lenawee County, Mich. remains to be described. he first clear indications of the beach were noted in the vicinity of Wauseon in a cut bank about a mile south of the town. From this point the beach was traced southwest- ward along the inner face of the Defiance moraine to within a mile of the south line of Fulton County, where it was found to cross over the moraine and turn northward along its outer or west face. The poimt where it crosses the crest is about 2 miles south of Pettisville. From this point southward, as already noted, the moraine has a very smooth surface, while to the north, in the part surrounded by the second Maumee beach, it is undulatory. From the point where the beach crosses the moraine south of Pettis- ville northward to Tedrow, a distance of 8 miles, there are frequent developments of gravel ridges which have been opened extensively to obtain material for the roads. One of the gravel pits is a half mile east of Pettisville, another a mile northeast, and still others 2 to 3 miles farther north. From Tedrow northward into Michigan the beach is very indistinct, owing probably to the fact that there was only a narrow bay back of the Defiance moraine. On the east side of the moraine the beach is developed at frequent intervals as a gravelly ridge from Wauseon northward into Michigan, its course being east of north as far as Wimemeg and then nearly due north across the State line past Lyons, Ohio. It is poorly developed for 2 or 3 miles in the vicinity of Black Creek, but finds its continuation, as above noted, in the ridge that passes through the southern part of Fairfield, Mich. This beach has been extensively opened for gravel about 3 miles northeast of Wauseon, on the farm of Frank Blair, and also about a half mile south- west of Winemeg. From Winemeg northward into Michigan the beach is composed of a very sandy gravel unsuitable for road use. Summing up the features of the portion of the Maumee shore between the Fort Wayne and Imlay outlets, it may be stated that the strength of the wpper beach is on the whole decidedly greater where it lies outside the Defiance moraine (from near Fayette, Ohio, to the Fort Wayne outlet) than BEACHES OF LAKE MAUMEE. 723 along the inner border of that moraine, there being but few points in the latter situation where it attains the average development of the former. The difference in strength or in continuity was recognized by the early settlers in the location of roads. The portion outside the Defiance moraine, from West Unity, Ohio, to Fort Wayne, Ind., was largely used as a highway and known as a ‘‘ridge road,” but the portion in Michigan lying inside the moraine was utilized only for short distances, the gravel ridges being too disconnected to give the beach much advantage over border districts. The difference in strength may also be appreciated from the fact that the Maumee beaches had not attracted attention in Michigan, while the Belmore beach had been known from the early days of settlement. The courses of the Maumee shores in Michigan were in large part first determined by the writer in 1899, when he extended his studies into that region; but in Ohio and Indiana the Maumee shores were as early and as well known as the Belmore. ; : This difference in strength is not due to a more favorable situation for the development of a beach in the part outside the Defiance moraine, for the situation there, on the whole, seems less favorable, the slopes being in many places too gradual for effective wave action, a condition that seldom obtained in the part inside the Defiance moraine. The difference seems largely attributable to the greater time in which Lake Maumee washed the portion of the shore outside the Defiance moraine. VARIATION IN ALTITUDE. It has been known for some years that the shores of the glacial lakes which occupied the basins of the present Laurentian lakes have been sub- jected to a differential uplift, which causes the beaches to stand higher on the northern and eastern borders of the lake basins than on the southern and western. While uplift has probably produced the principal variation in altitude, there are variations not dependent upon deformations of the earth’s crust which should be mentioned. The lakes now occupying these basins show very little fluctuation through tidal action, the amount being but a few inches, and it is probable that the glacial lakes were not affected to any great degree. This factor may therefore be dismissed, as it would cause no perceptible variation in the altitude of the beaches. But fluctuations through variations in rainfall 724 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. amount to several feet, and such fluctuations are liable to have been still greater in the glacial lake:, though there are at present no recognized means of computing them. The present lakes show also a marked fluctuation or disturbance of level through the action of wind. Strong winds from the west have been known to drive the water from the western into the eastern end of Lake Erie, until the level at Buffalo became several feet higher than at Toledo. No doubt disturbances of this sort affected the glacial lakes, there being some evidence that the wind was from the same quarter. It is probable that the combined influence of the rainfall and the wind would give Lake Erie a variation of 12 feet and possibly 15 feet in level, and a beach is liable to be formed at the highest as well as the lowest level. The writer found the level of a well-defined storm beach at Westfield, N. Y., to be 12 feet above the ordmary low-water level of Lake Erie, and this may not represent the maximum height attained by storm beaches in other parts of the shore. In addition to these factors of disturbance, the glacial lakes seem likely to have responded to the attraction of the ice sheet and to have stood appre- ciably higher near the ice margin than at points more remote. Woodward’s computations * indicate that the deformation of the lake surface may have amounted to several inches per mile in the vicinity of the ice margin. It is therefore a matter of some importance to determine how much of the north- eastward rise is due to ice attraction. Turning now to the Maumee beaches, it is found that the upper beach stands about 775 to 780 feet above tide in the vicinity of the Fort Wayne outlet. Near the State line of Ohio and Michigan, 50 to 75 miles from the head of the outlet, several observations unite in giving the beach an altitude about 20 feet higher. The Fairfield (Mich.) geodetic station is 799 feet, while the railway stations at Fayette and West Unity, Ohio, which stand very near the level of the beach at those points, are 798 and 800 feet, respectively; but upon continuing northeastward from Fairfield, Mich., the altitude for the next 30 miles seems to become lower rather than higher. The aneroid determinations from several railway stations sustain this view, and an inspection of the profile of the Toledo and Ann Arbor Railway con- firms it. This railway profile shows the altitude to be but 790 feet where it crosses the beach, 4 miles north of Milan. The altitude of the sand bar on ‘See Bull. U. S. Geol. Survey No. 28. BEACHES OF LAKE MAUMEE. (5) Summit street, in Ypsilanti, is also 790 feet, as determined by city engineer's levels. Farther north, near Plymouth, the aneroid indicates that the altitude still remains at 790 feet. The next railway measurement is near Birming- ham, 20 miles north of Detroit and 65 miles from Fairfield, where an electric-railway survey shows it to be 809 feet. Ten miles farther north, at Rochester, an electric-railway survey gives it an altitude of 820 feet. The second beach there is 780 feet. Twenty-five miles farther north, near the Imlay outlet, the second beach has an altitude of 849 feet, as determined by Spencer from the railway station at Imlay." The marked differential uplift seems, therefore, to set in between Plymouth and Birmingham, about latitude 42° 30’. The apparent exceptional altitude near the Ohio-Michigan State line is a matter concerning which an opinion can scarcely be ventured in the present state of knowledge. Had the beach terminated there just outside the Defiance moraine some reason might be found for attributing the increase in altitude to the attraction of the ice sheet; but the fact that the beach continues farther and seems to become a little lower unsettles this view to some degree. There is need for more accurate as well as more numerous determinations of level to make certain whether the beach declines a little im passig north from Fairfield. The altitude of the neigh- boring parts of the Belmore beach may prove of service in settling the question of ice attraction. Should the Belmore beach show a corresponding exceptional altitude in the vicinity of the Ohio-Michigan line it would strongly oppose the view that ice attraction had been influential in giving the Maumee beach its altitude, and would indicate that crust warping was the cause, for ice attraction can not be supposed to have had the influence upon that part of the Belmore beach that it might have had upon this part of the Maumee, as the ice sheet had probably withdrawn about to the limits of Lake Huron and had become greatly reduced in thickness before the Belmore beach was formed; but on this beach careful measurements have not been made. Until refined measurements have been made on each of the beaches it seems hazardous to venture an opinion on this point. The second beach seems to stand about 760 to 765 feet above tide from the Fort Wayne outlet northeastward to Bryan, Ohio, and to be no higher 1Am. Jour. Sci., 3d series, Vol. XLI, 1891, p. 209; see also F. B. Taylor: Bull. Geol. Soc. America, Vol. VIII, 1897, p. 37. 726 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. in the vicinity of Wauseon and Pettisville, where it crosses the Defiance moraine; but at Fairfield, Mich., it stands only 20 to 25 feet lower than the upper beach, or about 775 feet above tide. Near Ridgeway it seems to be about 775 feet, being only 15 feet below the upper beach. At Birmingham, as already noted, it is 780 feet, or 29 feet lower than the neighboring part of the upper beach, while at Imlay it is 849 feet. THE SOUTH SHORE OF LAKE MAUMHBEE. In the examination of this shore attention was given principally to the extent and character of the upper beach. The second beach seems, however, to be developed along much of the shore. From near Cleveland eastward into Pennsylvania, as indicated, below, it appears to be the only beach of Lake Maumee, that part of the lake basin having been occupied by the ice sheet at the time the upper beach was forming. DETAILED DESCRIPTION. Along the south border of the Fort Wayne outlet east from Fort Wayne there are two ridges of sand differing a few feet in level. The lower and more fragmentary one is utilized by the Fort Wayne and Van Wert road for a part of the way between Fort Wayne and New Haven. The higher one lies a short distance south, along the base of the bluff of the outlet. The lower ridge is only 3 to 5 feet in height, but the higher one is generally 6 to 8 feet. The lower ridge appears to be low enough to connect with the second beach, but the higher one seems to be above the level of that beach. On the east side of the Sixmile channel there is a very prominent hook where the beach turns into the channel. A gravel pit exposes its structure to a depth of 17 feet. The upper 5 feet is quite sandy, but below this depth there is gravel which shows cross bedding with southward dip. The beds also dip toward each side of the ridge in anticlinal fashion. The crest of this recurved ridge stands about 25 feet above the Nickel Plate Railway station at New Haven, or 786 feet above tide. It rises a few feet above the usual altitude of the upper beach and probably stands at least 5 feet above the highest lake level. From this hook eastward the upper beach is very sandy and in places low dunes appear. Wells show the sand to have a depth of 9 to 18 feet. The ridge rises abruptly about 15 feet above the lake plain on the north, and 6 to 8 feet above a sag on the south. The sand ridge terminates near BEACHES OF LAKE MAUMEE. C20 the southeast edge of New Haven, and for 2 miles east there is a cut bank to mark the position of the shore. This bank is 10 feet or less in height, eradually decreasing in strength eastward until it fades out. A bar known as “Irish Ridge” sets in north of the point where this bank fades out and leads eastward a distance of 3 miles, from near the center of section 10 to the northwest part of section 13, Jefferson Township. It stands about as high as the upper beach, its western end, near the Nickel Plate Railroad, being 779 feet, and it seems to have in a measure protected the shore back of it from wave action. The beach reappears near a Catholic church about a mile east from where the cut bank dies out. It consists of a low gravelly ridge, standing only 3 to 5 feet above the bordering plain, and is only 30 to 40 yards in width. Near Zulu it increases in strength and stands in places 6 to 10 feet above the plain north of it. There is here a thin gravel coating on the top of a cut bank. The beach runs south to Flat Rock Creek in section 36, Jefferson Township, and there terminates abruptly. There seems to be no trace of the shore for about 2 miles east of this creek. The surface is very ‘flat and there was probably so little depth of water at the lake border that wave action was weak. The beach reappears east of Kast Flat Rock Creek, in the southeast part of section 32, Jackson Township. From there to the State line of Ohio and Indiana it consists mainly of a low cut bank 5 to 6 feet in height, gravel deposits bemg meager. In the vicinity of the State line a series of four nearly parallel, low, gravelly and sandy ridges are found which ditter but little in altitude, and were probably formed in succession from south to north at the highest lake stage, though the northern one may pertain to the second beach. The northern ridge enters Ohio in the southwest corner section of Paulding County; the southern enters Ohio 2 miles farther south, near the line of sections 6 and 7, Tully Township, Van Wert County. The two southern ridges seem to be only locally developed, but the two northern are quite persistent for several miles into Ohio. Of these two ridges the inner one is the weaker and is a few feet lower (perhaps 10 feet) than the outer or southern one. The space between the two ridges is a mile or less. The northern one is followed by the Fort Wayne and Van Wert road from the State line to a point 1$ miles north- east of Convoy. The ridge there leads eastward, while the road turns 728 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. south to the southern ridge. The northern ridge seems to die out near the line of Tully and Union townships, but the southern is well defined from near Convoy to Van Wert, and is followed by the Fort Wayne and Van Wert road. The southern ridge from the State line to Van Wert is seldom less than 50 yards and in places is 150 yards in width. It stands 5 to 10 feet or more above bordering plains and in places is sandy. The northern ridge is only 30 to 50 yards wide and is very gravelly. At Van Wert the beach is only about 5 feet Iigh and 30 yards in average width, being below its usual strength. The writer was in the city in 1891 when pipes for waterworks were being laid, and found that the beach carries a clayey gravel at the surface, beneath which, at a depth of 2 or 3 feet, clear gravel and sand set in. There are frequent and abrupt changes from sand to gravel and the beds show plainly wave action from the north. About 2 miles east from Van Wert the beach becomes exceptionally strong and continues so for 5 miles in curving from a north of east to a south of east course. It rises 6 to 10 feet above the plain north of it and is largely a cut bank. At Dog Creek and also at Little Auglaize River eravelly material brought m by the streams has been worked upon by the waves and given a regular front on the lakeward side, standing about 10 feet above the lake bottom. On the borders of Dog Creek Valley two beach ridges appear, which are separated by a space scarcely a half mile wide and which become united both to the east and west from the creek valley. They differ but little in altitude, though the south one appears to be a few feet the higher. From Little Auglaize River eastward, toward Delphos, there are two distinct beach lines, each of which is weak. The northern, which is the more continuous, is followed by the Van Wert and Delphos road; the southern leads southeastward from the Little Auglaize River, along an angling road 2 miles to the southwestern part of section 26, Washington Township, where it dies out in a plain; but east of this point two small ridges were noted, one of which crosses the Pittsburg, Fort Wayne and Chicago Railroad about a mile west of the canal, while the other lies south of it in section 26. In the vicinity of Delphos the shore is not well defined, and Jen- nines Creek does not carry such a conspicuous delta as appears on Little Auglaize River and Dog Creek. BEACHES OF LAKE MAUMEE. (29 Between Delphos and the Auglaize River there are only faint devel- opments of the two ridges, but immediately east of Auglaize River both ridges become strong. The southern or outer ridge comes to the river at the crossing of the Pittsburg, Fort Wayne and Chicago Railroad, and takes a northeastward course from there to Gomer. It is a low sandy ridge 5 or 6 feet in height and about 100 yards in width. Parallel with it on the north and about a mile distant is the second ridge, which 1s followed by the Bueyrus and Delphos road. It appears by. aneroid measurement to be about 10 feet lower than the outer ridge, and it has about the same strength. From Gomer to Columbus Grove the two ridges are well defined, though the southern is not so continuous as the northern. The northern or inner ridge leads through the business part of Columbus Grove and the outer one near the southern limits of the village. The southern ridge is poorly defined for 3 miles east of Columbus Grove, but then reappears in considerable strength and continues strong for about 2 miles to Riley Creek, coming to the creek 3 miles south of Pandora. The ridge was not found farther east, and the lake shore probably returns northward to the northern ridge at Pandora. The northern ridge leads directly to Pandora from Columbus Grove along the line of the Bucyrus and Delphos wagon road. Between Pandora and Findlay the beach is very strong as far as Benton Ridge, there bemg usually a bank 10 to 20 feet high, capped by gravel several feet in depth. From near Benton Ridge to Findlay the bank is but 6 to 10 feet high and the deposits are rather sandy. This part of the beach borders a narrow bay south of the Defiance moraine, and in view of its situation is remarkably strong. North from Findlay the Defiance moraine rises nearly 50 feet above the level of Lake Maumee, but within about 10 miles west it drops nearly to the highest lake level and continues near that level for about 10 miles farther. It is there crossed by a beach which stands at the level of the second beach, 760 or 765 feet above tide. The upper beach, which is about 15 feet higher, is apparently represented chiefly by sandy accumula- tions of irregular form, which follow the crest of the moraine eastward to the point where it rises above lake level and then pass eastward to Findlay along the south face of the moraine. The second beach is strongly developed along the south face from near Gilboa northwestward to the place where it crosses the crest 25 miles northwest of Leipsic. It contains a large amount of gravel and has been 730 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. opened for road ballast at many pomts. The gravel pits show clearly that the gravel was washed up against the moraine from the southwest. Where crossbedding occurs the dip is uniformly toward the moraine. The gravel can not, therefore, be an outwash from the moraine. The form of the beach is also in itself sufficient evidence that the gravel is a shore deposit. In the vicinity of the point where the beach crosses the crest of the moraine, and for several miles eastward along the north face of the moraine, a cut bank 10 to 15 feet high was found. This in places carries a gravel deposit which is nearly or quite up to the level of the upper beach, but the base of the bank is as low as the second beach. The course of the beach is south of east for several miles from the point where it crosses the Defiance moraine. It then swings with the moraine to a course north of east and leads through MeComb and Van Buren to Fostoria. The upper and second beaches were not clearly differ- entiated in this part of the shore, though two ridges were observed in the interval between McComb and Van Buren which appear to differ a few feet in altitude. At Van Buren there is a cut bank 12 to 15 feet high, the base of which seems to be near the level of the second beach and the top near the level of the upper beach. Two ridges were also observed west of Fostoria, the southern being near the line of the Baltimore and Ohio Railroad and the northern along a wagon road about a half mile north. These differ apparently less than 10 feet in altitude, and both lie near the level of the upper beach, 775 to 780 feet above tide. Froin Fostoria the shore bears south of east through Bascom to Tiffin. There are in places two ridges, differing at most only a few feet in altitude. Neither ridge is strong, the usual height being 3 to 5 feet. A cut bank of snnilar height occurs along part of the shore. The weakness of the ridge in this part of its course seems largely due to the direction it takes. It is found that, in general, the weakest part of this and other shores of the glacial lakes in the Exie Basin are where the shore fronts toward the northeast. From Tiffin the shore takes a northeastward course into southeastern Sandusky County, coming to the Lake Shore and Michigan Southern Rail- way about 3 miles west of Bellevue, from which point it turns eastward into Bellevue. This part of the shore is marked by a strong beach, as is usual where the shore fronts toward the northwest. To the north and northeast of Bellevue there were small islands in the —_— a ee, ee oe ee U.S. GEOLOGICAL SURVEY MONOGRAPH XLI PL. XxXil - Peachtoy \ Piccolo < RENE ACE CREAN SS / a yo 22 Sr ~\ _/Kelleys Island x x e. cy SS 580- SANDUS!) 