697 
 65 
 
 , ' 1 1 i .1 
 
CORNELL 
 
 UNIVERSITY 
 
 LIBRARY 
 
 GIFT OF 
 C. J, Paterson 
 
 ENGINEERING LiBRAP''' 
 
Cornell University Library 
 QE 697.W94G5 
 
 The glacial boundary in Ohio, Indiana an 
 
 3 1924 004 111 948 
 
The original of tiiis book is in 
 tine Cornell University Library. 
 
 There are no known copyright restrictions in 
 the United States on the use of the text. 
 
 http://www.archive.org/details/cu31924004111948 
 
®tie peoteiit ^tefw/ S«0tovital Sotittg, 
 
 CLEVELAND, O. 
 
 THE 
 
 Glacial Boundary 
 
 IN OHIO, 
 
 INDIANA AND KENTUCKY. 
 
 PROF. G. FREDERICK WRIGHT. 
 
 CLi;VELAND, OHIO: 
 
 LEADER PRINTING COMPANY, I46 SUPICRIOR STREET. 
 
 1 884. 
 
Preface. 
 
 •yi^HEN. ten years ago, I began my investigations con- 
 yiy earning the kames of the Merrimac valley, in Eastern 
 I Massachusetts, I little thought to what it would lead; 
 and, after having traced the boundary of the glaciated area 
 from the Atlantic Ocean to the southern part of Illinois, I am 
 equally in doubt as to what the future has in store in this 
 most interesting line of exploration. 
 
 Ttie Detailed Report, occupying the larger part of the 
 present publication, is little more tlian a simple recital of 
 observations, designed to put the reader in my own position, 
 and to furnish the facts which all scientific men would wish 
 to know. I have endeavored to be so specific that future 
 observers may be able to verify my statements, and may intelli- 
 gently connect their own observations with mine. Whether 
 I shall publish, in equal detail, my observations already made 
 upon Indiana, the future must determine. I hope, however, 
 to continue my investigations across Illinois and Missouri, 
 and may then give fuller details of what I have already done 
 in Indiana. 
 
 The preliminary lecture (with its map on page 17), gives the 
 facts concerning Indiana with sufiBcient clearness to show 
 their relations to those more minutely described in Ohio. 
 
 When the present report was written, I had supposed that the 
 joint report of Pkofessor Lewis and myself, upon the glacial 
 boundary in Pennsylvania, would already have appeared; and 
 some sentences in my remarks upon Columbiana county, 
 Ohio, presume some degree of familiarity with the views we 
 had presented concerning what is called the "fringe" of the 
 boundary in Western Pennsylvania. As that report will soon 
 appear, it is not necessary to repeat here what will so soon be 
 accessible to the public. Furthermore, my preliminary lec- 
 ture puts the reader in possession of the general facts. 
 
 Among the satisfactory rewards coming to one who engages 
 in such unremunerative, but original, investigations as those 
 
4 Preface. 
 
 here recorded, is the ready appreciation of his work by so 
 wide a circle of intelligent men whose time is absorbed in 
 other occupations, but who, when the facts are brought to 
 light, are quick to see their importance. 
 
 I have, also, had special occasion in these investigations to 
 be thankful for the personal encouragement, appreciation, and 
 advice of such authorities as Prof. Charles H. Hitchcock, 
 Prof. Alpheus Hyatt, Prof. E. S. Morse, Prof. J. D. Dana, 
 Prof. J. P. Lesley, Prof. Edwaeu Orton, and Col. Charles 
 Whittlesey. But it is to the Cleveland Historical So- 
 ciety and its friends that I am specially indebted for the 
 means to prosecute my work in Ohio and Indiana, and 
 that the public is indebted for so full and complete a report 
 of the facts as is here given. The funds directly pro- 
 vided for my expenses, by the friends of the Society, amount 
 to $450.00, the most of which was contributed by Jarvis M. 
 Adams, Esq., President of the New York, Pennsylvania and 
 Ohio Railroad, and Messrs. Datst P. Eells, Joseph Perkins, 
 and T. P. Handy. To Mr. Adams I am also indebted, both 
 for passes on the railroad of which he is President, and for 
 others secured by his intervention on the Cleveland and Pitts- 
 burgh Railway; Cleveland, Akron and Columbus; Cincinnati, 
 Indianapolis, St. Louis and Chicago; Indianapolis and St. 
 Louis; Ohio and Mississippi; Cleveland, Columbus, Cincin- 
 nati and Indianapolis; Pittsburgh, Cincinnati and St. Louis. 
 