605 Ly > “yy yy _ se MAP OF BEACHES NEAR SANDUS KY OHIO BY FRANK LEVERETT JUUWUS BIEN SCO.LITH NY. 10 MILES 1901 Scale oO 5 c SS —— ——————— = Oo Ss 10 KILOMETERS = —S= ——$——S LEGEND Area above Lake Maumee BetweenMaumee and Belmore beaches Between Belmore and Forest beaches Below Forest beach Shore deposits, beaches spits, dunes, etc. ; Glacial striae 707 Altitudes above sea level 2 a7 F 2 Ky 5 Pied * 4c , | he ade gfe ee BEACHES OF LAKE MAUMEE. | (ewe lake, one being on the line of Sandusky and Erie County about 3 miles north of Bellevue, another i to 2 miles south of Castalia, and a third about 5 miles northeast of Bellevue immediately west and south of Seyenmile House. The beaches are well developed on the east, north, and west sides of these islands, but are rather obscure on the south side. The accompany- ing map, Pl. XXII, shows the character of the topography of the region between Bellevue and Sandusky, the Belmore and Forest beaches, as well as the Maumee, bemg complicated because of the uneven surface which that region presents. The shores were irregular along the south border of Lake Maumee for about 3 miles each side of Bellevue, where the surface is rather uneven because of low rock hills and ridges. A smoother tract sets in 3 miles east of Bellevue, and the beach extends southeastward past Hunts Corners to Pontiac, in northern Peru Township. There are sand dunes as well as gravel deposits in this broken tract near Bellevue. Some of these are 15 or 20 feet in height, and they may extend in places slightly beyond the limits of the lake. Near Pontiac the shore turns eastward and crosses both branches of Huron River about a mile south of the north line of Peru Township. The course is then northeastward through the northwest part of Bronson Town- ship into Norwalk Township. The beach passes through the extreme south- eastern part of the city of Norwalk and a mile east of East Norwalk. It leaves Huron County at the northeast corner of Norwalk Township and continues northeastward through Berlinville to Berlin Heights. Thence its course is shghtly north of east past Axtel into Lorain County, about parallel with the shore of Lake Erie and distant from it scarcely 4 miles. It crosses Vermilion River about 2 miles below Birmingham and continues eastward across southern Brownhelm and Amherst townships to the west part of Elyria Township, passing about 2 miles south of North Amherst. This part of the shore from Huron River northeastward is exceptionally strong. ‘It was not only exposed to the heavy waves raised by the west winds, but carried a sufficient depth of water along the shore to prevent the waves from breaking until they had reached the beach. There is frequently a cut bank 10 to 15 feet or more in height, along or near the base of which a gravelly beach appears. In the vicinity of the Huron River there is a space of a half mile or more between the cut bank and the gravelly beach, ioe GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. but the latter seems to be of about the same height as the base of the bank. Possibly the bank alone represents the upper beach and the gravel deposits the second beach, but the difference in level appears to be less than is generally found between the two beaches. However, only aneroid deter- minations have been made, and the difference may be more than it now seems to be. For 2 or 3 three miles east of Berlin Heights there is a prominent ridge of sandy gravel standing 8 to 10 feet above the tract south of it, and still more above that on the north. This is sueceeded toward the east by a cut bank that extends about to Axtel. Along this cut bank there a remarkable number of bowlders, showing, apparently, that the till in which the bank is cut was very stony. From Axtel eastward two ridges appear which differ a few feet in level, and perhaps represent the upper and second beaches. They are found both east and west of Vermilion River, though they are more closely associated east of the river than west. Much of the shore of Lake Maumee from near Elyria to Cleveland was traced in detail by A. A. Wright, for the Ohio Geological Survey." The double phase of the shore was clearly brought out both to the west and east of Elyria. Two ridges west of Elyria differing a few feet in level lead southward to the West Branch of Black River, the inner and weaker coming to the river about 3 miles south of the Belmore beach in Elyria, aud the outer about 14 miles farther up the river. The outer ridge is well developed between the West and East branches of Black River, pass- ine Patterson Station and coming to East Black River opposite Laporte. The inner ridge does not appear between these streams, but sets in on the east blutf of East Black River. Both ridges are nearly continuous from East Black River to Rocky River. The upper is known as Butternut and the lower as Chestnut ridge. They differ 15 to 20 feet in altitude, the upper being in harmony with the upper beach to the west, about 780 to 785 feet above tide, and the lower with the second beach, 765 to 770 feet. The upper beach is double for about 3 miles northeast from Laporte, but the two members seem to be nearly identical in level. The upper beack comes to the west bluff of Rocky River near the junction of the two forks of that stream, 3 miles northwest of Berea, and follows nearly the bluff of the stream northeastward for 3 miles, when it crosses to the east side and leads eastward with a curving course convex to the north, past West Park 'Geology of Ohio, Vol. II, 1874; map opposite p. 58. BEACHES OF LAKE MAUMEE. (De Station on the Lake Shore and Michigan Southern Railway, to North Linn- dale. The second beach comes to Rocky River immediately west of West Park. Upon crossing the river it becomes a cut bank and curves around nearly concentric with the upper beach to Big Creek at North Linndale, crossing Lorain street about a half mile west of the present city limits of Cleveland. Hach of the beaches is strong from Black River to Rocky River. The upper usually presents a cut bank 5 to 10 feet high, though in places assuin- ing the form of a gravel ridge. The second beach is commonly a gravel ridge 50 to 100 yards wide and 5 to 10 feet high. The course of the electric railway from Cleveland to Elyria is such as to give an excellent view of each of these beaches from Rocky River nearly to Ridgeville. It then fol- lows the Belmore beach to Elyria. From Big Creek at North Linndale eastward to Brighton there are traces of both the Maumee beaches.’ The upper beach is ordinarily « wave- eut bench with but little gravel. It leads through the southern part of Brighton, passing near the tollgates on the Parma road and the ‘‘Town line” road. The interval between Brighton and the Cuyahoga River is so broken by ravines that the course of the upper beach was not ascertained. The second beach, after crossmg Big Creek about a mile east of North Linn- dale, is developed for a mile or more as a gravelly ridge. It then becomes a cut bank, and leads through the midst of Brighton. It leads southeastward along an angling road to the Cuyahoga River bluff near the north edge of Independence Township. Upon passing to the east side of the Cuyahoga and ascending the bluff along the ‘‘Warner road” a beach is found at the top of the bluff on the north side of a small eastern tributary, about one-fourth mile south of the present limits of the city of Cleveland. The barometer indicates that it has the altitude of the second Maumee beach. A gravel pit shows a depth of 8 or 9 feet of fine gravel. From this point the lake shore passes north- ward along the east side of Mill Creek, while the ‘Warner road” rises above the level of the upper beach. This road comes down to lake level again at its intersection with Tumey avenue, just south of Mill Creek. The city levels make the altitude 207 feet above city datum, or about 780 feet above 1The first tracing of the Maumee beaches through the city of Cleveland was by Upham, whose observations and map are presented in the Bulletin of the Geological Society of America, Vol. VII, 1896, pp. 340-345, plate 15. The writer also followed them through the city as here indicated in 1899, (34 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. tide. It appears, therefore, to be the upper beach. The lake extended no farther up Mill Creek than this road, for the creek here comes out of high country into the old lake plain. From Mill Creek the old shore passes northward near the line of the Cleveland and Pittsburg Railroad to New- burg station, where its altitude is 212 feet above city datum, or about 785 feet above tide. It continues north near the rolling mills and crosses Union street where Patton street leads north. The top of the bank there is 210 feet above city datum. The upper beach seems to be represented still farther north by sand deposits near the corner of South Woodland and Woodland Hills avenues, as the altitude there is 208 feet above city datum. Farther north, in the vicinity of the Garfield monument, there is a steep bank extending from near the level of the second beach up to a level above the upper beach. The sandy deposits along the base of this bank appar- ently belong to the second beach. The upper beach is much weaker from the terminus of the Cleveland moraine at North Linndale eastward through the city of Cleveland than it is to the west, its strength being less than: that of the second beach. This change in strength seems attributable to the longer time in which the lake held this level in the part of the shore west of the terminus of the moraine. From Cleveland eastward the presence of the upper beach is rather uncertain. There are indications of the continuation of Lake Maumee as far east as the vicinity of Girard, Pa., and the barometric determinations suggest a double shore for a part of the distance, with levels differing about as in the region to the west. But in the absence of topographic sheets or accurate levels some uncertainty is felt concerning the presence of the upper beach east of the vicinity of Cleveland. Possibly it extends no farther east than the terminus of the Euclid moraine, 10 miles east of Cleveland. Before continuing the description of the Maumee beaches to the east of Cleveland attention should be called to a prominent terrace in the east part of Cleveland, on which the Garfield monument stands, and which has been referred to by Newberry as a lake terrace.’ This prominent terrace, which stands about 250 feet above Lake Erie,? or nearly 40 feet above the ‘Geology of Ohio, Vol. I, 1878, pp. 181-183; Vol. II, 1874, pp. 59-60. *It is reported in the Geology of Ohio to be 210 to 220 feet above the-lake, but the city levels show its altitude south of the Garfield monument, at the intersection of Mayfield road with Kent road, to be 247 feet above Cleveland city datum, which is near the mean level of Lake Erie. BEACHES OF LAKE MAUMEE. (BND) highest shore of Lake Maumee, is better defined for several miles east from Cleveland than any terraces at levels corresponding with either of the shores of Lake Maumee, the width being from an eighth of a mile to nearly a half mile. This terrace is as flat as the bed of a stream, and is usually . bordered on the southeast by an abrupt bank. It may have been formed by a stream passing westward between the ice margin and the escarpment before the ice sheet had withdrawn from the foot of the escarpment. It has not, however, been examined with sufficient care to justify a positive interpretation of such an origin. For some miles east from the east part of Cleveland the escarpment is so abrupt that the Maumee shores are marked simply by narrow benches cut im its face at the salient parts of the escarpment. About midway between Lake View Cemetery and the post-office at East Cleveland a bench was found at what appears by aneroid to be the level of the upper Maumee beach. It is much narrower than the bench above it, just men- tioned, that leads westward past the Garfield monument. A similar narrow bench is found at about the same level south of East Cleveland. In each place there are only scattered pebbles on the bench, resting directly on the shale. Between East Cleveland and Euclid a narrow bench was found along the face of the escarpment, which by aneroid appears to be at about the level of the second Maumee beach. It carries a small amount of sand and gravel. East of Euclid there are slight developments of a bench having apparently the level of the upper beach, for it stands 40 to 50 feet above the Belmore beach. Whether it was formed by the lake is not certain. Near the line of Cuyahoga and Lake counties the escarpment loses its boldness and drift deposits of considerable thickness set in. The Belmore beach is well developed, but the Maumee shore is rather weak. A gravel ridge was found, however, near the brow of the escarpment southeast of Wickliffe, which seems to have the level of the second Maumee beach. From the Chagrin River eastward nearly to Grand River the Belmore beach is cut into the inner slope of the Euclid moraine, and in places has a bank 20 to 40 feet high, but the Matimee shore is very weak and fragmen- tary, though the moraine rises high enough to catch it. East of Grand River from near Madison to the vicinity of Saybrook a distinct beach is found above the Belmore, having apparently the level of 736 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the second Maumee beach. It is finely developed at a cemetery a half mile south of Madison and seems to be about 25 feet higher than the Belmore beach. The beach here is 100 to 150 yards wide and stands nearly 10 feet above the plain north of it. It has been opened for gravel to a depth of 10 feet. A mile farther east it presents a cut bank nearly 10 feet in height, but from the vicinity of Unionville nearly to Saybrook there is usually a gravelly ridge 3 to 6 feet or more im height. For 5 miles east from Madison it stands but one-fourth to one-half mile south of the Belmore beach. The courses of the beaches there diverge, until near the corners of Geneva, Saybrook, Harpersfield, and Austinburg town- ships the Maumee shore is a mile south of the Belmore beach. From these township corners toward Saybrook they converge and become united in a single prominent bank south of that village. : From Saybrook to Ashtabula the bank is 20 to 30 feet or more in height. Its base is followed by the Belmore beach, while its top stands near the level of the second Maumee beach. here are sandy deposits along the brow, which may perhaps represent the second Maumee beach. Sand deposits were found, however, near the standpipe of the Ashtabula waterworks at a higher altitude than the second Maumee beach, the altitude of the standpipe, as given by levels at the city engineer’s office, being 216 feet above the zero of the Government gauge at Ashtabula harbor, and the crest of the sand ridge near it, 24 feet higher, or about 790 feet above tide. his altitude is in harmony with that of the upper Maumee shore, but is about 20 feet above the second Maumee beach of that region. Whether it should be taken as an indication that Lake Maumee extended to this point at its upper stage is not clear. Being composed entirely of sand, there is a possibility that it was formed by wind action, in which case it may stand considerably above the lake level. East of Ashtabula Creek the Belmore beach is finely developed south of the Nickel Plate Railroad at an altitude of 170 to 175 feet above Lake Krie. South of it there appears to be wave cutting on the inner slope of the Ashtabula moraine at about 195 feet above Lake Erie, or 765 to 770 feet above tide. About midway between Ashtabula and Kingsville sand knolls set in at a level 190 to 200 feet or more above Lake Erie and con- tinue eastward to Kingsville. They are 10 to 30 feet high and cap the highest points on the moraine. Near Kingsville a well-defined gravelly BEACHES OF LAKE MAUMEE. 737 beach appears at the north border of the sand, at the level of the second Maumee beach, about 190 feet above Lake Erie. The sand knolls may have been drifted back from this beach by the wind, though it is barely possible that they may represent the upper stage of Lake Maumee, whose level they reach. In this connection it may be remarked that whether or not Lake Maumee reached this far east at its highest stage, the streams and small lakes held between the ice margin and the escarpment to the south are likely to have stood about as high as the upper beach, and these may be responsible for some of the sand deposits. The gravel beach has been opened for road material in a field north of the Kingsville school building. It extends as a well-defined gravel ridge for about 14 miles west from Con- neaut Creek at Kingsville. Upon crossing Conneaut Creek one finds the sec- ond Maumee beach at intervals on the inner face of the Ashtabula moraine, between there and the Ohio-Pennsylvania line. It is usually simply a wave- washed surface without a definite ridge, but occasionally a gravel ridge appears. Such a ridge was noted 3 miles west of the State line, but it is there developed for a distance of only about 100 yards along the brow of a eut bank which extends down to the level of the Belmore beach. A smooth surface, apparently wave washed, extends back in that vicinity 100 to 200 yards or more from the brow of this cut bank. A more prominent ridge was developed for a distance of about one-half mile in the vicinity of the State line. Here also it is at the top of a cut bank back of the Belmore beach. Its altitude as shown by the Girard topographic sheet is above 760 feet. By aneroid it is 25 to 30 feet above the Belmore beach, or 770 to 775 feet above tide. The grading of the State line wagon road has exposed the Maumee beach to a depth of 7 or 8 feet. The beach rises 5 to 6 feet above a sag back of it, but within 100 yards south the Ashtabula moraine sets in and rises above the level of the bank. From the Ohio-Pennsylvania line this gravel beach extends east about one-fourth of a mile. Sandy knolls and ridges then set in, which continue east about a mile along or near the brow of a cut bank back of the Belmore beach. They are 10 to 20 feet high and are confined to a strip a half mile or less in width. The bank seems to be continued past West Springfield station in low sandy ridges, some of which, just north of the station, have been opened for molders’ sand. The altitude here is 777 feet. From West Springfield eastward to Girard this beach is more fragmen- MON XLI——47 738 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. tary than to the west. There are, however, low gravelly ridges in the vicinity of Cross station which seem to mark its continuation, and a gravel deposit on the west bluff of Elk Creek opposite Girard seems also to belong to this beach. From Girard eastward the writer was accompanied by F. B. Taylor in a search for the second Maumee beach. There appeared to us to have been some wave action in the southeastern part of Girard at the inner border of a moraine, but from that point to Fairview beach phenomena, if present, are very obscure. At Fairview there is a gravel deposit at about 770 feet which is apparently a delta formed by Trout Run. It is immedi- ately back of the Belmore beach and yet stands 25 to 30 feet above it. It may have been formed: in connection with the Maumee beach, but of this some uncertainty was felt. This uncertainty increased as we passed east- ward to Swanville, for the morainic knolls there extend down to the border of the Belmore beach, and so far as we could detect show no traces of wave action at a level corresponding to the Maumee beach. Nor did we find any- thing suggesting wave action above the Belmore beach between there and Erie. In the southwestern part of Erie, however, is a plain south of the waterworks reservoir at the right altitude for the Maumee beach, where there are traces of water action, either by waves or by a current. There is not a well-defined beach, but a flat tract which leads westward from Mill Creek to Cascade Creek has a definite south border rising in places like a bank. It seems to us not unlikely that glacial waters may have discharged westward through this flat tract while the ice sheet was occupying a range of drift knolls on which the reservoir stands. We certainly should not cite this place as a clear indication of the presence of Lake Maumee. Continuing eastward into New York we were unable to find any defi- nite shore line above the Belmore beach. There were a few places where the drift surface seemed to have been subjected to leveling by water action, but these appear at various altitudes and are chiefly above the level which Lake Maumee would have reached. They seem better explained as the work of water escaping along the ice front while it was still closely bordering the escarpment. The shore of Lake Maumee appears therefore to terminate between Girard and Erie, Pa., and it is doubtful if the lake had even a transient extension farther east. By the time the ice sheet had withdrawn beyond Erie the water had probably fallen to the level of the Belmore beach, and Lake Whittlesey had succeeded Lake Maumee. BEACHES OF LAKE MAUMEE. 739 VARIATIONS IN ALTITUDE. There appears to have been very little warping of the south shore of Lake Maumee west of the Ohio-Pennsylvania line. The slight variations displayed by each of its beaches are no greater than may be found along the present shore of Lake Erie; but near the Ohio-Pennsylvania line a differential uplift had caused the beaches to increase perceptibly in altitude in passing eastward. ‘This, however, affects only the second beach of Lake Maumee, and that for but a few miles. The discussion of the uplift may therefore be taken up to better advantage in connection with the beaches of Lake Whittlesey and Lake Warren. The upper beach of Lake Maumee stands about 775 to 785 feet above tide throughout its course from Fort Wayne to Cleveland. The second beach stands about 765 feet above tide in the same interval, but rises about 10 feet between Cleveland and the Ohio-Pennsylvania line, and attains near its terminus in northwestern Pennsylvania an altitude of about 780 feet. RELATION TO THE ICE SHEET. The dwindling and disappearance of the beaches of Lake Maumee in passing from northeastern Ohio into northwestern Pennsylvania, taken in connection with the fact that the ice sheet withdrew in that direction, makes it practically certain that the eastern limits of the lake were determined hy the ice sheet. It appears, also, that the presence of the ice sheet in the low places on the rim of the Erie-Huron basin in Michigan and’ of the Ontario basm in New York caused the lake to rise to the Fort Wayne and Imlay outlets. The withdrawal of the ice sheet from these low places, as indicated farther on, brought them into use as outlets and thus allowed the lake level to become lower. It is probable, also, that the Lake Escarpment morainic system was in process of formation during most of the time that Lake Maumee stood at the level of the second beach, and that the Cleveland and Defiance moraines were formed while it occupied the upper beach. The strength of the portion of the upper beach inside the Defiance moraine is about as great on the south shore as the portion outside that moraine; but on the west shore, as already indicated, the portion inside the Defiance moraine is decidedly weaker than that outside. It is not difficult to find an explanation for the strength of the portion of the south shore inside the Defiance moraine. Much of this part of the shore fronts 740 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the northwest, while outside the Defiance moraine much of the shore fronts the northeast. An examination of the beaches has shown that portions which front the northwest are uniformly stronger, other conditions being equal, than those fronting the northeast. This is true not only of the Maumee beaches but of the Belmore beach, the beaches of Lake Warren, and the beach on the present shore of Lake Erie. This seems to indicate that heavy waves were chiefly raised then, as now, by the winds from the west. In addition to this advantage of frontage toward heavy seas, the portion inside the Defiance moraine had on the whole deeper water near the shore than that outside, so that large waves were less liable to have been broken at some distance from the shore than in the district outside the moraine. CAUSE FOR TWO BEACHES. The cause for the occurrence of two beaches in connection with Lake Maumee, as already suggested, is apparently found in the opening of the Imlay outlet, which increased the capacity for discharge and produced a lower level than that which prevailed while only the Fort Wayne outlet was in operation. se ¥ eee MICHIGAN worosen— a 5 CI = z MIDLAND 10 ISABELLA UL MECOSTA 12 NEWAYGO 13 OCEANA 14 MUSKEGON 15 MONTCALM 16 GRATIOT 17 SAGINAW 18 TUSCOLA 9 SANILAG 20 ST.CLAIR 21 LAPEER 22 GENESEE 23 SHIAWASSEE 23 CLINTON 25 IONIA 2€ KENT 22 OTTAWA 28 ALLEGAN 29 BARRY 30 EATON Si INGHAM 32 UVINGSTON 33 OAKLAND 34 MACOMB 35 WAYNE 36 WASHTENAW 37 JACKSON 38 CALHOUN 39 KALAMAZOO. 40 VAN BUREN 41 BERRIEN “ASS. 43 ST.JOSEPH 45 BRANCH 45 HILLSDALE 46 LENAWEE 47 MONROE INDIANA 1 LAPORTE. 2 ST.JOSEPH 3 ELKHART B KOSCIUSKO 9 MARSHALL 10 STARKE 1s 17 HUNTINGTON 18 WABASH 19 MIAMI 0 CASS 21 CARROLL 22 HOWARD GRANT. 24 BLACKFORD JAY 26 RANDOLPH 43 JENNINGS RIPLEY 5] DEARBORN 52 SWITZERLAND 53 JEFFERSON 54 SCOTT 55 WASHINGTON 56 CLARK 57, FLOYD 58 HARRISON OHIO 1) WILLIAMS 6 ASHTABULA 7, TRUMBULL & GEAUGA 9 CUYAHOGA 10 LORAIN 1 ERLE SANDUSKY Wooo HENRY DEFIANCE PAULOING PUTNAM. HANCOCK SENECA 40 HOLMES 4{ COSHOCTON 42 TUSCARAWAS. 43 CARROLL 43 HARRISON 45 JEFFERSON 46 BELMONT 41 GUERNSEY 48 MUSKINGUM 42 LICKING 50 DELAWARE 5| UNION 52 LOGAN 53 SHELBY 54 DARKE 55 MIAMI 56 CHAMPAIGN 57 CLARK 58 MADISON 59 FRANKLIN 60 PICKAWAY 61 FAIRFIELO HIGHLAND PIKE JACKSON MEIGS. GALLIA LAWRENCE SCIOTO ADAMS: BROWN CLERMONT 68 HAMILTON KENTUCKY Renton 1 z 3 CAMPBELL 4 GREENUP: 3 Lewis & MASON 7 BRACKEN, 8B PENDLETON 9 GRANT. 0 30 JEFFERSON BULLITT 32 SPENCER: 33 ANDERSON 34 WoooroRD 35 FAYETTE HONTGOMERY NEW YORK JEFFERSON tg CHENANGO 20 CORTLAND 21 TOMPKINS PENNSYLVANIA 15 VENANGO 16 CRAWFORD =} * 5 z & MONONGALIA 7 MARION 8 PRESTON 9 TAYLOR O HARRISON \ DODDRIDGE 2 TYLER 3 RITCHIE % PLEASANTS 1s WooD 18 WIRT 17 CALHOUN 15 GILMER 19 LEWIS 20 UPSHUR 21 BARBOUR 22 TUCKER 23 RANDOLPH 24 BRAXTON 25 ROANE 26 JACKSON 27 MASON 26 CABELL 22 PUTNAM 30 KANAWHA 31 CLAY 32 NICHOLAS 33 WEBSTER 34 POCAHONTAS 35 GREENBRIER U.S. GEOLOGICAL SURVEY Stone ii 5 les I SS SS SS d ht ees, MONOGRAPH XLI lee XXIt! LAKE WHITTLESEY AT ITS GREATEST EXTENT WITH CONTEMPORARY GLACIATION BY FRANK LEVERETT AND © FRANK B. TAYLOR 1901 Seale i) 10 20 30, 40 50 100 Miles ——— = al 10 6 10 20 30 40 50 100 Kilometers a Contour interval 500 feet Datum is mean sea level NOTE The position of the south and west shores of Late Whittlesey ts based DE elt work and that of eariter students. The north or Canadian shore has been traced chiefly by JW.Spencer: The Vbly outlet and the correlative moraine onthe borders of Saguuw Bay, Lake Huron, and Lake Ontario (in Canada) have been traced by laylor. The correlative moraine west of the Genesee River in New York was traced by Leverett. Parther east the margin ts hypothetical. mao Thus stage of thesmau lakes discharging tromthe Finger Lakes to the Susquehanna may rot have been strictly corn- temporancous wihthis most expanded stage ot Luke Whittlesey = =e ee ail — 78° WAS. | JUWUS BIEN & CO LITH NY LEGEND Glacial lakes and drainage Ice covered Previously glaciated,border incomplete eastoflongitude78° Unglaciated ee Determined borders of Slacial lakes or ofice Approximate borders of ial lakes or of icé Conjectured borders of Slacial lakes or of ice wanon to 5 PLEY. BEANHORN SWITZERLAND 2 Serrenson 32 scorr o Ss WASHINGTON 33 con gets 3, WaRinioon OHIO 1 WILLIAMS EN Esky ewes BYSSESRYSBSLEPRUNSSSasas eS LAKE WH ITTLE SEY AT ITS GREATEST EXT WIth CONTEMPORARY GLACIATION ny FRANK LE INT AND FRANK hf, TAYLOK 1901 Seale __100 Milos Joo Kilomaters = Contonr interval 500 feet Datum ts mean sea level West shores olLaleWhiltlesey that of eanier whidenty. jaws been toaved chiehy hy live moraine Ora he WES OP the G by-LeverettFarthercas ‘ypothetical This Seog Z Lakes to th, temporane Joctuirod bordons of a delat lakes cn of too CaEAG PAT BR eXw hi. THE GLACIAL LAKE WHITTLESEY. INTRODUCTORY. The name Lake Whittlesey was suggested by Taylor in 1897, for the lake which formed the Belmore beach of the Erie-Huron basin. He also discovered the lake’s outlet across the “thumb” of Michigan and named it the Tyre-Ubly outlet.” He has since shortened the name to Ubly outlet. The Belmore beach was named and partially described by N. H. Winchell in 1872,° but parts of it had been mapped many years earlier. Bela Hub- bard had traced it for more than 60 miles in southeastern Michigan at the time his report to Douglas Houghton was prepared in 1840,* and he men- tioned its presence at Plymouth, York, and Ridgeway, Mich. A map in the same report, drawn by 8. W. Higgins, shows the position of the beach in Wayne County, Mich. In a report published the following year,’ Hub- bard called attention to the continuation of the mapping of this beach across Macomb into St. Clair County. At a still earlier date Whittlesey made reference to the lake ridges south of Lake Erie in an official report published for the First Ohio Geological Survey,° but it is not certain that he had attempted to trace their courses at that time. A few years later he had traced two or more of the beaches from Erie, Pa., westward past Cleveland to the Vermilion River, and noted that from that point they bear farther inland.’ This tracing seems to have included the Belmore beach. He found difficulty in accounting for the beaches, inasmuch as they occur above 1 Bull. Geol. Soe. America, Vol. VIII, 1897, p. 39. ? Loe. cit., pp. 40-41. 3 Proc. Am. Ass. Ady. Sci., Vol. X XI, 1872, pp. 177-179. *Third Ann. Rept. of Dr. Douglas Houghton, pp. 102-111. Published as house document No. 8, Detroit, 1840. 5 House document No. 27, pp. 120-122, Detroit, 1841. 6 Second Ann. Rept. Geol. Surv. of Ohio, 1838, p. 55. 7 Notes upon the drift and alluvium of Ohio and the West: Am. Jour. Sci., 2d series, Vol. V, 1848, pp- 205-217. On the natural terraces and ridges of the country bordering Lake Erie: Am. Jour. Sci., 2d series, Vol. X, 1850, pp. 31-39. On the fresh-water glacial drift of the Northwestern States: Smith- sonian Contrib., Vol. XV, 1867, 32 pages. 741 742 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the level of the ridge cut through by the Niagara River near Buffalo, and also above the divide at the head of Lake Michigan, for at that time the relation of the lakes to the ice sheet was not even dimly conceived. The Belmore beach is the ‘‘third beach” of Gilbert’s series in the Mau- mee basin,' and is the same to which Spencer applied the name Ridgeway in Michigan.? The name Belmore, however, has priority, and has also the advantage of being less liable to lead to confusion than Ridgeway. The latter name has been applied to at least thirteen towns in the United States, and there is a Ridgeway in each of the four States bordering Lake Erie. As a further disadvantage the name Ridgeway is applied to a town in New York that stands on a different beach from the one under discussion. The course of the Belmore beach had been mapped throughout much of its extent from southern Michigan through Ohio and northwestern Penn- sylvania to southwestern New York before the writer began investigations. Attention, therefore, has been given chiefly to such portions as others had not attempted. The extent of the beach in southwestern New York was worked out in company with F. B. Taylor. Taylor also assisted in tracing the beach around the part of Defiance Bay north of the Maumee River. UBLY OUTLET. This outlet for Lake Whittlesey having been discovered and brought to notice by Taylor’ and no opportunity having been afforded the writer to examine the outlet, Taylor’s discussion, both of the outlet and of neigh- boring parts of the Belmore beach, is here presented: The most northerly point of Spencer’s tracing [of the Belmore beach] is 2 miles east of Emmet, where the altitude is 770 feet. From this point 1t was followed north and then east past Spring Hill, 2 miles northeast of Avoca, where its altitude is about the same. It is a strong and well-formed beach and is easily followed to this point. At Spring Hill it culminates in a great blunt spit of gravel compounded of many beach ridges laid up one against the other. The head of the spit projects toward the north- east, is about 40 rods wide, and at its front stands about 15 feet above the flats to the east and 10 feet above those to the northwest. Two more fragments of this beach were found within 3 miles northwest from the spit, both gravelly projecting, points. Mr. Gilbert also traced this beach from Emmet to Spring Hill. North of the spit there is a stretch of 10 miles or more of very flat land on which no beach was seen. Four miles west of Crosswell a faint shore line was found along the base of high 1 Geology of Ohio, Vol. I, 1873, pp. 554, 569-570. ? Am. Jour. Sci., 3d series, Vol. XLI, 1891, pp. 204-208. $ Bull. Geol. Soc. America, Vol. VIII, 1897, pp. 39-46. OUTLETS OF LAKE WHITTLESEY. 7438 ground about a quarter of a mile north of the corner at Buel; altitude about 780 feet. Again, on the east slope of a kame-ridge, 34 miles west of Applegate, is perhaps the best developed beach seen in Black River Valley north of Spring Hill. Its altitude is about 770 feet. It is a low ridge of fine sandy gravel facing east over flats 30 to 40 feet lower and 3 to 5 miles wide. Ata point 23 miles west and 1 mile north of Apple- gate the same faint beach was found at the same height, and it was found again on a slope 6 miles west and 1 south. There is also a very faint mark at the same height on the north slope of this kame-ridge, facing north over Elk Creek and the great Black River Swamp. * * * Along Black River from Carsonville southward toward Applegate there is an extensive gravel plain 30 to 35 feet below the beach. At the cemetery, 2 miles south of Carsonville, the valley at the head of the beach is narrowed somewhat where it passes between the high moraine east of Black River and the kame- ridge which lies along the south side of Elk Creek. From the narrows the Black River Swamp extends northward over the summit to Cass River at Tyre and Ubly, a distance of 30 miles. In this stretch no beach or certain water mark was found. The Belmore beach had, therefore, to be given up without having definitely established its connection by continuous tracing with any outlet channel. The faint fragments near Buel and Applegate are the only ones found north of Spring Hill that could be supposed to belong to this beach. Nevertheless it is clearly the correlative of the Tyre-Ubly outlet described next below. The Black River Swamp passes over the col to the head of Cass River, about 2 miles east of Ubly. A low gravel bank on the west side and midchannel bars on the crossing east of Ubly indicate that the water was at least 10 or 12 feet deep on the col. This is now about 790 feet above sea level. The old water level is there- fore about 800 feet. On this crossing the swamp is nearly a mile and a half wide. The main channel passes northwest from the col to a point about a mile north of Ubly, where it becomes much narrower, scarcely more than a half mile, and makes a sharp bend to the southwest, in which direction it continues 17 miles to its terminus, about a mile east of Cass City. Ubly is on the floor of the channel, on the east side, 1 mile south of the bend. Two other smaller branch outlet channels cross cols about 2 miles east and southeast of Tyre. At this place they unite and pass thence as one channel close to Ubly on the south, and join the Ubly channel at a point a mile or more below the latter place. Tyre is about 4 miles southeast of Ubly and is also on the channel floor. Both channels possess distinct characters of water courses. The Tyre channel is a bowldery swamp for some distance above the town, and at the station there is scarcely any covering over the underlying sandstone. The strata are bare in many places and the thin soil is very gravelly and stony. The Ubly chan- nel is floored almost entirely with beds of gravel above the junction of the branches. Bowlders are numerous in some places, as on the east side a little below the bend, 1 mile north of Ubly. The gravels were observed at several places to be at least 4 or 5 feet deep. Below the bend the width of the channel mereases to three-fourths of a mile to a mile, and keeps this width to Cass City. From the junction the floor of the channel is covered with great numbers of bowlders for the most of the distance down to its lower end. ‘The bowldery floor, nearly a mile wide, is well displayed at Holbrook, about halfway down from Ubly. The floor a mile and a half east of Cass City has an altitude of about 730 feet. In its present attitude the floor descends 744 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. about 70 feet from the col east of Ubly to Cass City, about 22 miles, but the descent of the water surface was probably somewhat less. Cass City is built upon a gravel plain about 2 miles long east and west and nearly a mile wide, which from its position strongly suggests that it may be a delta of the outlet of Lake Whittlesey. Its top level is about 750 feet above sea level or 20 to 25 feet above the old channel bottom. There appeared to be a fragment of the same plain on the south side of the river also, as though the original deposit had been cut in two. ; The contemporary position of the ice front with respect to this outlet is very clearly marked. The last land-laid moraine of the Huron lobe of the ice sheet lies close to the east side of Black River all the way northward from a point 6 or 8 miles northwest of Port Huron. Where the Black River Swamp is wide the main crest of the moraine is sometimes 4 or 5 miles from the river, but it is usually half that distance or less. The moraine is usuaily dual or triple in form, with 2 or 3 crests or ridges running roughly parallel half a mile to a mile and a half apart, the western one being the highest. Toward Ubly the moraine trends northwest, and at a point about 3 miles northeast of Ubly it meets the contemporary moraine of the Saginaw lobe coming from the southwest, and the two form a sharply defined angle of 75°. The high ridges of the two moraines do not unite, but are cleft just in the angle. A small brook, the headwaters of Willow River, drains a part of the gravelly channel bed at the extreme north angle of the bend and carries its waters away north through the narrow gap to Lake Huron, near Grindstone City. This cleft probably marks the entrance of a small glacial tributary to the great outlet river flowing from the ice sheet when its front rested close by on the main moraine. The bend of the channel is exactly in the angle of the two moraines, but the narrowest point is half a mile farther west. The crest of the Saginaw moraine from the bend to Cass City is 80 to 100 feet or more above the channel floor, and the channel runs close along its foot all the way. The inner angle of the bend is held by a high, steep hill of drift, with many bowlders. It is the northwest end of a lower ridge, which seems to belong to the eastern or Huron lobe of the ice sheet. This hill has been cut away to some extent on its north and west:sides, leaving many bowlders at its base. The base of the moraine opposite is also quite steep, apparently from the same cause. The hill in the angle evidently once extended a little farther to the northwest. Southwest of Tyre morainic ridges, mostly of moderate height, trend in a general east-to-west course. One of these lying next south of the Tyre branch is high at its west end, like the one north of Ubly, and appears at one time to have stood in much the same relation to the river. It stands in the angle where the Tyre channel turns southwest into the main channel. The Tyre branch was apparently opened before the Ubly, and the former served as an outlet, while the ice front of the Huron lobe still rested on the morainic ridge which now separates the two branches. A later retreat of a mile or two by this lobe left an open space close along the ice front in the new position, and this became the Ubly branch. After the Ubly branch opened the volume of discharge by the Tyre channel must have been largely decreased, but the level of the lake was probably not lowered much, for the heads of both branches are nearly at the same level. Judging from the comparative magnitude of the moraine between the channels and the later BEACHES OF LAKE WHITTLESEY. 745 main moraine, it seems certain that the early activity of the Tyre channel must have been quite short, as compared with the later period of their combined activity. In no other instance known to the writer is the relation of a great ice dam and the outlet of the waters which it retained so close or so clearly and unmistakably shown. Ten miles north of Ubly the surface of the thumb begins a gradual descent of 200 feet to Lake Huron. The circumstances in this case are such that there can be no possible doubt as to the place of the ice front while this outlet was active. It was not over a mile or two from Ubly, and the outlet river from the col to Cass City flowed close along the foot of the ice front. This position of the outlet was a natural consequence of the fact that the ice front was retreating northward down a slope, which happened to be the lowest part of the rim of the lake. For this reason the outlet hugged the receding ice front, and changed its place as fast as lower points of escape were uncovered. By following the course of the Saginaw moraine to the southwest, curving back to the north on the west side of the valley, and the course of the Port Huron moraine to the southeast, curving back to the northeast in Ontario, we find the exact position of the great ice dam in the basins of Saginaw Bay and the south arm of Lake Huron. It only remains to locate the contemporary ice front in the eastern part of the Erie basin to know the exact boundaries of Lake Whittlesey. THE BELMORE BEACH FROM THE UBLY OUTLET TO THE MAUMEE RIVER. The writer has examined the beach no farther north than the vicinity of Romeo, Mich., but from notes furnished by Taylor its course can be outlined from Kmmet to this pot. From Romeo southward the writer has given it sufficient attention to outline much of its course from his own notes, but has received from W. H. Sherzer, of the Michigan geological survey, notes concerning its course in Washtenaw County. DISTRIBUTION. From Emmet the course is southward to the vicinity of Lenox, in northeastern Macomb County. It there curves around to a course north of west past Armada to a point about 2 miles northeast of Romeo, where it swings southward and leads through Washington to Clinton River just below Rochester. The village of Rochester stands upon a delta which was formed in connection with this beach. The beach continues in a course west of south for about 12 miles from Rochester, passing 14 miles southeast of Birmingham. It there curves abruptly westward, forming an interesting series of hooks in its curving portion and crosses to the west side of East Rouge River about 2 miles southwest of Birmingham. From this point its course is southwestward through Farmington to Plymouth, where it crosses 746 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. West Rouge River. A complicated series of bars was formed on the delta of this system opposite Plymouth and extends the beach southward a half mile or more beyond the north end of the ridge on the west side of the stream. From Plymouth the course is west of south to Huron River about 2 miles below Ypsilanti. This river has a broad terrace at Ypsilanti which harmonizes in level with the beach and was apparently formed in con- nection with it. The beach continues in a southwestward course to Saline River at York and thence past Ridgeway to Raisin River, a mile west of Lenawee Junction. From this stream its course is southward 5 or 6 miles, then southwestward about 3 miles to Black Creek near Jasper. It then bears southeastward into Ohio, entering that State about 3 miles west of Metamora. From the Ohio-Michigan line the beach continues southeastward only 3 or 4 miles. It then curves around to a southwest course and leads. through Ai and Delta to Ridgeville Corners, where the course changes to the south and the beach comes to the Maumee River about 4 miles east of Defiance. Throughout its course in Michigan it lies east of the Defiance moraine, but in northern Ohio it turns toward the moraine and rises to the crest near Ridgeville, from which point it follows the crest to the Maumee River. DESCRIPTION OF THE BEACH. The beach presents remarkable uniformity on the western shore of the lake. It is commonly a low bank, 4 to 8 feet high, with very gradual slopes which are coated with gravel. The gravel extends up to the top of the bank and gives it a relief of a foot or two above the plain back of it. There are very few places in which the beach differs markedly from this type form, and the gaps are remarkably few and small. Although a weak feature so far as dimensions are concerned, its continuity and its regularity are such as to arrest the attention of all who cross it. The deltas formed where streams entered are usually of gravelly constitution and are as strong on this west shore as in any part of the lake border, the rate of fall in the streams being rapid and much gravelly material being formed along their courses. The deltas are usually best developed back of the beach, but in places they extend out some distance into the old lake bottom. A conspicuous instance of such an extension appears along Huron River. Sherzer has BEACHES OF LAKE WHITTLESEY. 