 The cost of the investigations has, also, been diminished 
 by various friends, who have accompanied me and borne their 
 share of the expense, among whom should be mentioned Mr. 
 J. H. Kbdzie, of Chicago, C. 0. Baldwin Esq. (Secretary of 
 this Society, and through whose well-directed eilorts the local 
 interest in the subject is largely due), and finally the late la- 
 mented Rev. Charles Terry Collins, whose sudden death 
 will inflict a loss upon a multitude of philanthropic and educa- 
 tional enterprises. The Rev. Mr. Collins was first and fore- 
 most among those who set themselves to interest the Cleveland 
 public in this matter, and he was with me two weeks in the 
 field, entering into every minutiae of the investigation with 
 unbonnded enthusiasm, and with sagacious appreciation of 
 the whole bearing of the discoveries. 
 
TABLE OF CONTENTS. 
 
 GLACIAL PERIOD IN AMERICA : page. 
 
 Introduction 7 
 
 Signs op Glaciation 9 
 
 1. Scratches upon the Rocks 9 
 
 2. Till, or Boulder Clay 10 
 
 3. Transported Boulders and the Terminal Moraine 11 
 
 a. Irregularity of the Boundary Line 11 
 
 6. Irregular Elevation of the Boundary Line 18 
 
 c. Character and Amount of the Debris 21 
 
 Some General Considerations 23 
 
 1. Relation of the Glacial Period 23 
 
 a. To Agriculture and Health 23 
 
 b. To Archaeology 24 
 
 2. Date of the Glacial Period 28 
 
 3. Centers of Glacial Dispersion 29 
 
 Conclusion 31 
 
 DETAILED REPORT FOR OHIO: 
 
 Columbiana County 35 
 
 The Fringe .35 
 
 The Moraine Proper 37 
 
 Stark County , 38 
 
 The Fringe 38 
 
 The Moraine Proper 38 
 
 Holmes County 43 
 
 Beriin Township 44 
 
 Hardy Township 44 
 
 Monroe 47 
 
 Knox 48 
 
 Knox Oounty 49 
 
 Jeflferson Township 50 
 
 Union , 50 
 
 Butler and Jackson 51 
 
 Licking County 51 
 
 Eden Township 52 
 
 Mary Ann 52 
 
 Newark 53 
 
 Licking and Franklin 53 
 
 Perry County 54 
 
 Thorn Township 54 
 
 Reading 55 
 
 Fairfield County 55 
 
 Richland and Rush Creek Townships 56 
 
 Pleasant 56 
 
 Bern and Hocking 68 
 
 Madison 59 
 
 Pickaway AND Hocking Counties 59 
 
6 Contents, 
 
 Ross County 60 
 
 Colerain Township 6® 
 
 Green 62 
 
 Springfield 63 
 
 Union 63 
 
 Concord and Twin 64 
 
 Buckskin and Paint 66 
 
 Paxton 66 
 
 PiKB County 68 
 
 Highland County 68 
 
 Marshall Township 69 
 
 Jackson 69 ' 
 
 Adams County 70 
 
 Brown Bounty 70 
 
 Hamilton County 72 
 
 Kentucky 73 
 
 Campbell County 73 
 
 Kenton County 73 
 
 Boone County 74 
 
 APPENDIX: 
 
 1. Abstract of the Bearings of Glacial Strise and Grooves in Ohio (Compiled by 
 
 Col. Charles Whittlesey) 77 
 
 2. The Glacial Dam at Cincinnati 81 
 
 a. Its Effects Along the Upper Basin of the Ohio (A Paper by Prof. I. C. 
 White) 81 
 
 b. Its Effects in Boyd County, Ky 85 . 
 
 c. Mr. G. H. Squier on its effects in Bath County, Ky 86 
 
 d. Prof Lesley on the Glacial Dam 86 
 
 PLATES: 
 