747 found a fine gravelly deposit spread out in fan shape to a distance of fully 3 miles below the point where the river crosses the beach. The distance to which this deposit reaches seems greater than the limits of transportation by the river currents. It is possible, however, that the material was extended lakeward in connection with the lowering of the lake to the next beach. VARIATIONS IN ALTITUDE. This western shore of Lake Whittlesey appears to be nearly horizontal from the Maumee River northward to Birmingham, Mich., or about to latitude 42° 30’. The altitude of the crest of the ridge is usually between 735 and 740 feet. Northward from latitude 42° 30’ the rise is very gradual as far as Armada and Lenox (about latitude 42° 50’), the altitude being between 745 and 750 feet at those points. But at latitude 43°, near Emmet, the beach is reported by Spencer to be 770 feet, and at the head of the Ubly outlet, 40 miles farther north, the old water level was found by Taylor to be near the 800-foot contour. The exceptionally rapid rise between Emmet and Lenox may not be entirely due to uplift. Taylor’s observations indicate that the ice sheet stood at that time only a few miles east from Emmet. Ice attraction may therefore be responsible for part of the rise shown by the beach. It should also be borne in mind that the levels here given are from railway surveys, and a comparison of the different surveys shows differences amounting sometimes to several feet in the altitude of a given point. THE SHORE OF DEFIANCE BAY. In his description of the Belmore beach in northwestern Ohio, Gilbert, after tracing the beach to the Maumee Valley, stated that a landlocked bay west of it stretched up the Maumee Valley,’ but he gave it no name and seems not to have determined its full limits, nor does he mention the occur- rence of a beach along its shore. ‘This beach apparently was not definitely traced until 1899, when the portion north of the Maumee was worked out by the writer in company with F. B. Taylor, and the portion south by the writer alone. The name Defiance Bay was agreed upon by Taylor and the writer as suitable for this extension of Lake Whittlesey, for the double reason that the city of Defiance stands near its deepest portion and the Defiance moraine separated it from the remainder of the lake. 1Geology of Ohio, Vol. I, 1873, p. 554. 748 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. | From the Maumee River east of Defiance the beach which was formed on the east side of Defiance Bay follows nearly the crest of the Defiance moraine for several miles to the north and south of the river, as indicated on the accompanying map, Pl. XXIV. It is not so regular and continuous as the beach formed by the lake in that vicinity, but its average strength is about as great. It was favorably situated for receiving the heavy waves raised by winds from the west, and this seems to account for its exceptional strength in that part of its course. It is very regular and con- tinuous for 4 miles north of the river, and differs but little from the lake beach to the east. It shows clearly by its bedding as well as its form that it was built by a body of water standing west of it. It rises about 6 feet above the western base and but 2 or 3 feet above the eastern. Upon entering Adams Township it soon breaks up into disjointed ridges, which are distributed over a space a mile or more in width. It then becomes regular for a few miles, in passing across western Henry County. In Henry County the lake beach turns northeastward, while the beach of the bay continues north. The crest of the Defiance moraine soon rises above the level of the beaches, and they then follow the slopes. -- The beach of Defiance Bay crosses Brush Creek south of Archbold and continues northward through the west part of that village, passing just west of the public-school building. It then turns east of north, but becomes very faint within 3 or 4 miles, and finally merges into a sandy plain that hes between the Defiance moraine and Bean Creek Valley within 6 or 8 miles of the Ohio-Michigan line. West of Bean Creek a well-defined beach was found that crosses from Fulton into Williams County about 3 miles east of West Unity, and bears southwestward across Brady Township at a distance of 1 to 2 miles west from Bean Creek. It seems to be at about the level of the Belmore beach, but it is so much stronger than the remainder of the beach as to raise a suspicion that it was not produced solely by the waves of Defiance Bay. However, no other agency can as yet be suggested. Between this bank and the Maumee beach at West Unity there is a tract of sharply undulating drift, which dies out ina plain. The cut bank also loses streneth and becomes very faint in southwestern Brady Township. Upon the disappearance of the cut bank a strip of sandy gravel sets in to mark the continuation of the shore. This in places carries low ridges 2 to 4 feet high, but has generally a nearly plane surface. The best defined U.S, GEOLOGICAL SURVEY MONOGRAPH XLI PL. XXIV LEGEND Crest of Defiance moraine outside or aboye the Belmore beach. Belmore beach Lake Whittlesey Defiance Bay SSS SS AS - we Yi Yi tly JUUUS BIEN S CO) LITH N.Y, MAP OF THE BELMORE BEACH ON THE BORDERS OF LAKE WHITTLESEY AND DEFIANCE BAY NEAR DEFIANCE, OHIO BY FRANK LEVERETT 1901 Secale 2 SMILES a a 2 a SKIFOMETERS BEACHES OF LAKE WHITTLESEY. 749 ridge noted crosses the Lake Shore and Michigan Southern Railway 34 miles east of Bryan, or about a mile west of the Springfield and Pulaski township line. This ridge continues from this point southwestward for about 2 miles to the valley of Beaver Creek, 2 miles directly east of Bryan, beyond which it is not so definitely developed. This western shore of Defiance Bay from the latitude of Bryan southward presents only patches of sand and occasional slight traces of wave cutting to show its position. The plain on which it was formed descends so gradually toward the east that there was scarcely sufficient depth of water to afford strong wave action. The delta of the Maumee is also ill defined, and apparently was spread out as a thin sandy deposit extending from near Fairport, Ind., eastward about to Cecil, Ohio, a distance by direct line of nearly 20 miles. At Cecil the plain bordering the Maumee stands only about 15 feet below the level of the beach and at Fairport scarcely 10 feet above it. The slope averages, therefore, but little more than 1 foot per mile. A peculiarity of drainage east of Fairport also seems to indicate that the delta sets in near that village. Sixmile Creek, a tributary of Auglaize River, leads away from near the south bluff of Maumee River like a distribu- tary of a delta, and it is found that a sag or shallow channel connects the river with the head of the creek. South from Maumee River the first suggestion of the position of the west shore of Defiance Bay was found near Flat Rock Creek, northeast of Payne, Ohio. A low ridge strewn with bowlders appears about 3 miles north of Payne, near the corners of sections 14, 15, 22, and 23, Harrison Township, and leads southeastward through sections 23, 24, and 25 to Flat Rock Creek, near the line of Harrison and Paulding townships, and thence to Worstville station, on the Nickel Plate Railroad. From Worstville it bears eastward along the south side of the railroad to Briceton, and there takes a course north of east and is traceable as far as section 20, Jackson Township. This ridge has a clay surface, but is known to contain some gravel, there being a pit opened in it about 2 miles northeast of Briceton. Some hesitancy is felt in referring to this as a shore feature, though it occurs at about the level of the Belmore beach and its size is no greater than the usual size of that beach. It looks quite as much like a low glacial ridge, and the large number of bowlders which it carries seems to bear out this interpretation. It stands, therefore, as a rather questionable shore line. The level at which the Belmore beach should occur was crossed at ' 750 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. many points on the west border of the bay southeastward from the end of this ridge, but evidences of strong wave action were not discovered, and but few places were found that even suggested a shore. It is possible that this part of the bay was occupied by rushes or other vegetation which protected the shore from wave action. The bay probably extended up the Auglaize River Valley to within 3 or 4 miles of Fort Jennings and up the Ottawa River beyond Kalida. There are low, sandy ridges setting in about 2 miles southeast of Kalida and passing eastward into northwestern Pleasant Township, which are thought to have been formed along or near the shore of this bay. The bay probably extended up Blanchard River 2 or 3 miles beyond Ottawa, but its depth was scarcely 10 feet at the site of that city. North and also northwest of the city there are low, sandy ridges which were probably formed by the bay. A definite beach sets in about 4 miles north of Ottawa near Brickner post-office and leads northward along or near the Napoleon wagon road to the Nickel Plate Railroad. It is there near the border of the Defiance moraine, and the Maumee beach lies but a short distance northeast of it. It is much weaker than the Maumee beach, being a ridge only 14 to 3 feet in height and a few yards in width. The course of this beach was not definitely located for 3 or 4 miles northwest from where it crosses the Nickel Plate Railroad. A faint sand ridge was found on the crest of the Defiance moraine in the north part of section 17 and south part of section 8, Liberty Township, which probably belongs to this beach. In the northwest part of Liberty Township a definite beach was found which leads from the north part of section 7 northwestward into section 1, Palmer Township. It is 3 to 6 feet high and is composed mainly of gravel. Its form is much like that of the shore of Lake Whittlesey to the north, but it faces southwest and was evidently formed from that direction. From this point northwestward to Pleasant Bend, short gravelly ndges appear at frequent intervals and there is said to have been a well-defined gravel ridge in the village, passing near the Toledo, St. Louis and Kansas City Railroad station, but it has been removed for road ballast. Gravel has also been obtained from this ridge on the farm of John Burkhardt, 2 miles southeast of Pleasant Bend. Near the line of Henry and Defiance counties, 2 miles northwest of Pleasant Bend, a strong beach sets in which leads northwestward past Ayersville to the Maumee Valley, 3 miles east of Defiance. The shore of BEACHES OF LAKE WHITTLESEY. 751 Lake Whittlesey lies only 1 to 14 miles north of it, and sandy ridges fill in part of the interval between the two beaches. In the part north of Ayersville the lake seems to have washed the eastern face, while the bay washed the western face of the ridge. But the lake subsequently built up a beach farther east, leaving the western ridge to be washed by the bay alone. ‘This interpretation is based upon the bedding of the gravel as well as the form of the ridge, large gravel pits in the western ridge north of Ayersville showing clearly that the waves came in from the east. The east and west ridges became united at the north near the Baltimore and Ohio Railroad, and from the north end a hook curves around to the west and south in such manner as to suggest that a current passed into the bay from the lake. Sand dunes are not confined to the interval between the two ridges, there being a prominent range west of the west ridge 1 to 2 miles west of Ayersville. The complexity of the shore features will be seen by reference to the map (Pl. XXIV). The altitude of the beach of Defiance Bay at Pleasant Bend is shown by the profile of the Toledo, St. Louis and Kansas City Railroad to be 742 feet, while the beach of Lake Whittlesey at New Bavaria is shown by the same railroad to be about 5 feet lower. This slight difference may prevail for some distance southeast from Pleasant Bend, for the bay beach stands very near the water parting on the moraine while the lake beach is 2 or 3 miles north of the water parting. The surface for some distance north from the crest or water parting is, however, so flat that ditching is necessary to obtain adequate drainage, and the fall can be but a very few feet between these beaches. At Archbold the Defiance Bay beach has nearly the same altitude as the Lake Shore and Michigan Southern Railway station, or about 735 feet. It is as low as the neighboring part of the lake beach. The ridge crossed by the same railway on the west side of the bay is shown by the profile to be 173 feet above Lake Erie, or very nearly 735 feet above tide. THE SOUTH SHORE OF LAKE WHITTLESEY. DISTRIBUTION. From the south bluff of the Maumee River, about 3 miles east of Defiance, a well-defined beach similar to that north of the river leads southeastward to New Bavaria, thence eastward to Ridgeland, thence south of east through Belmore and Deweyville into northwestern Hancock hays GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. County. It there curves around to a course north of east and passes into Wood County near North Baltimore. About a mile north of North Balti- more it turns eastward and passes north of Bardstown and Bloomdale and leaves Wood County about 4 miles north of Fostoria. For 3 or 4 miles in the western part of Seneca County it is ill defined on account of the presence of rock hills, but near Amsden it reappears in strength and leads northeastward past Kansas about to the county line. It there curves abruptly to a southward course and runs out at a creek valley about a mile east of Kansas. Faint traces of the shore were found near Angus and thence south- eastward along an angling road to the Pan Handle Railroad which it crosses at the township lie about 3 miles north of Tiffin. The beach then bears eastward near the township line to the Sandusky River, and after crossing the river takes a northeastward course, passing through Watson and about. 2 miles south and east of the village of Greenspring. It passes about 2 miles east of Clyde and enters Erie County 5 or 6 miles north of Bellevue. In western Erie County a bay extended back to the north edge of Bellevue, but the border is indistinctly outlined because of the shallowness of the water and the presence of small islands to the north and east. There were also islands immediately southwest of Castalia which add to the complexity (see Pl. XXII). At North Monroeville, about 6 miles east of Bellevue, the lake shore becomes reduced to a single definite ridge which leads southward into Huron County past Monroeville and there curves around to the east, cross- ing Hast Huron River about a mile south of the Lake Shore and Michigan Southern Railway. Its course is then northeastward through Norwalk and East Norwalk into Erie County. For several miles it lies near the Maumee beach and passes with that beach through the village of Berlin Heights. From Berlin Heights eastward to North Amherst it lies 1 to 2 miles north of the Maumee shore. From North Amherst it swings around southward to the city of Elyria. It leads into Elyria from the northwest, but leaves that city in a course north of east and, passing through Ridgeville and Dover, comes to Rocky River within a mile north of the Maumee shore. _ t curves around with that shore through West Cleveland and runs through the southwestern part of the city of Cleveland along Dennison avenue. Upon crossing the Cuyahoga Valley it passes northward through the BEACHES OF LAKE WHITTLESEY. 753 eastern part of Cleveland into East Cleveland and thence takes a course northeastward about parallel with the shore of Lake Erie, and distant from it but 3 to 5 miles, through the northeast part of Ohio. It lies south of the Nickel Plate and the Lake Shore and Michigan Southern railways, and is within view from one or both railways from Cleveland eastward into Pennsylvania. In Erie County, Pa., the beach continues about parallel with the shore of Lake Erie,’ passing through East Springfield and just north of Girard and Fairview, and leading through the southern part of the city of Erie and the northern part of the village of Northeast. At the Pennsylvania-New York line this beach stands between the Nickel Plate and Lake Shore railways, but soon passes to the south of the Nickel Plate and leads through the southern part of Ripley and the extreme southern edge of Westfield. It passes south of the villages touched by these railways farther east, being near the base of the escarpment. It crosses the Dunkirk and Allegheny Valley Railroad about a mile east of Sheridan and Walnut Creek, within a mile of Forestville. It then swings northward to Hanover Center and there makes an abrupt turn to the east and con- tinues in that direction to the valley of Cattaraugus Creek, which it crosses about a mile above Versailles. An extensive gravel delta known as the “Fourmile level” was formed in the Cattaraugus Valley above Versailles in connection with this lake stage. On the east side of Cattaraugus Valley there is some complexity because of islands on the border of the lake. The most prominent extends from the Indian Council House 2 miles east of Versailles northward nearly to North Collins, a distance of 3 or 4 miles. It received the strong action of the waves and protected a narrow strip of water back of it from wave action. A bar or spit extended eastward from the north end of this island, nearly shutting off the passage back of the island, as indicated in Pl. XXY. From North Collins the shore followed the base of an escarpment north- ward to Eden Center, where it swung eastward to the west fork of Eighteen- mile Creek. In crossing this valley it turned northward, passing about a mile east of Eden Valley. A small island appears about 14 miles northeast of Eden Valley, as indicated in Pl. XXV, which was separated from the mainland to the south by a narrow channel into which a prominent spit was extended from the island toward the mainland. East from this island the MON XLI——48 Tot GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. shore curves around from a northeastward to a southeastward course and comes to East Eighteenmile Creek Valley near the line of Hamburg and Boston townships. It then passes northward toward Orchard Park, crossing the Hamburg moraine immediately south and east of that village. There were small islands along the south border of the moraine (see Pl. XXYV). From Orchard Park the course was traced eastward by the writer in company with F. B, Taylor in the autumn of 1899, and the sinuosities of the shore shown in Pl. XXV were mapped in considerable detail. It will be observed that the beach follows the inner slope of the Hamburg moraine in a very winding course as far as the village of Marilla, where it appears to terminate. Its apparent terminus is south of the western end of the Marilla moraine, and, so far as examined, no trace of it was found on that moraine. This negative evidence, combined with the fact that the beach is very weak from the point where it crosses the Hamburg moraine eastward to Marilla, led us to conclude that the lake level had dropped before the ice sheet had withdrawn from the Marilla moraine. VARIATIONS IN STRENGTH. From the Maumee River southeastward as far as the Sandusky River the Belmore beach is no stronger than on the west shore of the lake, and its general appearance is quite similar to that of the west shore. The portion between Fostoria and the Sandusky River is weaker, on the whole, than any section of similar length found on the west shore of the lake, though the beach is welt defined between Amsden and Kansas, where its trend is from southwest to northeast. The weak places are found either at hilly tracts or at points where the shore faced the northeast. East of the Sandusky River the shore for about 25 miles faced the northwest, and this portion shows the effect of somewhat stronger wave action than is commonly found in the portion already described. ‘There is usually a cut bank standing 10 or 15 feet above the plain on its inner border which is in places flanked by heavy deposits of gravel. Among the hills of western Erie County the beach is very irregular in strength and far from continuous; but from North Monroeville south and east to Norwalk there is a regular and continuous ridge similar to that found on the west shore of the lake. Near Berlin Heights the shore is chiefly a U.S.GEOLOGICAL SURVEY URES SOUTHEAS BY FRANK LEVERE MONOGRAPH XLI PL. XXV LEGEND Morainic driftwith many bowlders Drift with nearly plane surface and few bowlders Outwash gravel and lines of glacial drainage Shore deposits, beaches, spits, etc Bed of Lake Whittlesey outside of Lake Warren W Yj We Bedof Lake Warren outside of Lake Erie UUUUS BIEN & CO, LITH NY U.S.GEOLOGICAL SURVEY MONOGRAPH XLI PL. XXV | Morainic driftwith many bowlers Drift with nearly plane Surface and tew bowlers Shore deposits, deaches, spits, ete Sod of Lake Whittlesey Outside of Lake Warren Bedof Lake Warren Outside of Lake Erie VUUUS BIEN BCO.LITH NY BEACHES OF LAKE WHITTLESEY. aD cut bank, but eastward from there to Elyria and thence to Cleveland it con- sists usually of a well-defined gravelly ridge similar in strength to the ridge which forms the west shore of the lake. It seldom rises more than 10 feet above the plain north of it, and is usually but 50 to 100 yards in width. In the western part of Cleveland it extends out as a spit, 15 or 20 feet high, from the prominent poimt in West Cleveland a mile or more toward the Cuyahoga River. In the eastern part of Cleveland it consists mainly of a cut bank. From Cleveland northeastward as far as the vicinity of Dunkirk, N. Y., the beach is a very conspicuous feature, often presenting a cut bank 20 to 30 feet or more in height. As this bank was cut in a plain of gradual slope the shore must have worked back in some cases a mile or more to produce so high a bank. The exceptional strength of this portion of the shore seems attributable to its frontage toward the heavy seas raised by the winds from the west. : The strength of the beach begins to wane near the western end of the Gowanda moraine south of Dunkirk. The weakness on the south side of the Cattaraugus Valley is not surprising, since that portion of the shore would be directly exposed only to the waves produced by winds from the north, and such winds are less frequent and violent than winds from the west. But the portion of the shore north of Cattaraugus Creek had a front- age directly toward the west, and yet the strength of the beach is far below that displayed by similarly exposed parts of the shore west of Dunkirk Continuing northeastward across the Hamburg moraine the shore becomes still weaker, and although fronting the northwest its strength is even inferior to that of the portions of the shore in Michigan and Ohio which front the - east and northeast. ‘The beach is commonly a ridge only 3 to 6 feet high and 50 yards or less in width. This diminution in strength, as already remarked, fits in naturally with the interpretation that the lake is of glacial age, and that the moraines between the lake escarpment system and the Marilla moraine are the correlatives of the beach. VARIATIONS IN ALTITUDE. The altitude of the beach on the south shore of Lake Whittlesey has very little variation from the Maumee River near Defiance eastward to the vicinity of Ashtabula, Ohio, a distance of 200 miles, the lowest measured 756 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. altitude being 731 feet and the highest 742 feet above tide. A part of this difference may be due to discrepancies between railway surveys and a part to the difference in the height to which the beach was built above mean lake level. These elements of error and of variation being eliminated, it is doubtful if enough difference will remain to require any crust warping. Eastward from Ashtabula, the beach is found by levels on the Girard topographic sheet to reach 746 feet at the Ohio-Pernsylvania line, 748 feet near East Springfield, Pa., and 752 feét 4 miles farther east, while levels run by Taylor show it to be 765 feet at Swanville. This gives the beach a rise of 19 feet in a distance of about 19 miles. At Erie, 10 miles farther . east, the city levels show the altitude to reach 772 feet, and at Northeast, 15 miles farther, levels run by Gilbert show the beach to be 788 feet above tide. Near the Pennsylvania-New York line, about 5 miles from North- east, the profile of the Lake Shore and Michigan Southern Railway shows the altitude to be only 785 feet, but in the next 10 miles to Chautauqua Creek, south of Westfield, the beach, as shown by the Westfield topo- graphic sheet, rises above the 800-foot contour. About 20 miles farther, near Fredonia, as shown by the Dunkirk topographic sheet, the beach rises above the 820-foot contour. Near Sheridan, 6 miles farther, Gilbert found the altitude by Locke level to be 834 feet. Six miles farther, near Han- over Center, the beach reaches the 840-foot contour. From Hanover Center to Cattaraugus Creek the course of the beach is south of east, or nearly at a right angle to the direction of uplift, and it holds a very uniform level at about 840 feet. It is very nearly 840 feet on the east side of Cattaraugus Creek, near the Indian Council House, as determined by spirit level by Fairchild from Lawton station. Four miles north, opposite North Collins, as determined by Locke level from North Collins station, it reaches 850 feet, bemg 20 feet above the railway station. Beyond this point measurements were made only with the aneroid, but these show a strong increase, the altitude southeast of Hamburg being 875 feet and near Elma station 890 feet. At the supposed terminus in Marilla the aneroid indicates an altitude of nearly 900 feet. The rise of about 150 teet between the Ohio-Pennsylvania line and Marilla, N. Y., is made in a distance by direct line of not more than 125 miles, and contrasts strikingly with the variation of less than 15 feet in the 200 miles west from the Ohio-Pennsylvania line. BEACHES OF LAKE WHITTLESEY. 757 CAUSE FOR THE LOWERING OF THE LAKE. It is probable that the lake level was lowered through the opening of lower passages than the Ubly outlet, either across or around the north end of the thumb of Michigan. Taylor has noted channels and scourways among the morainic hills north of the Ubly outlet that seem to have afforded outlets sufficiently low and capacious to have drawn down the lake level. As that region is now Gn 1901) under investigation, the precise relations will probably soon be determined. 1 Bull. Geol. Soc. America, Vol. VIII, 1897, pp. 47-48. CUEA PUB XV THE GLACIAL LAKE WARREN. INTRODUCTORY. The names Lake Warren, Warren Waters, and Warren Gulf have been applied by Spencer to the most extensive sheets of water in the Great Lakes region, and have been variously applied by other geologists. This has led to some confusion, and in order to make the application more specific Taylor has proposed to restrict the name Lake Warren to the body of water which existed when the fourth beach of Gilbert was forming. At that time the water in the Erie-Huron Basin seems to have had its greatest extent, and this meets as nearly as practicable the application made by Spencer. As this restriction of the name is a matter of some consequence, Taylor's reasons are here given:* When Dr. Spencer had traced parts of the Forest, Arkona, and Ridgeway beaches in Ontario, he named the water which made them Lake Warren, in honor of Gen. G. K. Warren, whom he regards as ‘‘the father of lacustrine geology in America.” This name was first published in Science for January 27, 1888, page 49; but in this and in all his subsequent publications relating to these beaches, Dr. Spencer had stated his belief that they are really of marine origin. Besides calling the waters that made these beaches Lake Warren, he has as frequently called them Warren Water and Warren Gulf. The current ideas of their size and origin have been diverse from the beginning, so much so as to make the application of the name rather uncertain. Dr. Spencer has always defined Lake Warren as covering the whole of the Great Lakes area, and Upham and Lawson have supposed it to cover all but Lake Ontario. The whole series of beaches has been regarded as the work of one lake at as many halts in the fall of its level. This is true in a wide sense, but there were so many elements of change as the waters fell that it seems appropriate and necessary to consider the several stages as separate lakes and give a special name toeach. The waters changed their shape, size, and level as they fell, and, what seems still more important, they changed the place of their outlet several times. The need for the restricted use of the name Lake Warren here proposed is a natural result of the progress of discovery. With the finding of outlets and terminal moraines intimately related to the beaches, the moraines marking the place of the ice barrier that held the waters up, it becomes a positive necessity to recognize the 1 Bull. Geol. Soc. America, Vol. VIII, 1897, pp. 56-57. 798 MICHIGAN Zs SHIAWASSEE 25 IONIA E 36 WASHTENAW 37 JACKSON 3 CALHOUN 39 KALAMAZOO 4O VAN BUREN 45 HILLSDALE 45 LENAWEE 47 MONROE INDIANA | LAPORTE 2 ST.JOSEPH 3 ELKHART 4 LAGRANGE 5 STEUBEN 3 MARSHALL \0 STARKE 11 PULASKI 12 FULTON 13 WHITLEY 16 WELLS. 17 HUNTINGTON 18 WABASH 19 MIAME 20 CASS 21 CARROLL 23 GRANT. 24 BLACKFORD 25 JAY 26 RANDOLPH 27 DELAWARE 28 MADISON 25 TIPTON 30 CLINTON 41 42 FAYETTE 43 UNION 44 FRANKLIN 45 DECATUR. 46 BARTHOLOMEW 54 SCOTT 55 WASHINGTON $6 CLARK 57 FLOYD 58 HARRISON OHIO 1 WILLIAMS 15 DEFIANCE 16 PAULOING. 17 PUTNAM 22 SUMMIT 35 AUGLAIZE 36 HARDIN 37 MARION 38 MORROW 35 KNOX 40 HOLMES 41 COSHOCTON 42 TUSCARAWAS 43 CARROLL 44 HARRISON 45 JEFFERSON 56 CHAMPAIGN 57 CLARK 58 MADISON 59 FRANKLIN 60 PICKAWAY. 61 FAIRFIELO 89 VINTON 70 ROSS 7) FAYETTE 72 GREENE 73 MONTGOMERY 74 PREBLE 7S BUTLER 76 WARREN 27 CLINTON 78 HIGHLAND OWN 87 CLERMONT BE HAMILTON KENTUCKY GRANT. 10 GALLATIN 11 CARROLL 12 TRIMBLE 13 OLOHAM 14 HENRY 1 OWEN HARRISON BOYD. 2) LAWRENCE 22 ELLIOTT 22 ROWAN 2a BATH 25 NICHOLAS 26 BOURBON 2B FRANKLIN ELBY gO JEFFERSON LARK 37 MONTGOMERY NEW YORK JEFFERSON SENE! ONONDAGA MADISON CHENANGO SERBERNND SSLoobONL SoG Inu bGN—oeaSousun— ALLEGANY 28 CATTARAUGUS CHAUTAUQUA, PENNSYLVANIA. NISeoseuaun— JEFFERSON CLEARFIELD CENTER UNION NORTHUMBERLAND 28 MONTOUR: COLUMBIA HARRISON DODDRIDGE TYLER: RITCHIE PLEASANTS Wooo WiRT CALHOUN GILMER LEWIS UPSHUR BARBOUR TUCKER RANDOLPH GREENBRIER 36 FAYETTE BOONE UNCOLN WAYNE .S.GEOLOGICAL SURVEY ices SON ondels Ag IW SS SS 5, ge o NY \\ SN LAKE WARREN AT ITS CREATEST EXTENT WITH ; baal CONTEMPORARY GLACIATION BY FRANK LEVERETT AND FRANK B. TAYLOR 1901 Seale 10. 20. 30. 40) 50 100 Miles —=s wo 0 10 20 30 40 50 100 Kilometers a Contour interval 500 feet Datumis mean sea level NOTE Thegreater part of the shore of Lave Warren his been traced. by eartter students. Gilbert, Spencer Fauchila, and members of eMichigan and Ohvo geological surveys. Taylors workor this shoreline has beenprincipally in Michigan and Leveretts tr Ohwo. The correlative morainetn NewYork westor Genesce River was traced byLeveretl. The position of the ie barrier | near Syracuse Wewlork, was determined byhairchiia Therelations of we and lake muargins have not been deter- mained in Canada, and the position of the te margin within the borders of Lake Huron and Lake Ontarw ts necessarily coryectiral = =!) 1 78° Te JUWUS BIEN & CO. LITH NY. Previously glaciated, border incomplete eastoflongitude7&° Unglaciated fon Determined borders of glacial lakes or of ice roximate borders of glacial lakes or of ice Conjectured borders of Slacial lakes or of ice MICHIGAN 22 rman $8 oecaTun RANTWOLOM EW OHLO bo Trane mene % 4 a8 eran” WAMAEN +} camo 18 wlan can, U_S.GEOLOGICAL SURVEY MONOGRAPH XLi_ PL.XXVI u irs 12 TRIMBLE 13 CLOMAM % Gewrooweny NEW YORK 1 surrenioN ory Ungaciatert i. if Bae i : é A : : J {Xigetic | } 1p MADISON a S g ta 2 fs & : > : . , 7 iretionite : {] Deternined borters off 1e Sunance | % % : 4 a 7 J Oe m 4 aT § Bacial lakes eof tee ? ) = - ; y : > oat f aT A pT { BUR Romenie era bw Catia gan pt Shiga : ) RSQ : : 23 cartanauaue , . e A 2 > ~ aia borctine ow tal takes OF es | Coneetured borders of Glacial lakes oe of iow SANS SYS XX N LAKE WARREN AT ITS GREATEST EXTENT " witht c sue; ot. : 5 -\isb $ se : sss S 3 ? YARIS AT was ? it 4) : i us 2 ia Ss : SS . , SS CONTEMPORARY GLACTATION 1 isoon f rds S 4 eae é Bomieet : : : . \ : my a FRANK LEVERE TT ann 3s Hoeaiores J be Cong aay tg Mt . PLS RSA 4 Cine t ie aN Naas) : : as ° ; S : FRANK TE TAYLON ¥ t lt a: 7S i t ing H i \ . NG SS . . S on Seale ee es ~ wo Mlometers nur interval 40 fret BEACHES OF LAKE WARREN. Tag new facts, and this can be done best, as it seems to the writer, by subdivision and restriction in nomenclature, as is sometimes done in the biological sciences. The whole series of lakes here described might be called the Warren lakes. This would be one way of preserving Spencer’s nomenclature, but in the writer’s opinion this use of the name would be unfortunate. A collective name ought to have some geo- graphic significance. The name Erie-Huron, which is used here, serves this purpose admirably, and the name Lake Warren may then be applied in a more restricted way to that one of the several separate lakes of the series which most closely corre- sponds to Spencer’s original idea. The Forest beach marks the widest extent of the Erie-Huron glacial waters, and was the last and most extensive lake of the series. It seems more appropriate, therefore, to call this stage Lake Warren than to apply this name to any of the higher, less extensive stages. The Lake Warren beaches as here discussed and as mapped in Pl. XXVI, include the whole of a complex series which occupy levels about 50 to 75 feet below the Belmore beach. The members of this series are more distinct from Cleveland eastward than around the western end of the Erie Basin. -Wind-drifted sand greatly confuses the shore features in the latter region. Perhaps the upper ridge, to which Spencer applied the name Arkona beach, is sufficiently distinct from those below it to justify separating it from the Lake Warren series. Taylor has considered it the product of a distinct but transient lake, and does not include it in this series. In southern Mich- igan it lies along the outer border of the same belt of sand which in Ohio constitutes Gilbert’s fourth beach, but bemg composed usually of gravelly material, it may be distinguished from the belt of clear sand which it borders. Its gravelly ingredient seems to disappear in northwestern Ohio, so that it can not well be separated from the remainder of the sand belt. The Wood- land avenue beach at Cleveland seems likely to be a continuation of the Arkona beach, and the upper member of the series from Cleveland eastward should probably also be thus considered. The upper limits of sand ridges in the district south of the western end of Lake Erie is also about at the level of the Arkona beach. The writer has examined this series of beaches at but few points in Michigan, and as they are soon to receive further study in that State, the description will extend no farther north than the Ohio-Michigan line. The only detailed work which the writer has attempted on these beaches is in the district between the Maumee and Vermilion rivers in northwestern Ohio and in Erie and Genesee counties, N. Y. The portion north of the Maumee had been mapped by Gilbert, and the portion between the Vermilion 760 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. River and Cleveland by A. A. Wright, while the portion between Cleve- land, Ohio, and Cattaraugus Creek in New York has long been known to the geologists who have made investigations in that region. Fairchild has continued the examination of the Warren shore from Hrie County, N. Y., eastward beyond the Genesee River, as indicated below. The outlet of Lake Warren appears to have been westward from Saginaw Bay through Spencer's ‘ Pewamo Strait”' to Lake Chicago, in the southern end of the Lake Michigan Basin, and thence through the Chicago outlet to the Ilinois and Mississippi rivers. But as this, as well as the part of the beach in Mich- igan, is soon to be made the subject of further study, a description will not be attempted in this place. DESCRIPTION OF THE BEACHES. The portion in Ohio north of Maumee River is reported by Gilbert to be a broad belt of sand, chiefly in the form of dunes but nearly level on the inner margin. The altitude of the sand extends from about 90 feet above Lake Erie down to 60 feet, or even lower. The western border leads from the Ohio-Michigan line near Sylvania southwestward to Napoleon. Gilbert remarks that the border is not so definite as it would need to be to admit of easy mapping, but stands near the line just indicated. The inner border of the sand belt touches the Maumee for a short distance just above Toledo, but for several miles farther it lies 2 or 3 miles back from the river, after which it again extends to the river. Sherzer’s studies, which have been extended southward from Michigan a short distance beyond the State line, have brought to light a range of sand ridges standing between 650 and 660 feet, which he considers the Forest beach. This range has not been examined by the writer, but upon inspection of the Toledo topographic sheet it is found that the rise is quite abrupt between the 640 and 660 foot contours, as if the lake had cut back its shore there. In the district between the Maumee and Sandusky rivers there are several conspicuous ridges of sand and belts of dunes whose altitude is more than 100 feet above Lake Erie. The plains on the border of these ridges have generally an altitude about 100 to 115 feet above the lake, or 670 to 685 feet above tide, and the main lake level appears to have been TAm. Jour. Sci., 3d series, Vol. XLI, 1891, p. 207. ees BEACHES OF LAKE WARREN. 761 between 680 and 690 feet. This altitude harmonizes more nearly with the Arkona beach than with the Forest. There seems to be no definite shore in this district below the level of these sand ridges to correlate with the Forest beach. The general altitude is 15 to 20 feet higher than Gilbert's estimate of the sand in the district north of the Maumee. It is possible, however, that the sand north of the river reaches an equally high altitude, Gilbert’s estimates having been made when there were fewer data than now concerning altitudes. There is a strip of sand south of the Maumee River setting in a mile or so above Napoleon and leading nearly due east for 9 or 10 miles. It consists of a series of overlapping ridges that trend west-southwest to east-northeast. The well-defined ridges are usually continuous for 1 to 2 miles, but several are a half mile or less in length. The ridges are 10 to 20 feet in height and 50 to 100 yards or more in width. The base seems to be nearly uniform at an altitude about 680 feet above tide. The mode of overlapping is such as to indicate that the ridges were built up succes- sively in a series from east to west by winds blowing from the west. From the eastern end of this system of ridges near McClure there is an interval of about 8 miles to Weston, in which the sand shows only oceasional ridging but forms a thin coating on the plain. The trend of this part of the shore being southeastward it was unfavorably situated for the action of the west or strong winds. At Weston a prominent sand ridge sets in which leads in an east-northeast course to Bowling Green, a distance of 8 miles, and is continued in faint form 8 miles farther in the same direction along the north side of Portage River. The altitude of the plain north of this ridge is about 675 feet above tide, and there appears to have been a shore near the line of this sand ridge; but the ridge was evidently wind drifted. Its highest points rise above the 700-foot contour, and one dune in Bowling Green reaches 720 feet. There are occasional sand ridges north of this main ridge. A conspicu- ous instance is found in a belt of ridged sand which sets in near Craws station, 4 miles north of Bowling Green, and leads west-southwest, with occasional gaps, 3 or 4 miles. The base of this sandy belt stands near the 670-foot contour, as shown by the electric railroad profile, and the ridges rise 5 to 20 feet above that level. A sand bar seems to have formed here at about lake level that was subsequently ridged by wind. East from 762 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Craws a rock ridge sets in which stands 8 to 10 feet above the plain and leads eastward past Sugar Ridge village. This also received a sand coating. For several miles south from Bowling Green small sand ridges appear which seem to have been formed by the wind from sand deposited in a shallow bay that extended up Portage Valley a little farther west than the meridian of Bowling Green. This bay must have been very shallow, for the railway altitudes at Mermill and Mungen indicate that its bottom was about 685 feet. From near Rudolph, about 8 miles south of Bowling Green, a belt of sand leads eastward through Jerry, and thence northeastward through Freeport and Bradner into the edge of Sandusky County. It is about as strong as the one which passes through Bowling Green, the dunes being from 10 to 25 feet in height and the belt of sand about one-fourth mile in average width. The lake seems to have extended southward on the line of Wood and Sandusky counties nearly to Rising Sun, for another sandy belt sets in a mile east of that village which leads northeastward about to _ Helena. This sand belt is in places nearly a half mile in width and has been drifted into dunes 10 to 20 feet in height. It is the easternmost promi- nent sand belt found in the district between the Maumee and Sandusky rivers. A few low sand ridges appear between Helena and Haven station (4 miles west of Fremont), but they are seldom more than 10 feet in height and but a fraction of a mile in length. A well-defined gravelly beach leads past Haven station in a course from north-northwest to south-southeast. It can be traced from the south- east corner of section 2, Jackson Township, to the south side of section 13, a distance of over 2 miles. Its height is 4 to 8 feet and breadth 50 to 75 yards. For about a mile south from the south end of this beach no ridge is found, but low sand ridges there set in which continue the shore in a southeastward course to Sandusky River near the mouth of Wolf Creek, about 6 miles above Fremont. On the east side of Sandusky River there is a sandy plain extending from Fremont southward into the edge of Seneca County. A few low ridges, 5 to 10 feet high, are found about 6 miles south of Fremont in sec- tions 33, 34, and 35, Ballville Township, Sandusky County, which probably constitute the continuation of the beach. The beach becomes more definite im section 19, Green Creek Township, and from that point runs in an east- northeast course to Clyde. The altitude at Clyde is about 680 feet and BEACHES OF LAKE WARREN. 