 I. -Glaciated Region of North America 8 
 
 II. Glaciated Region of the Delaware Valley 12 
 
 III. Glaciated Area of Pennsylvania 13 
 
 IV. Same of Ohio 14 
 
 V. Glacial Boundary in Indiana 17 
 
 VI. Palseolith from France 24 
 
 VII. PalEBolith from New Jersey 25 
 
 VIII. Columbiana County 34 
 
 IX. Stark County , 34 
 
 X. Holmes County 45 
 
 XI. Knox and Licking Counties 45 
 
 XII. Licking, Perry, and Fairfield Counties 57 
 
 XIII. Fairfield, Hocking, Pickaway, and Ross Counties 57 
 
 XIV. Ross, Pike, and Highland Counties 67 
 
 XV. Highland, Adams, and Brown Counties / 67 
 
 XVI. Brown, Clermont, and Hamilton Counties 71 
 
 XVII. Kentucky 71 
 
A LECTURE 
 
 ON THE 
 
 Glacial Phenomena in the United States, 
 
 BY 
 
 PROF. G. FREDERICK WRIGHT, 
 
 GIVEN BEFORE THE WESTERN RESERVE HISTORICAL SOCIETY, 
 
 IN CASE HALL, CLEVELAND, OHIO, 
 
 NOVEMBER 27, 1882. 
 
 Note. — When this lecture wa3 delivered my inveatigations had reached only the Indiana 
 line. During the present summer (1883), I have continued the exploration to the Illinois 
 line, and hence have thought it best to make such changes in the lecture as will give the 
 latest results. 
 
 T HATE been led by the circumstances in whicb I have been 
 ■*■ placed, and which I need not here rehearse, to study some- 
 what extensively the glacial phenomena of the Atlantic States 
 and of the Mississippi basin. By reason of some special famili- 
 arity with the subject, acquired by a long residence in New En- 
 gland, I was invited two years ago, in company with Professor 
 H. C. Lewis, of Philadelphia, to trace the southern limits of 
 glacial action for the Geological Survey of Pennsylvania. A full 
 report of our work will soon appear. It is through the though t- 
 f ul generosity of several friends of this Society that I have been 
 permitted to continue these inv,estigations in Ohio ; and I will 
 take this occasion to return thanks to these gentlemen and to 
 the railroad companies who have facilitated my work. I should 
 also say that both in this State and Pennsylvania our work has 
 been simply supplementary to that of previous surveys. No 
 one can appreciate more fully than myself the value of the gla- 
 cial observations made by Colonel Whittlesey, Professor New- 
 berry, Professor Orton, Professor Andrews, Mr. M. C. Eead, 
 and others of the Ohio Geological Survey. But unity could 
 not well be given to the subject, except one person should go 
 over the whole line, and be able to compare the phenomena of 
 one section with those in another. 
 
 GBNBEAL SURYEY OF THE SUBJECT. 
 
 To understand the significance of the glacial phenomena of 
 the State, it is necessary to take a brief survey of the general 
 facts concerning the glacial period. A study of the phenom- 
 ena of the glacial period gives one an impression of the irre- 
 sistible power and grandeur of nature's operations, second only 
 
Glacial Period in America. 
 
 to the study of the geological forces which elevated the conti- 
 nents, and to that of the astronomical forces whose effects are 
 seen in the motions of the heavenly bodies. During the glacial 
 period more than 4,000,000 square miles of the land surface of 
 the Northern Hemisphere was enveloped in glacial ice. In 
 North America this ice sheet extended, upon the Atlantic 
 coast, as far south as Long Island and New York City, and on 
 the Pacific coast to the southern border of British Columbia : 
 
Glacial Period in America. 9 
 
 while in the central portion of the continent the glacier every- 
 where advanced nearly to the Ohio Kiver, and in two places 
 crossed it. The depth of this ice-sheet in America we know 
 to have been at least several hundred feet at its margin, while 
 in the interior it was severtil thousand feet in depth, or deep 
 enough to cover the highest mountains in New England. 
 