763 barometric determinations give the ridges in Ballville Township a similar altitude. There appears to be no well-defined lower shore north or west of Clyde. Sand ridges appear east and south of the village up to an altitude about 710 feet above tide. These, however, were probably drifted by wind above the level of the old lake. From Clyde a very definite shore leads northeastward to Castalia. It presents usually a cut bank 10 feet or more in height, on whose face and crest deposits of sandy gravel occur. There are also sandy ridges for some distance south of this old shore. Before reaching Castalia the beach comes to a limestone cliff and follows its western base past that village. At the north end of the cliff, about a mile northeast of Castalia, the beach turns eastward and recurves as a spit along the east side of the cliff. From this cliff southeastward for several miles the beach is ill defined, though sandy ridges near Bloomingville and Prouts station seem to repre- sent it (see PI. XXII). About a mile east of Prouts a definite ridge of sandy gravel sets in which leads southeast another mile. Back of it a slightly higher ridge appears and leads southward to Huron River, passing just east of the village of Enterprise. It crosses Huron River 3 miles west of Milan, near the line of Erie and Huron counties. This ridge is composed of sandy gravel, is 3 to 6 feet in height and 50 to 75 yards in width.. It is remarkably regular for 3 miles north from Huron River and also for a similar distance on the east side of that stream in northern Huron County. On Marblehead Peninsula, north of Sandusky Bay, there is a small tract which stands sufficiently high to catch what appears to be the Forest beach. Its altitude is very nearly 100 feet above Lake Erie, or 670 to 675 feet above tide. It is developed for a distance of fully 2 miles, setting in about a mile east of Lakeside and following the north border of the penin- sula to that village, after which it bears southwestward into the interior. It is a low ridge, 3 to 5 feet high, composed. in large part of blocks of lime- stone, but occasionally containing gravel. The rocky character of this beach is strikingly similar to that of the shore of Lake Erie below it, where the waves are now piling up blocks of limestone derived from the clitts of the peuinsula. The beach which crosses Huron River 3 miles above Milan presents a well-defined gravelly ridge as far east as that village, but is rather indefinite from there northeastward to Vermilion River because of wind action, 764 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. there being a belt of dunes at about its level. From Vermilion River to Cleveland the main shore is a remarkably distinct and nearly continuous ridge of sandy gravel which in a few places becomes drifted into dunes. It crosses Black River about 4 miles north of Elyria and leads through the villages of Avon and North Dover, as indicated in the map prepared by A. A. Wright for the Geology of Ohio." It leads into Cleveland from the west along or near Detroit street, and after crossing the Cuyahoga River lies near Euclid avenue to the east edge of the city. From the point where it enters the city eastward nearly to the Cuyahoga, there is a bank 10 to 15 feet in height cut in the till which is capped by small deposits of gravel; but from near the river eastward it is built on the sand and gravel delta of the Cuyahoga and presents a smooth ridge, standing slightly above the plain south of it and 5 to 10 feet or more above the plain on the north. There is in Cleveland a higher and weaker beach known as the Wood- land avenue beach, which stands about 20 feet above the main beach. Its altitude, as determined by Upham,’ is 115 to 120 feet above Lake Erie or about 690 feet above tide, while the main beach is 95 to 100 feet above the lake or about 670 feet above tide. The upper one consists usually of a well-defined gravelly ridge, 3 to 8 feet in height and 50 to 75 yards in width, but in places is sandy and forms a broad swell, 100 to 200 yards in width. This upper shore seems to have about the altitude of the Arkona beach, while the lower apparently corresponds to the Forest beach. It is probably the Forest beach that Wright mapped as the “North Ridge,” from the Vermilion River eastward to Cleveland, lle the Arkona has not been mapped in that region. The portion of the shore from Cleveland prea aele to the Cattaraugus Valley in western New York has received only incidental notice, but the beaches are known to be well defined throughout the entire interval of more than 150 miles and to stand only 2 to 4 miles back from Lake Erie.. They are more sandy than the Belmore beach and dunes are very common. Usually there is a single strong ridge, which is known as the ‘‘north ridge,” the Belmore ridge being called the ‘‘south ridge.” But at many points two, and in places, three, ridges are found whose levels differ but a few feet. The main ridge is commonly the lowest in the series, and stands 65 or 70 1Geology of Ohio, Vol. II, 1874, p. 58. * Bull. Geol. Soe. America, Vol. VII, 1896, p. 343. BEACHES OF LAKE WARREN. 765 feet below the Belmore. The remaining bars or beaches are variable in altitude and in number, as well as in strength, and the causes or conditions which produced them are not at present clearly understood. The lowest or main beach marks a well-defined, long-continued lake level. The shore of Lake Warren, like that of Lake Whittlesey, shows marked differential uplift in passing eastward from the Ohio-Pennsylvania line. At the State Ime the upper ridge stands very near the 700-foot contour, while a lower ridge is shown by the Girard topographic sheet to be 678 feet above tide. The latter is the main beach between Cleveland and the. State line and seems to be the Forest. Its altitude is less than 10 feet higher than at Cleveland though the distance from Cleveland to the State line is nearly 70 miles. From the Ohio—Pennsylvania line eastward to Westfield, N. Y., a dis- tance of 50 to 55 miles, the first or uppermost ridge rises 42 feet, or to 742 feet as determined by Locke level from the railway station, while a second ridge stands 717 feet and a third ridge 705 to 707 feet above tide. At this place the second ridge is much weaker than the first and third ridges, yet its altitude, if compared with the first ridge, supports the view that it is the continuation of the Forest beach or second ridge found at the State line, the interval in each place being not far from 25 feet. The third ridge, though well defined at Westfield, with a bank 8 to 10 feet in height, seems not to have been developed extensively along the south shore - of the lake. The beaches continue to rise as far as the vicinity of Silver Creek, 25 miles beyond Westfield, but for a few miles from that place the shore bears south of east to Cattaraugus Creek, near Versailles, and the beaches show but little change in altitude. For much of the way between Westfield and _ Cattaraugus Creek there are only two ridges. The upper one reaches the 780-foot contour near Sheridan, and the lower one the 760-foot contour about 3 miles northeast of Sheridan, as shown by the topographic sheets. The shore bears away from Lake Krie near Silver Creek, running up the south side of Cattaraugus Creek to Versailles, nearly 10 miles from the lake. It comes back only a short distance on the north side of Cattaraugus Creek. The best defined beach formed for a few miles north of the creek seems to be a continuation of the lower of the two ridges found west of the creek. It leads northeastward past Brant Center, and near Pontiac to 766 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Eden, and thence to Hamburg. There is a complicated series of ridges from near Eden to Hamburg which apparently occupy the imterval from the lower up to the higher ridge. At Hamburg there are two beaches which differ nearly 20 feet in altitude. The lower and weaker one, known as Cooper ridge, leads westward from Hamburg about 2 miles, directly away from the upper beach, following the crest of a ridge on the north side of Eighteenmile Creek. The upper or main ridge leads northeastward past Abbotts Corners, Websters Corners, Spring Brook, and Elma Center to West Alden, crossing Cazenovia Creek at Spring Brook, Buffalo Creek at its bend 3 miles northeast of Elma Center, and Cayuga Creek about a mile southwest of West Alden. On each of these streams, as well as on smaller streams, there are prominent deltas at the points where the beach crosses, and the beach itself is exceptionally strong throughout this part of its course. The lower ridge was traced only about 2 miles northeast from Hamburg and is reported to be ill-defined between there and West Alden. About 3 miles southwest of West Alden weak, sandy ridges were found back of the main ridge at a slightly higher altitude, but they seem to be of very limited extent and their significance is not clear. The main beach from Hamburg to Alden, like the Arkona beach of the western end of the Erie basin, stands only about 50 feet below the Belmore beach, but it is a stronger shore line. At West Alden there is a separation into two distinct beaches, one of which leads eastward through Alden along the inner face of the Marilla moraine into Genesee County, where it dies out in a narrow plain standing between the Marilla and Alden moraines. The other beach bears north- ward through Alden Center, and thence northeastward past Crittenden, and comes to Tonawanda Creek at Indian Falls. The outer shore or beach seems to be a few feet higher than the inner, at least railway levels at Alden and Crittenden bear out this interpretation, the altitude at Alden being about 12 feet higher than at Crittenden, but at the point of separation near West Alden there is scarcely 5 feet difference. The outer beach is remarkably strong clear to its terminus. It consists near Alden of a series of overlapping ridges trending northeast to southwest, which were apparently built up in succession from east to west. They are rather sandy but contain also considerable gravel, so that they can not be the product of wind alone. BEACHES OF LAKE WARREN. 767 The inner ridge is strong and nearly continuous from West Alden to a point about a mile east of the Erie and Genesee County line. It there dies out as a ridge, but appears as a cut bank on the western ends of the Pem- broke ranges of gravel hills. A bay seems to have extended back along the north side of the north range of hills nearly to East Pembroke. The altitude of the beaches shows a marked increase in this interval between Cattaraugus and Tonawanda Creeks. From an altitude of 780 feet at Cattaraugus Valley the upper beach rises to 810 feet at Hamburg, 840 feet at Elma Center, and fully 860 feet at Alden. The lower beach rises from 760 feet to 790 feet between Cattaraugus Creek and Hamburg. The inner ridge, leading north from West Alden, is only 850 feet at Crit- tenden, but rises to the 880-foot contour about a mile northeast of Indian Falls, as shown by the Medina topographic sheet. This beach was traced by the writer only to the brow of the Corniferous escarpment a short distance northeast of Indian Falls, but it has since been traced eastward by Fairchild beyond the Genesee River. This tracing by Fairchild has extended Lake Warren beyond the limits assigned by the writer in a paper published in 1895,’ and is marked by his thoroughness and painstaking attention to details. The following description of the portion between Tonawanda Creek and the Genesee River is taken from Fairchild’s recent paper:° At Indian Falls the channel of Tonawanda Creek interrupts the beach for three- fourths of a mile, but it reappears in excellent form on the summit of the hill at the north edge of the village. A strong ridge of somewhat angular gravel lies upon the east side of the road and supports the house of Mr. C. T. Pratt. The southern end of this bar turns west, crosses the road, and then turning north runs along the west side ot the road to a three corners. Here the bar swings eastward, crosses the road by the house of Mr. Bascom, then curving northward passes behind the house of Mr. Peter Lester. In a short distance the bar turns east, at which point another branch runs west, the latter crossing the road and terminating upon the crest of the Cornit- erous escarpment. The eastward branch soon breaks into a series of overlapping bars and spits of good development. Turning northward, in about one-half mile the beach crosses an east-and-west road, by which is an old gravel pit in the ridge and soon drops over the edge of the Corniferous limestone a few rods east of a north- and-south road. For a short distance the shore line is a cliff in the limestone, but quickly surmounts the escarpment as a well-developed ridge of almost clear chert. 1 Correlations of New York moraines with raised beaches of Lake Erie: Am. Jour. Sci., 3d Series, Vol. L, 1895, pp. 1-20. * Bull. Geol. Soc. America, Vol. VIII, 1897, pp. 274-277. 768 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. . It is an interesting fact that the altitude of the Corniferous escarpment and the surface of the Warren waters were nearly coincident. From Indian Falls around to northeast of Batavia, a distance on the shore line of perhaps 20 miles, the beach is usually on the crest of the rock ledge as a ridge of nearly clear chert. At a few points the rock was higher than the water, and wave-cut cliffs are conspicuous. The best cliffs are south of Smithville, east of Daws Corners, and northeast of Batavia. From the point last mentioned in the detailed description the beach follows the irregular crest of the rock escarpment for 23 miles, crossing several highways, as shown in the map, and terminates behind a rock hill near a stone schoolhouse at three corners. A strong wave-cut cliff is seen upon the west end and north side of the hill which is an outlier of the Helderberg-Corniferous strata. About a mile west of the north-and-south, Smithville-Pembroke, road the shore line again becomes a ridge upon the drift-covered escarpment. ‘The beach then runs south 1 mile and after some interruption in a kame area crosses at four corners to the south side of the east-and-west town-line road and breaks into several bars. Another very heavy ridge is found one-fourth of a mile north on land of Mr. Weber Stevens, in an old orchard on the east side of an old road. This ridge of gravel runs east and south- east 1 mile. At the next north-and-south road, leading south from Oakfield station on the West Shore Railroad, the shore line is a cliff in till, but soon resumes its nor- mal character as a strong ridge of chert gravel along the south side of the east-and- west town-line road. For 3 miles the beach, as embankment or cliff, runs parallel with the road, close upon the south side, against the north side of the moraine or drift-covered terrane. It is generally 25 or 30 feet above the highway, which Jies upon the lake floor, the latter stretching north as a smooth plain. About a mile west of Daws Corners the strong bar curves southeast, then etter a gap by stream erosion it swings by curves Gctward to the Elba-Batavia road, which it crosses about one-half mile south of Daws Corners, close to the house of Mr. Sylvester Strong. The bar, which here is destitute of chert, ends about one-half mile east of the road ina heavy spit on the edge of a broad stretch of low ground. A wave-swept plain of sand borders the depression on the north with low spits run- ning into the depression. One-third of a mile south the shore line is conspicuous as a bold cliff in the east-and-west escarpment. Running eastward one-half mile, it becomes a bar and then makes a curve to northward lyi ing on the summit of the high, steep escarpment ot the Helderberg, about one-third of a mile south of the town-line road. At the extreme northern point the shore line is just beneath the very top of the escarpment, which is Corniferous. From this point the beach runs southeast 1 mile to the northeast-southwest road, at which point the ridge has been excavated for gravel. Here it is on the top of the escarpment as a good ridge, and so continues eastward for one-half mile, when it falls below the crest of the ledge and curves around to southward as a rock cliff for nearly 2 miles. The shore line crosses to the east side of the north-and-south town-line road, then after running along the road for about one-fourth of a mile it lies in the non nag for about the same distemace. then recrosses to the west side, and in half a mile becomes a well-developed gravel ridge. In the ground of Mr. Charles Thornwell it bears a gravel pit, visible from the highway. Near the gravel pit the bar has been cut by drainage, and south of the gully a fine BEACHES OF LAKE WARREN. 769 ridge is found, with north-and-south direction, on the land of Mr. J. Miner. This is about 23 miles northeast of the center of Batavia village. East of Batavia village the moraine, with strong relief, lies partially below the Lake Warren level. The lake waters were here entangled among the hills, and the beach is broken for 2 miles, but two well-defined wave-cut cliffs are conspicuous. These are clearly seen from the main line of the New York Central Railroad, which, eastward from Batavia, traverses the moraine and descends rapidly upon the silt plain formed as the floor of the Warren waters. The more westerly cliff is upon the ‘north and east side of a till ridge about 1 mile southeast of the bar last mentioned and about one-fourth of a mile east of the railroad. Well-defined but broken shore phenomena connect this cliff with another cliff in drift 1 mile farther eastward. The beach then runs northeast another mile, as a good ridge, to a strong cliff in Cornif- erous limestone, which shows excellently the effects of heavy wave action upon a headland. From this cliff a nearly continuous bar or ridge is found for the 6 miles 1 IL@ROW¥y 7 The beach passes through the southern and higher part of the village of Mor- ganville, and shows in good form both east and west of the village. The altitude of the beach is here definitely known. One and one-half miles northeast of Morganyille and about half a mile west of schoolhouse No. 3 is a station of the United States Lake Survey, located exactly upon the beach ridge, with a corrected altitude for surface of the ground of 880 feet. Upon the west side of the north-and-south road, by school No. 3, which is situated upon the beach, the crest of the beach is 4.56 feet under the top of rail of the Lehigh Valley Railroad at the road crossing one-fourth of a mile south. The altitude of rail is 884.60, making the crest of beach 880 feet. One-half mile farther east the railroad crosses the beach by a cutting, and the altitude is 879 feet. “Approaching Leroy, the beach becomes obscure upon a kame-like surface among low drumloids about one-fourth mile northwest of the railroad station. The level of the water surface passes through the lower or northern part of the village. The next appearance of the beach is a good gravel ridge about one mile east of the village, between the Leroy-Caledonia highway and the three railroads, on the land of Mr. A. H. Olmstead. The ridge curves around northeast of the farmhouse and barns, and once formed a hooked spit near the highway, which has been cut away for gravel. Across a brook and upon the south side of the highway the beach reappears in excellent form as a heavy gravel ridge beneath the residence of Mr. Abram Van Valkenburg. For about a mile the ridge follows along the south side of the highway, slightly diverging and giving location for the residences upon that side of the road. Eastward from here the ground is lower, with long, drumlin ridges. The shore line is exceedingly crooked and the ene phenomena obscure in the embay- ments, but usually pronounced at the north ends of the ridges. * * * Within 3 miles of Caledonia the shore line is thrown rapidly southward upon the west side of the Genesee Valley embayment. The Warren waters occupied the valley of the present Genesee River as far south as Mount Morris. The accumula- tion of sand and silt either side of the gorge (‘‘High Banks”) west of the village MON XLI——49 770 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. doubtless represents the delta deposits of the stream durmg the Warren episode, before the gorge was excavated. The waters occupied the preglacial valley of the river, now possessed by the Kishawa Creek as far as the village of Nunda, and numerous terraces and plateaus in that valley are thought to represent the work of those static waters. Fairchild also describes in the same paper a well-defined beach on the east side of the Genesee Valley leading from near Geneseo northeastward to Lima. Since publishing that paper he has noted evidences of the presence of a body of water having the level of Lake Warren in the valleys of several of the Finger lakes of western New York. In interpreting the lake history of that region he has called attention to a succession of lakes in these valleys.’ The earliest lakes were formed as the ice sheet first began to recede from the southern end of the valleys. They seem to have been very small and of short duration. As the ice sheet withdrew passages were opened between the different valleys and a common level for several lakes was established with an outlet across the lowest pass to the south at Horseheads, N. Y. To the lake thus formed Fairchild had earlier applied the name Lake Newberry,’ though at that time he supposed it to be a successor of Lake Warren. As the elacial retreat continued passages were opened between Lake Newberry and Lake Warren, and the former took the level of the latter. The Lake Warren waters appear to have advanced eastward with the retreat of the ice to the vicinity of Marcellus, N. Y., before a passage eastward to. the Mohawk Valley became available. With the opening of this passage the lake level was lowered and Lake Warren closed its history. The channel near Marcellus, which afforded a new outlet for the lake waters, was first brought to notice by Gilbert in connection with other channels in western New York,® but it remained for Fairchild to discuss the relations to Lake Warren. In the more recent of the two papers above cited Fairchild makes the following statements: Two miles south of Marcellus village a huge delta lies on the west side of the valley [Otisco], at the mouth of a great channel cut in the Hamilton shales. The topographic sheet gives the height of the delta terraces as 860 down to 800 feet. The delta is the débris derived from the excavation of the gorge and dropped by the 1 Bull. Geol. Soc. America, Vol. X, i899, pp. 27-68. *Tbid., Vol. VI, 1895, pp. 462-466. °Old tracks of Erian drainage in western New York: Bull. Geol. Soc. America, Vol. VIII, 1897, pp- 285-286. BEACHES OF LAKE DANA. oe powerful river in the slowly falling waters of the Otisco Valley. The gorge heads 4 miles northwest of Marcellus, and a mile west of Sheppards Settlement, on limestone, with an elevation at the intake, as given by Dr. Gilbert, of 812 feet. Here, at the head of the eroded ‘‘ gulf” (the only local name), the drift and shale are removed down to the hard limestone rock over considerable area. It is evident that an enormous vol- ume of water escaped at this point. This was the water of Lake Warren, which found here an outlet lower than its old one westward across Michigan to the Mississippi. Its western flow, that had been sustained perhaps some thousands of years, was, by the removal of the ice dam in this region, slowly reversed and shifted to the east toward the Mohawk-Hudson. This was the end of Lake Warren proper. For the similar body of water, but with falling surface and diminishing area, which found lower and lower outlets eastward along the ice front, we can have no specific name, but, using a generic term, may speak of it as the hyper-Iroquois waters. The Warren overflow into the Otisco Valley would have been quickly checked if some eastward outlet were not provided. This is found in another rock gorge, which we call the Cedarvale channel, that leads southeast from Marcellus to the Onondaga Valley. A great part of the excavation of this gorge was done pari passu with the cutting of the gulf and by the same water, but the initial height of the outlet must have been less than the height of Lake Warren. Theoretically the Warren waters entered this region with an elevation of more than 880 feet. Evidence of erosion at near this level appears in a cliff on the west side of the valley, 1 mile south of the intake, which has the appearance of stream cutting. This is near Mud Pond. On the east side of the channel, at the east-and- west road, one-half mile below the intake, is a gravel plain at 880+ feet, which is probably a flood plain of the early river. THE WITHDRAWAL FROM LAKE WARREN TO LAKE ONTARIO. LAKE DANA (LAKE LUNDY?) In falling from the level of Lake Warren to that of Lake Iroquois the glacial waters appear to have made brief halts at several levels below the lower beach of Lake Warren. These halting places are indicated by weak beaches. Of these temporary lake levels probably the most important is one which has recently been given the name Lake Dana by Fairchild In explanation of the halting at this level Fairchild has suggested the great resistance to erosion offered by the limestone which underlies the Cedarvale channel near Marcellus, it being thought that the Cedarvale channel was utilized by the falling waters down to that level. The shore of this lake has as yet been but partly traced, the most important section being on the west side of the valley of Seneca Lake in the vicinity of Geneva, N. Y. It has there been given the name Geneva because of this relationship to 1 Bull. Geol. Soc. America, Vol. X, 1899, pp. 56-57. 772 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. the town site. Fairchild states that the correlation of the Geneva beach with the Cedarvale channel is still theoretical, but that the knowledge of the problem, together with the aid of the topographic sheets, is sufficient to give great confidence in the accuracy of this correlation. He remarks further that Lake Dana existed perhaps a century, or several centuries; yet, as compared with Lake Warren, it had a brief life. There is but one place in western New York where the writer has noted evidence of a shore at the Lake Dana level. A gravel deposit at West Seneca, south of Buffalo, which seems to be the product of lake waves, stands about 180 feet below the level of the Forest beach, and is theoretically a continuation of the Geneva beach. It follows the crest of a narrow ridge which rises just above the 620-foot contour, while the lower of the two beaches on the neighboring part of the shore of Lake Warren, as shown by the Buffalo topographic sheet, stands near the 800-foot contour. This observation was made in 1893, before Fairchild had found the Geneva beach, and the ridge was traced only about a mile, as it appeared at that time to have little significance. In this connection the ‘‘Lundy beach” of Spencer should be con- sidered, since it stands near the level of Lake Dana. The name Lundy beach was applied by Spencer some years ago to gravelly deposits found on the borders of the Erie Basin at a level 140 to 155 feet below the Forest beach, which seemed to him to mark the shore of a lake1 These deposits are fragmentary, and the interpretation of shore phenomena seems open to question at several of the places cited by Spencer, if not at all of them. In view of this uncertainty, and aiso because the level seems to be 25 to 40 feet out of harmony with the Geneva beach, it hardly seems advisable to cite the “Lundy beach” as a feature of Lake Dana. Faint beaches have been noted in western New York at levels still further out of harmony with Lake Dana. About 4 miles south of West Seneca, on a bluff back of Bay View, a cut bank was found at a level 60 feet higher than the gravel deposit at West Seneca, the altitude being above the 680-foot contour. This bank, which has also been observed by Taylor, apparently marks a temporary shore of the lake, yet it harmonizes in altitude with neither the Geneva nor the Lundy beach. A few miles farther south, at North Evans, on the south bluff of Hight- ? Am. Jour. Sci., 3d series, Vol. XLVIII, 1894, pp. 207-212. BEACHES OF LAKE DANA. 773 eenmile Creek, and thence southwestward past Derby, gravel ridges were observed by the writer and subsequently by Taylor at an altitude of fully 700 feet which have both the form and the structure of a beach. These are stronger as well as more characteristic than any of the supposed shore features at the lower levels. (See note on p. 775.) Still other places were noted where beaches occur between the Forest beach and the shore of Lake Erie. One of the best defined is at the mouth of Chautauqua Creek, north of Westfield, N. Y. Taylor and the writer found its altitude by Locke level to be 34 feet above the surface of Lake Erie Gn August, 1899), or about 606 feet above tide. This is 136 feet below the highest Warren shore at Westfield, and about 100 feet below the lowest. There are several places between Westfield and the mouth of Eighteenmile Creek where a weak beach occurs at altitudes ranging from 35 to 60 feet above Lake Erie. These were examined by Taylor and the writer in 1899, and were at first thought to mark a single shore which rises more gradually toward the northeast than the shore of Lake Warren. But upon further reflection and a correction of barometric determinations, by means of the topographic maps of that region, it seems quite as probable that they are merely incidental shore phenomena of a falling lake. In view of the fragmentary character and the lack of harmony in level presented by these weak shore lines on the borders of the Erie Basin, it will probably be a difficult matter to establish satisfactorily the extent. of Lake Dana or the equivalents of the Geneva beach. The lowering of the lake level from Lake Dana to Lake Iroquois seems to have been accomplished by the withdrawal of the ice sheet and the uncovering of successively lower channels leading toward the Mohawk Valley. Fairchild states that the district from 15 miles southwest of Syracuse to 12 miles east was apparently the critical region, because a broad expanse of the low Ontario plain (400-4; see Pl. I) meets abruptly the elevated plateau, and here the ice body lingered in its last effort to dam the Huron-Erie-Ontario waters from the Mokawk-Hudson Valley. But as yet the full succession of,events and the relationship of channels subsequent to Lake Dana have not been determined. The history is partially obscured in the low Syracuse district by the changes in hydrography which have occurred since the ice removal. These, as stated by Fairchild, are (1) the possible existence of a pre-Iroquois water body with elevation toward TT4 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. 500 feet and consequent deltas and silting; (2) the primitive Iroquois with clevation much under 440 feet; (3) the rise of Iroquois to 440 feet and consequent filling of former channels, and (4) the stream erosion subsequent to Iroquois. LAKE IROQUOIS. This lake, which occupied the Ontario Basin and discharged eastward past Rome, N. Y., into the Mohawk Valley, will here receive only a brief notice, for the writer has given but little attention to its shores and outlet. Furthermore, it lies mainly outside the district under discussion. The portion of its shore from near Toronto, Ontario, around the western end of the lake and along its southern shore attracted notice in the early days of settlement. It was utilized as a trail by the red men and adopted for a high- way by the early white settlers. The name Iroquois, applied by Spencer, was given it because of its use as a trail by an Indian tribe of that name. The beach as determined by Spencer has an altitude of but 362 feet at the west end of Lake Iroquois, near Hamilton, Ontario. Spencer has found a marked rise on the north shore, the altitude at Trenton, Ontario, about 140 miles by direct line from Hamilton, being 632 feet. The south shore shows a gradual rise from Hamilton eastward to the vicinity of Rochester, its alti- tude there as shown by the topographic sheet being about 435 feet, but it lies so nearly at right angles with the axis of uplift from Rochester eastward to the Rome outlet as to be nearly horizontal. From the Rome outlet north- ward the rise is very marked, the altitude being 440 feet in the vicinity of the Rome outlet and 675 feet at Adams Center, only 60 miles to the north. The rise is thought by Gilbert to be even greater, for uplift was in progress while the beach was forming, so that it presents a compound form north of the outlet. The upper members of the compound beach joi the lower members upon approaching the outlet, but are thought to pass below them in the part of the lake which extended south farther than the outlet. Lake Iroquois was apparently held up to the level of the Rome outlet by the body of ice which still occupied the St. Lawrence Valley. Upon the withdrawal of that ice the sea entered the St. Lawrence Valley and the ~ Lake Ontario Basin, there being a beach containing marine shells exposed at the eastern end of the lake. This beach stands very nearly 200 feet below the Rome outlet. It passes below lake level near Oswego, N. Y., as determined by Gilbert. The discovery of a marine shore line at this level LAKE IROQUOIS. C0) has recently been supplemented by Coleman’s discovery of fresh-water shells in the Iroquois beach near Toronto. It now seems well established that Lake Iroquois stood nearly 200 feet above sea level. This determination is of value in working out the altitudes of the glacial lakes which preceded Lake Iroquois. It follows that Lake Warren, which stood about 450 feet above Lake Iroquois had an altitude not far from 650 feet above the sea, while Lake Whittlesey stood slightly over 700 feet, and Lake Maumee at its highest stage stood about 750 feet. These altitudes are but 30 to 40 feet lower than the present altitudes in the western part of the Lake Erie Basin, and covering, as they do, several lake stages, they bear testimony to long-continued stability in that region. Norr.—In eastern Michigan A. C. Lane has found a well-defined beach about 50 feet below the lowest of the Lake Warren beaches, or 690 to 700 feet above tide, which he has named the Grassmere beach. About 20 to 30 feet below the Grassmere is a fainter shore line which he has named the Elkton beach.t W. H. Sherzer has recognized the Grassmere beach in southeastern Michigan, and has traced it a short distance into Ohio. It there stands between 610 and 620 feet above tide, or about 40 feet above Lake Erie. He finds the lowest Lake Warren shore to be below the 660- foot contour.” The Grassmere beach may be a continuation of the beach at Derby, N. Y., noted on page 773, but as yet the plain south of Lake Hrie has not been exam- ined with sufficient thoroughness to warrant an opinion. In eastern Michigan and in the adjacent part of Canada a strong beach known as the Algonquin appears at the south end of Lake Huron at a level only a few feet above the present lake surface, but northward it rises to a much greater altitude.’ The Algonquin beach of the Huron basin, it is thought, may be of similar age to the Iroquois beach of the Ontario basin, but further study is necessary to insure satisfactory correlations. ' Geol. Survey Michigan, Vol. VII, 1900, part 2, pp. 73-75, Pl. VIII. 2 Tbid., pp. 141-143, Pl. VIL. 5J. W. Spencer: Am. Jour. Sci., 3d series, Vol. XLI, 1891, pp. 12-21. CHOY PRs Ve SOILS. SOURCES OF SOIL MATERIAL. The soils of the glaciated portion of the Ohio River Basin and of the Lake Erie Basin are very largely derived from the glacial drift and the loess and lacustrine silts that cover the drift. The underlying rocks are indirectly a source of much material, since their decomposed surface por- tions were incorporated in the drift, but they constitute a minor source so far as direct contribution is concerned. The great agencies involved in producing the soils of the glaciated district—the ice sheet, the glacial lakes, and the glacial streams—have lone since ceased to operate, but modern streams are still at work spreading alluvium over valley bottoms in their flood stages. The small lakes that remain in the depressions of the drift are precipitating marl deposits and carrying on their borders a vegetal growth which will some day yield a rich soil as the lakes are lowered. Vegetation has also been enriching the soil with humus over much of the plane-surfaced drift from the time it first gained a foothold on the drift surface; while organisms of various kinds, both plant and animal, have united with the atmospheric agents to break up the soil and mix it thoroughly. The preceding discussion has shown that there are wide differences in the ages of the drift deposits, there being deposits of Kansan or pre-Kansan, of Hlinoian, of Iowan, of early Wisconsin, and of late Wisconsin age. The exposed portion of the oldest (Kansan or pre-Kansan) drift in northwestern Pennsylvania constitutes but a limited part of the drift surface, amounting to but a few hundred square miles. The Ilinoian drift of northwestern. Ohio and southeastern Indiana extends over several thousand square miles outside the limits of the Wisconsin drift, but it is covered so deeply by silt of later (lowan) age that it forms the soil only on the valley slopes or in 776 Ee el tees a all SOILS. Cut places where the underlying silt has been eroded. The surface soil of that region is mainly on the Iowan silt, while the Sangamon soil that was formed between the Illinoian and Iowan stages of glaciation has been buried beneath that silt. The early Wisconsin drift within this region has a somewhat limited exposure. The remaining part of the drift surface, comprising a large area, is therefore of late Wisconsin age. The unglaciated portion of the Ohio River Basin is covered somewhat widely by Pleistocene deposits. There are not only the valley deposits brought down to the Ohio from the glaciated districts by glacial and modern streams, but also deposits on the uplands of a fine silt apparently of Iowan age. The soil of the flat portions of uplands in southeastern Ohio and even in States south of the Ohio is formed from this silt. Much of the unglaciated part of the Ohio River Basin is, however, so broken that the silt has been removed and soil is being formed from the Paleozoic rock for- mations, as it was before the deposition of the silt or the advent of Pleisto- cene glaciation. There are uneroded places in which the residuary clays formed by the disintegration of the rock surface may be clearly distin- guished in color and texture from the overlying silt of Pleistocene age CLASSES OF SOIL. There are several modes of classification of soils in use, based gener- ally on either chemical constitution or physical texture or characteristics. The classification which seems best to serve our purpose is based mainly on physical characteristics. The control which the physical characteristics exert upon moisture and temperature has been found by experimentation to be far more important than the mere chemical composition of the soil. It is found that under favorable conditions of moisture and temperature the majority of plants can readily gather sufficient food material from almost any soil. : In the Erie and Ohio basins the following classes of soils are present: (1) Residuary soils, or soils formed from the underlying rock; (2) stony clay soils, derived from the till or bowlder clay; (8) gravelly or stony soils; (4) sandy’soils; (5) silts or clays of fine texture, but more or less pervious to water; (6) peaty soils with a large amount of organic material. A tabular statement is here presented which shows the origin or mode of deposition and the areal distribution of the several classes of soils. 778 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. Table of soils in the Ohio and Erie basins. Class. Derivation. Areal distribution. Residuary Stony clay ....-..- Gravelly, or stony. Sandiyiieecesce c= Silty or clayey -..- Peaty or organic... Decay of the under- lying rocks. Glacial Glacial, glacial out- wash, streams, wave- action. Glacial drainage, streams, lakes, wind. In part by slowly flowing waters, probably in part by wind; also as a sediment in glacial lakes. Vegetal accumula- tions and shell de- posits. Unglaciated portion of the Ohio basin, where silt as well as glacial material is absent, and also on valley slopes within the glaciated region where the drift covering is too thin to afford a soil. On a large part of the moraines, and much of the till plains of Wisconsin age; along valley slopes in the Iki- noian drift; very limited exposure on the older drift of northwestern Pennsylvania. On the older drift of northwestern Pennsylvania; in inter- lobate moraines of Wisconsin age; to a limited extent as kames on till plains and moraines of Wisconsin age; to a very limited extent in the Illinoian drift; as glacial outwash along valleys in connection both with the Wisconsin drift and the older drift, and as outwash aprons to a limited extent on the outer border of mo- raines; as stream deposits both along glacial and modern drainage lines; as deltas along parts of the shores- of the glacial lakes where vigorous streams entered; as wave products along parts of the old lake shores. The valley deposits vary in coarseness with the strength of the current, and contain much sand both in the glacial and modern deposits; beaches of glacial lakes are composed largely of sand, and the lake bottoms are covered to a limited extent with sand; the beaches of Lake Warren are especially sandy; wind has drifted the sand into dunes to a limited amount in northwestern Ohio, and ina few places farther east, in the area covered by glacial lakes. Mainly outside the limits of the Wisconsin drift through- out the exposed portion of the Illinoian drift, and on flat portions of the unglaciated districts bordering the Ohio, both in valleys and on bordering uplands; the lower part of the Scioto and Grand River basins, much of the Maumee basin, and flat areas in northern Ohio, also carry a surface clay with few pebbles, partly a slug- gish stream deposit and partly a lake sediment; silt deposits are of limited extent in northwestern Pennsyl- vania and western New York, chiefly in lowlands and valleys. Locally in the Erie basin and the glaciated portion of the Ohio River basin, where drainage is imperfect; the most conspicuous deposits are in basins and lakes in- closed among the morainic knolls, but there are exten- sive peat bogs in northern Ohio between moraines where adequate drainage has not been developed. SOILS. 