 In Europe the land is less continuous than in America, and 
 hence the glacial phenomena are more difficult to interpret. 
 But nearly all of Ireland, the whole of Scotland, and the north- 
 ern part of England and Wales show marks of long-continued 
 and extensive glaciation. In Switzerland the glaciers foi nierly 
 extended till they filled the whole valley between the Alps and 
 the Juras, and upon one side flowed down the valley of the 
 Ehone as far as Lyons, which is in a straight line 130 miles 
 from Geneva. The whole distance traversed by that portion 
 of the Swiss glacier was 270 miles. On the other side of the 
 Juras, in the valley of the Ehine, the Swiss ice-current prob- 
 ably met, upon the plains of Germany, the counter current 
 coming down from the Scandinavian peninsula; while in Italy 
 glaciers extended to within a short distance of the river Po, or 
 more than a hundred miles south of the summit of the Alps. 
 The Scandinavian peninsula was completely enveloped with 
 glacial ice, moving southerly, easterly, and westerly, in lines 
 of the least resistance. Upon the shores of the White Sea the 
 motion was nearly east and west. In Finland and in the neigh- 
 borhood of Stockholm the motion was south, while upon the 
 west coast the motion was towards the Atlantic Ocean. 
 
 SIGN'S OF GLACIATION. 
 
 The signs of glaciation are three-fold, and are unmistakable 
 in their meaning. These are : first, the scratches upon the 
 rocks ; second, the till or boulder clay ; third, the transported 
 boulders and terminal moraines. 
 
 First. Scratches' upon the Rocks. — All over the regions 
 which we have mentioned the harder and freshly uncovered 
 rocks show abrasion; they ai-e polished. This, however, might 
 have been done by the action of water in rolling pebbles and 
 gravel over them. But th is is not all. ■ They are scratched and 
 grooved as if the sand, gravel and pebbles, which abraded them. 
 
10 Glacial Period in America. 
 
 had been held in a firm grasp. These strise and furrows are, 
 in the main, parallel with each other, and they continue across 
 the hard portions of the rock as well as the softer. There are 
 places upon the shores, and among the Islands near the west 
 end of Lake Erie, where many acres together of rocks, thus 
 scratched and furrowed, are exposed, and where frequently the 
 furrows may be traced in a continuous line for a long distance. 
 These are effects which water alone could not produce. Water, 
 by giving motion to pebbles, may polish the rocks over which 
 they are moved, yet it docs not give the rocks an even surface, 
 but wears down the softer portions faster than the harder. 
 Only moving ice is competent to produce such polishing and 
 scratching as we have described ; and so extensive and uniform 
 is this striation that the theory of icebergs — majestic as they 
 are — is entirely inadequate to account for the facts. 
 
 Second. Till, or Boulder Clay. — The competency of water 
 for the production of the phenomena ascribed to glaciation is 
 excluded also by the character of the superficial deposit which 
 is everywhere found-over the area indicated. This deposit was 
 formerly called "boulder-clay," but, in scientific circles, now 
 goes by the name of "till," and its character is un i.istakable. 
 
 Till is an unstratified accumulation, and in this respect dif- 
 fers from all deposits which take place in water. Water is a 
 more perfect sieve tlian any of man's invention. It carefully 
 sorts whatever it transports, carrying along the finer material 
 farther than the coarse, and depositing it by itself. Now in 
 the till there is no such separation of the fine from the coarse 
 as water would secure. Fine clay, gravel, fragments of stone 
 of various sizes, sometimes several feet through, are mingled 
 in one indiscriminate mass. The larger part of the material 
 composing till is usually derived from the rocks of the vicinity; 
 but with this there are also mingled fragments that have been 
 brought from a longer distance, sometimes from localities hun- 
 dreds of miles away. A noticeable peculiarity of the pebbles 
 and fragments of rock which occur in till is that they too, like 
 the rock beneath, are scratched, and usually the direction of 
 the scratches on them is that of the longest diameter of the 
 fragments. 
 
Glacial Period in America. 11 
 
 Prom this description of till it will be recognized, by those 
 who have visited the glaciers of Switzerland, as similar to the 
 accumulation taking place beneath the glacier, and which is 
 called the "ground moraine." In short, the fine material of 
 the till may be compared to the dust with which a lapidary 
 polishes his gems, and the larger fragments to the tools with 
 which he engraves them. 
 