779 RESIDUARY SOILS. The residuary soils show variations which correspond in a rude way with variations in the structure of the rocks from which they are derived, In regions underlain by limestone there is usually a reddish-brown clay. In shale areas the residuary material is an adhesive clay varying in color to correspond with the underlying shale In sandstone and freestone areas the residuary material is siliceous rather than clayey or argillaceous. It often presents a color and texture similar to the deposits of Iowan silt that overlie it so that the lme of junction is difficult to determine. With proper rotation of crops the residuary soils are usually productive and profitable for agriculture, though they can scarcely compete with the soils formed on glacial drift. The fertility of the unglaciated tracts is also difficult to maintain because of the steepness of the slopes and the resulting great erosion. STONY-CLAY SOILS. The soils formed on the bowlder clay or till are usually very produc- tive, being composed of a varied rock material, a large part of which is in a sufficiently fine state of division to be available for plant food. In physical constitution also it is well calculated for agriculture, being suffi- ciently porous, as a rule, to allow air and water to penetrate it readily. Portions of it, however, have so compact a texture that underdraining by tile has been found necessary. In general all grains and fruits suitable to the latitude will flourish, especially where the surface is rolling or well drained. It has been found necessary to use fertilizers to insure a wheat crop on land that has been in cultivation for periods of forty to-fifty years, and advantageous on ground which has been under cultivation but a few years, a fact which testifies to the value of certain chemical ingredients to the growth of that cereal. The importance of the stony-clay soil may be appreciated from the fact that it constitutes the soil of the major part of the great agricultural States of Ohio and Indiana, as well as the most productive portions of western New York and northwestern Pennsylvania. GRAVELLY OR STONY SOILS. On the older drift of northwestern Pennsylvania and the gravelly portions of the moraines of Wisconsin age throughout the region under discussion as well as on the kames, the soil is usually stony. There are, however, but a few places where there is not a sufficient matrix of fine 780 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. material to afford sustenance to plants. Indeed, the grains and fruits are found to flourish in this class of soil. The gravelly outwash aprons border- ing the moraines and the deposits along the lines of discharge for glacial waters usually carry a capping of loam from a few inches to several feet in depth, which adds to their productiveness. It is only the trees and the deep-rooting plants that extend down to the gravel. The deltas and gravelly portions of beaches on the shores of the glacial lakes usually carry sufficient sand and loam as a matrix to supply the needs of plants. SANDY SOILS. The sandy soils are as a class the least productive of the whole series. They are, however, confined to narrow strips along valleys and to small areas on the borders of the glacial lakes. The most extensive tracts are near the shores of the glacial lakes Maumee and Warren in northwestern Ohio and the neighboring part of Michigan, and there they cover but a few townships. Elsewhere they are in narrow strips, usually but a fraction of a mile and often but a few yards in width, that follow the old shore lines. SILTY SOILS. The silty soils display considerable variation in texture, some being a compact clay nearly impervious to water, others a loamy clay in which water has a moderate movement, and still others a loam in which water has a free movement. The silt that covers the Illinoian drift in southeastern Indiana and southwestern Ohio is nearly impervious to water, and its flat areas are subject to flooding in wet seasons and to baking in seasons of drought. The term “slash land” has been applied to these poorly drained areas. The soil is in places underlain at the depth of a few inches by an ochery clay or ferruginous crust which is exceedingly refractory and difficult to break up. This ferruginous crust is so extensive here and also in districts farther west that it merits careful investigation as to methods for breaking it up and rendering more productive a soil which seems otherwise well calculated for profitable agriculture. The silt that covers the Wis- consin drift in parts of the Scioto, Grand River, and Maumee basins is usually sufficiently porous to permit water to pass up or down through it. Although the areas of Wisconsin drift which are covered with silt are generally so flat that some flooding occurs in wet seasons, the passage of water through the silt is sufficiently free to prevent baking in seasons of SOILS. 781 drought. he silt with loosest texture is usually found on the borders of the valleys. In places its coarseness is such that it might perhaps be better termed a sand, though the term loam is more commonly applied to it by the residents. Its texture is so open as to render it very productive. The silt which covers the residuary clays in unglaciated parts of the Ohio Basin is on the whole sufficiently loose textured and sufficiently varied in chemical constituents to afford a fertile soil. It remains only in small patches on the uplands, but is extensively preserved in the lowlands and abandoned valleys of southeastern Ohio and neighboring parts of West Virginia and Kentucky. PEATY OR ORGANIC SOILS. The peaty and organic soils occur in basins or in poorly drained tracts where the rank vegetation becomes submerged at certain seasons and is thus prevented from atmospheric decay. When drained, the peat being allowed to ripen and become warm, these bogs will in many instances yield large crops of potatoes, onions, celery, and other garden truck. These bogs, which for years stood as waste land, are thus becoming a productive class of soil. Norr.—It has been thought best to attempt no special discussion in this monograph of the wells and other water supplies of the region covered, for the Survey has already published several special papers on these subjects. The water supplies of Indiana and Ohio have received a general discussion by the present writer in Part IV of the Highteenth Annual Report of the United States Geological Survey, and the wells of Indiana have been treated in some detail in Water-Supply and Irri- gation Papers Nos. 21 and 26. Orton has discussed the rock waters and the flowing wells of Ohio in Part IV of the Nineteenth Annual Report, and Rafter has included western New York in his discussion of the water resources of New York in Water- Supply and Irrigation Papers Nos. 24 and 25. In addition to the material in the papers just mentioned many well sections and other data concerning water supplies may be found in the present report, chiefly in connection with the discussion of the structure of the drift. ay fing 7 A. Abbott, —, statement by - .------------------------- Aboit, Ind., altitude at and near morainic topography near INDEX. Alum Creek, Ohio, features of valley of--------...- Ackley, Pa., morainic topography near -----.-----~ Ht Acmaton, Pa., gravel terrace near ------ -- 746 Adamsville, Pa., strise near ---------------- 464 Adario, Ohio, wells at --------.-------.--- 558 Adelphi, Ohio, glacial deposits near 259, 268 morainic topography near --------------------- 397 Adrian, Mich., preglacial channel near .- 718 Agosta, Okio, altitude near -- oS 549 WEI De saa pos we csesos see eeoapeeS oe 559 Akron, Ohio, glacial deposits near-_-...-.---.-- 563-564, 605 Srawelyplailenea eee eae een eee eens aan 388 striz near 423 Aladdin, Pa., fluvial plains at, height of -.-----.-- 145 Albion, Pa., preglacial drainage near -------------- 137 Albion moraine, altitude of, range in --- 703 distribution Ofj--s—=-ss2—===—=—=—=-=== 701-702 drift of, structure of ---------.--- _ 106-707 inner border phenomena of--_----------------- 707-708 relation to Lake Warren. .---.----------------- 707 topography of ---- .--.-------------- - 703-706 Alden moraine, altitude of, range in -- E 684 distribution of 2322 ss2=——= === =- == : 684 drift of, structure Of =-2=--.-------2-- ---- == 685 cuter border drainage of----------------------- relation to Lake Warren--- topography of --. Alexandria, Ind., drift near---- Rite Ens coe Sees aoses Sebastes ac-eA eee eae Allegheny, Pa., fluvial plains at, height of ---_---- glacial gravel at gravel filling near, upper limit of -.- rock island at section in shale and gravel at, contact of_---.-.---.------ Allegheny Coal Measures, occurrence and char- FXOUELP OF .sogst eobser eocsceee seoe sete pee Bese Allegheny River, course and drainage area of .--. course, preglacial, of. ..-.----.----- ------------- fallioressss= = = 98 gradation plain on-_------.---- = gravel deposits in valley of Oldidivad CXOnmeemes sear soe eae cre ik rock floor of __- valley of, description of -- 5 See also Old Allegheny drainage system. Allegheny Valley Railroad, profile along Alliance, Ohio, altitude at Alquina, Ind., altitude at 125 129-148 , 125-127 129 Amanda Township, Ohio, striz in----.------------ Anderson, Ohio, wells at : Andersons Fork, Ohio, stris on-------------------- Andover, Ohio, altitude abe sseeesss seen eae striz near Andover Center, Ohio, drift near Andrews, H. B., cited__----.---..--- reference to-.-------- Angelica Creek, N. Y., length of-.--.--.------------ Anna, Ohio, altitude at ....-.-.--- boringsiat.-2. -s-c-s -seeeneees glacial channel near ---.. -- Appleton, Ohio, well at_-...-.-.---.---------------- Arcanum, Ohio, wells at Archbold, Ohio, beach near Area discussed, boundaries of __. elacialema pio Laesees eee eee topographicwmap Ofass-- anaes eee eee Arkwright, N. Y., altitude near__..-..------------ moraine near Arnold, Pa., glacial gravel at gravel filling near, upper limit of-------------- fluvial plains at, height of ---_---.-------------- Arthur, C. S., fossils collected by-----------. -.---- Ashland, Ohio, altitude near morainic topography near -.--.---------------- Ashtabula, Ohio, beaches near_.-----------.------- Ashtabula Creek, Ohio, course of-- Section onie-ee- = ose = Ashtabula moraine, course of-- topography Of 2272-2 eee eee noone a ee Attica, Ind., altitude at Attica, Ohio, altitude at_- wells near-. Atwater, C., reference to ....--.-..---------------- Atwater, Ohio, wells near---.-....-.-.-.---.-------- Auburn, Ind., altitude near_-.....-... .-....---.-- driftiat, 2. = 222s nee Auburn Center, Ohio, drift near_.-..-.-------.-- Auglaize River, Ohio, beach near--....-.---------- COUTSC.Of 22a = ese = en eee Aurora, Ind., gas boring at section near. -2---- ----2. ==. Aurora Township, Ohio, well in -.----- Austins Ohiontilliat. Spee e eee cee aoe eee Austintown, Ohio, striz at------- Ayer Flats, Ohio, glacial gravel on .---..---.------ Ayersville, Ohio, beach near-_---.-....------------- 661-662 189 _ 564 750-751 = ER 784 INDEX. Page. 1335 Bainbridge, Ohio, bowlder near --...-.--.--------- 420 Bainbridge Center, Ohio, well near----.-.--------- 593 Bainbridge Township, Ohio, striz in-- --- 422,609 Balbec, Ind., drift near. ---.---- -- - 517-518 morainic topography near - ----- 513-514 Bald Knob, Ohio, well on-.-.--------- -------------- 417 Baldwins Run, Ohio, bowlder on -----.------ ------ 420, Bangs station, Ohio, wells at--.-. 408 Barclay, Ohio, drift near---.----------------------- 645 Barre moraine, altitude of, range in- -----.-------- 696-697 distribution of ---------.---- --- . 695-696 drift of, structure of ------ -- - 700-701 relation to Lake Warren- = TOL OTOP Ts hiya Leena eee 697-700 Bartholemew, G. W., jr., information furnished [OP ee eel ie eee en eomeeu eres cee 366 Basil, Ohio, section near -----.---------------------- 410 Batavia, N. Y., altitude near------------- .--------- 689 [WEEK EERE ooo pasoseeercas Oe ebos oneccorecdiaeds 769 Batavia Junction, Ohio, section near --...--.------ 282 Batavia moraine, altitude of, range in - -, 689 GME OYENKON OF oop cae Saess2 ss cee cseseeesacem aces 688-689 drift of, structure of 690 HOpOP ap hiya@ beeen sate ane = men eee 690 Bayard, Ohio, altitude at--- Sears 440 morainic topography near ---.----------.--- ---- 451 Beach City, Ohio, boring at and near -------------- 403 Bean Creek, Ohio, beach near.----- ------ ------ ---- 748 Beanblossom Creek, Ind., drift in valley of, struc- ture of. ..------ 263 dvift border near, topography of --.----------- 254-255 Beaver, Pa., gravel filling near, upper limit of - --- 246 terrace remnants near ---..--------------- Beaver Creek, Ohio, change in course of Beaver Falls, fluvial plains at, height of Beaver River, altitude in valley of .-..-------.---- drainage area of _-..-.---.--- PA Ope teeta ee hate oe fluvial plains on, height of - glacial outwash in valley of-_.--..-----.-------- 25) gradation plain on--_--.------.--------- gravel deposit in valley of -- outlet northward of Upper Ohio through-.--- 94-98 inoleltc saVolore A) leva ame eee eal ha ee 150 rocks along, character of---..-- 96-97 strise in valley of 465 Bedford shale, occurrence and character of-- 61-62 Beech Flats, Ohio, drainage changes near --------- 267 Béechy Mire, Ind., well at_-.---.----.---------- ---- 331 Bellaire, Ohio, gradation plain near ----.- 93 gravel and sand near - = 122 topography near 93 Belle Center, Ohio, morainic topography near--_-_. 533 Soria iatiand mear es. - so 2222 soba es Be 424, 487,529 wells at and near -.- ~--.----- 482, 534-535 Bellefontaine, Ind., wells near -.----.-------- ...-.-. 519-520 Bellefontaine, Ohio, altitude of drift and rock sur- HENGS) WIENS OSS Lone tating ase ee eee a 356 dnifttiatitnickness/ofes2sses sss 70. Sue eee 361 Strice near_-.--.-.-.- 380 wells atand near---- 367 Bellevue, Ky., drift near -_---. .---------------.----- 258 Bellevue, Ohio, beach near-- Bas 730-731 MPLS: Abra 2 22 = aoe see ee ae ese. _ 424,609 Bellevue, Pa., fluvial plains at, height of- 145 Egllville, Ohio, wells near _--.----.--.----- 406 Belmore Beach, altitude of, variations in -------.- 747 GOSerip blony Of oes eho ame eee ae ne 746-747 Page. Belmore Beach, distribution of..............--...- 745-746 map of,near Defiance, Ohio__.._..-.....-._.... 748 section of -_--.-.- Ppocsine Solos sac2 S800 Stsconar seus 669 Bemis Point, N. Y., drift at Seas 642 TWO fey ee a eee 2 453 Berea, Ohio, drainage changes near._-._-.--------- 618 Strie near: = 225. s2ceigse ae eee eee eee See oboe Berea grit, occurrence and character of. 62 Berlin, Ohio, drift) mean sses sree aes e eee eae 404 Bethel, Ohio, bowlders near ---.---.--------------- 276 buried |Soilimean== asses as eanan aenen eee eee 278 section near = -U22 Vase eee eee cen eee 273 Bibliography. 22202035 - eee ae eee 28-49 Big Bend, Pa., terrace at----=-222--- 28. ee 472 welliat) 2 3222s Seances eee ene see 469 Big Blue River, Ky., gradation plain on -.--.--.-. yas Big Bone Creek, Ky., abandoned channel near ... 114-115 Big Cedar Creek, Ind., course of ----.-------_----- 547 Big Sandy Creek, Pa., morainic topography near. ANT SDT 80) TLCS ae erate es 464 wells near _ 459 Big Sandy River, W. Va., rock flodtat, altitude of . 105 Big Springs, Ohio, strie at and near -.-.-----.--.-. 424,529 wellat.2. 2.530 ste. jee eee ee 535 Big Walnut Creek, Ohio, gravel belt on-- 433 Bingham, Pa., altitude near ~.--.------.-- ‘i 201 Birmingham, Mich., altitude near._-.---.--_-- ate 725 beach near 721 Birmingham, Ohio, striz near- - 423, 609 Bishop, I. P., cited 708 Black Fork, Ohio, knolls in valley of 566 striso nearsee ee toi ek Te oe Nees ene 423 Black River, Ohio, beach near -.--_---.------... 732-733, 743 course, present and preglacial, of --- 217 topography near.- 614 Blanchard moraine. See Defiance moraine. | Blanchard Townsbip, Ohio, striz in._-.-..-..-.--- 581 Bloomtield Center, Ohio, drift at -----.-----..----- 645 Blue Creek, Ind., course of_------.---- Blue River, Ind., fall of, rate of ------.------------ Blue Eye Creek, altitude near -..-...-------------- Bluffton, Ind., altitude near ------------- VEER. 549 morainic topography near -- -.-.-----.---.---- 553 Boardman, Ohio, borings near- -----~--- ae 462 Bokes Creek, Ohio, flowing wells along ---.------- 5387-538 Bolivar, Ohio, topography near ----.-. ...----------- 388 Bon Harbor Hills, Ky., rock island at -- 87 Bond Hill, Ohio, sand deposits near -- - 280, 281 Borden, W. W.., cited _-_- ---.-----_-- 58 reference to----..-- Se Sees 28 Boston Ledges, Ohio, strise at -----.-.----.--..---- 423,609 Botkins, Ohio, altitude of --..--- 512 morainic topography near -------- 513 Bowling Green, Ohio, sand ridges near --..---.---- 761-762 Bownecker, J. A., cited -.--..---..-.--.---. 181, 183, 368, 501 reference tolls. 4s. 2essctescse Joe saape nee 518, 520, 576 Bowser, Ind., altitude at -- 497 Braceyille, Ohio, wells at-- 469 Braceville Township, Ohio, striz in-...----------- 465 Brandon, Pa., drift at and near--..--.--.---.---.-- 233 Bremen, Ohio, drainage changes near --.--.-----.- 170-171 Briggs, C.,jr., reference to 20 Brighton; Ohio, stris mean -ss oe a eeen seen 423, 609 Bristolville) Ohio, driftiat sess ssas eee 645 Broadway, Ohio, morainic topography near------ 533 WGI means See a ee eee en os 5385 Broadway moraine, altitude of, range in - ae 532 ibowilders:on’ {22.2.2 2.6 5 eee en eae eee 535-636, correlation of {5.225 -e ee ee eee eee Obese INDEX. Page. Broadway moraine, distribution of -...--_._._.... drift of, structure and thickness of -._ inner border phenomena of ---.---------..---- g outer border phenomena of -----.- THE VEO a eee goeece cca ltc Sate eee ees Strimjalone oases: eee eee at co sone ee topography of .--..------- Brockport, N. Y., altitude near----.--.-------- Brokenstraw Creek, Pa., course, preglacial, of... 140,142 Griftiom Gar ee esses ota eee sm a see Sees 234 morainic topography along.----.----..----.-- 445 Brookfield, Ohio, strize at Sees 465 Brookville, Ind., altitude near--.--- .-----.-..----- 308 (BOTs Pa bee eee ee on a oe 285 glacial deposits near -..-.--...---------- -- 323 gravel knolls near--_- coi occ ae 313 rock floor at and near, altitude of ---- 185 Wellsim@antes sess sles eee ee = eo 320 Brunswick Center, Ohio, well at ---_---------_---- 615 Brush Creek, Ohio, preglacial course of -- - liz GL Ak Omer ee ee ee et eck 273 Bryan, Ohio, altitude near ---_.----.---------2.---- 570 Ibeachinean se -wess seo ssne os ccen eee Gale Shoreline mean ass se. 2s a. ae eee pe 749 Bryant, Ind., altitude at___._...___..._.._---- 512 Buck Creek Valley, Ohio, glacial deposits in_-_..__ 315 Buck Ridge, Ohio, bowlder on _----------. --------- 420 Buckskin station, Ohio, striz near zt 424 Bucyrus, Ohio, altitude near_-_._------- .- oe 549 CURT bates en ean ee ce 559 Buttalo, N, Y., Pleistocene features near, plate SHOWING paces eee eee pe pemeeeen 25.5. % S brie bhe ees cose eaae hearer. a 708-709 Buffalo Creek, N. Y., present and preglacial course Of saa inp es emp eaa ny pee 211-212 Bull Run, Ohio, striz on. hse ve 348 Bunker Hill, Ind., drift at- ses = A487 Bunker HallPa., dritt apes... =. 22s ate 233 Bunn, A. D., acknowledgments to --_-.--.--.-..---- 408 Burbank, Ohio, altitude at and near -------_._..-. 549,569 morainic topography near -_-----.------ 571 Bure; El @hio; Shrissepeee = ene | ee 465 Buried soil. See Soil, buried. Burns. Nev al bibdate ne 202 Butler, Ind., morainic topography near --..-.----- 55d Seehlomiat-:--2_- oe eepeeene pe oases eas cone 504 Cc. CablesOhio; drift nearleeemsee 28-2 -----. = 28 47 Ceesars Creek, Ohio, gravel beds on ____-_-___-._._ 336-337 ; Sbrico meats... 0 eet. se 1BAQYADE Cambridge, Ind., wells at 22222225. ---_-- ---..----- B24 Strisomean. . 22.25 ase oe setts oe 327 Camden, Ind., sections near_----..-.--._.--___.--._ 520 Camden, Ohio, altitude of drift and rock surface near Brn. == = 306 drift at, thickness of -- 2. ceeeoblean Campbell, M. R., cited ._--- ii Campbellsport, Ohio, well at --.._._.._ ___.___._-- 462 Canal Fulton, Ohio, drift near ----__-.__. __...----- 402-403 Canal Winchester, Ohio, borings at and near --__- 411 Caneadea, N. Y., terraces at, altitude of ____-. ---- 206 Caneadea Creek, morainic topography near ------ 639 Cannelton, Ind., Tertiary deposits near----_-.-__- 111 Canton, Ohio, altitude at--.------<52s.-_. -_.------- 441 bowlder near 420 topography near a-hs-.-.-- 2 ose oe 388 MON XLI 310) Page Carey, Ohio, stri# near _...-.-----.--------- $25 581 Carlisle, Ohio, altitude of drift and rock surface Mear _ 2.22322 wedee eee = 52 356 gravel plain near Carll, J. F., cited 129, 132, 187, 138, 140, 142, 229, 458, 454, 455 reference to.______- Lees 27,137, 214 Carroll, Ohio, boring at - 411 Strioa Nears... cue sneees 424. Carrollton, Ky., drift ridge near 257 mock. island near: -oos7- seeeee nese es oo 5 oo eee 86 welliat.—-...--. : Cass City, Mich., beach near _.__.-.....--.--.-.-.-. 743-744 Cassadaga Valley, N. Y., altitude in-..-.-_/.-.-__. 626.. drift in 623, 635 moraine in 655 topography of 664 Castalia, Ohio, beachinear -_--.__---._ =. --1 2-2. 763 Catawba, Ohio, altitude near _----_-_---. ------~..-- 335. Catawba village, Ohio, wells at-__-..--------_.----- 416 Catskill group. Ste Berea grit. Cattaraugus Creek, N. Y., altitude near .________. 658: course, present and preglacial, of _______-_____- 212-2138 Moraine Nearii/ssseeelee see eee ee eee eo bot till on gay 675 Cedargrove, Ind., boring at 285 Celina. Ohio, altitude near 549 Centerville, Ind., well at ___ Pees B25 Centerville, Ohio, ridge near _________- 358 Centerville, Pa., altitude at __.__-_.___. 440: Chagrin River, Ohio, altitude near ___.__-__._____. 626. GOUTSO Of . ==. -2e Sas eee eee ee ae 215, 216 topography near - 327, 660 wells near __-__- = 643. @hamberlin, T..C.citedies sees ee 24, 50, 228, 241, 299, 302, 304, 349, 354, 371, 372, 416, 437, 473, 482, 494, 608. letter of transmittal by 17 qmoted!.. +... eee 4 -- 199, 442 mererence to. 22-255. seseeseesens coos eee 341, 352, 384 pWOPI: OF _ - 23 eR Eee eee Non Sane 28: Chamberlin, T. C., and Leverett, Frank, cited ____ 89,95., 123-124, 212 Chamberlin, T. C.,and Salisbury, R. D., quoted____ 421 Champion Center, Ohio, drift at___-...___.-._-.__. 645 @hance, H. IM. (citede2= =e | ipa I ee P40, 242 WOLKIOL.! teases é aT Chandlers Valley, Pa., altitude at ________- “ 439 morainic topography near _._-___-_ ._____ 444, pwell s sin |= 22 tee eee eee cs deeds @haplin, J. P:;;reference tose... ---. = --2-peee os 2-88 108 Chardon, Ohio, altitude near_ 626 drift near eae re = 5 Strive near. See eee a2 os eee eee 466 Charlestown, Ind., wells at --_._---....-- 284 Charlestown Center, Ohio, altitude at 441 Chatfield, Ohio, altitude near _____.___...____ 570 Chatham Center, Ohio, altitude near 583 WiGllsiatjeeee ween eens. os oes 595 Chautauqua Lake, N, Y., altitude near-- -- 626, 657 drifttimeare aioe. 2-022. ioe ee Be. 642 gravel plain near Ee 649 topography near 634, 635, 663 Chemung group, occurrence and character of___- 59 | Cherry Creek quadrangle, N. Y., map of portion (3 ee Sr oom CAPE O reaat 654 Cherry Valley, Ohio, drift near_._..._-._...__.____ 646 | Chester Township, Ohio, strize in___...__....-____. 422, 609 i eee ee ee gk See. ae Bae ee 3 eg ee . ao a iss Rs ss = : :