 Third. Transported Bovlders and the Terminal Moraine. — 
 A third evidence of the reality of the great ice movement of 
 which we are speaking, is to be found in the character, position 
 !ind limits of the transported material. This inti-oduces us to 
 the particular field of my own observations. There is a well- 
 defined southern limit to the marks of glacial action in the 
 United States. I have now followed that boundary line nearly 
 all the way from the Atlantic Ocean to the State of Illinois, 
 and can mark it upon the map with nearly as much confidence 
 and accuracy as I can that of the shores of Lake Erie. 
 
 a. There are some peculiarities in this line which it is worth 
 while to note, the first of which is the irregularity. As shown 
 upon the maps, the boundary of the glaciated region in North 
 America runs, opposite New England, through Nantucket and 
 Martha's Vineyard, and forms the backbone of Long Island, en- 
 tering New Jersey at Perth Amboy, Just below New York. 
 
 It was my privilege, several years ago, in a more definite 
 manner than had been done before, to call public attention to 
 the nature of these accumulations in. Southern New England. 
 I was enabled to do this through information furnished me by 
 Mr. Clarence King who gave me the facts in 1876, to be pub- 
 lished in a communication to the Boston Society of Natural 
 History upon the Glacial Phenomena of Eastern Massachusetts. 
 (See Proceedings, Vol. 19, p. 62, 1877.) When this clew had 
 once been furnished, it was a short matter to trace the line 
 along tlie southern shore of New England and through Long 
 Island. This work was done by Mr. Warren Upham. 
 
 By independent investigations Professors Cook and Smock, 
 of the New Jersey Geological Survey, discovered the signifi- 
 cance of certain glacial accumulations in that State, and a little 
 later published (Eeport on the Geology of New Jersey for 1878) 
 
12 
 
 Glacial Period in America. 
 
 a map of the Terminal Moraine in New Jersey. This runs by 
 au irregular course from Perth Amboy to Belvidere, on the 
 Delaware Kiver, a few miles above Easton. 
 
 PLATE 11. (taken from "Studies in Science Vnd Religion") shows, in addition to the 
 glaciated area of New Jersey, the glacial terraces of gravel along the Lehigh and Delaware 
 Rivers, and also the "Delta Terrace" at Trenton, fifty feet above the river, in which Dr. C. 
 C. Abbott has found palBBolithic implements. (For cuts, see Plates VL and VU., pp. 24, 25 ) 
 
Glacial Period in America. 
 
 13 
 
 From that point tha line runs in a general northwesterly 
 direction to the vicinity of Salamanca, N. Y., and thence 
 southwesteily into Boone county, Ky., across the river from 
 Cincinnati. Thence, by a circuitous route, hereafter to be de- 
 
14 
 
 Glacial Period in America. 
 
 scribed, it passes to the southwest corner of Indiana. So far 
 it has been accurately traced. From geological reports we 
 suppose it to trend across Illinois into Missouri, and thence in 
 a more northerly course into the States and Territories beyond. 
 Taken in their full extent, the curves in this boundary line 
 are both graceful and majestic, and may yet furnish to the 
 mathematician some clew as to the depth of the ice and the 
 distance of the centers from which it was dispersed. Various 
 minor curves in the line are also worthy of notice, one of which 
 appears in New Jersey, where near Eockaway the line makes 
 a right angle. One or two graceful curves are also noticeable 
 between the Delaware and Susquehanna rivers. Near Sala- 
 
 PLATE IV. Map showing Southern Boundary of Glaciated Area of Southern Ohio. 
 
Glacial Period in America. 
 
 15 
 
 LIST OF COUNTIES WITH NUMBERS COERESPONDINQ TO THOSE IN MAP. 
 
 No. I. 
 
 1. Williams. 
 
 23. Hardin. 
 
 45. 
 
 Pike. 
 
 2. Defiance. 
 
 24. Logan. 
 
 46. 
 
 Adams. 
 
 3. Paulding. 
 
 2.T. Champaign. 
 
 47. 
 
 Scioto. 
 
 4. Van Wert. 
 
 28. Clarke. 
 
 48. 
 
 Erie. 
 
 5. Mercer. 
 
 27. Greene. 
 
 49. 
 
 Huron. 
 
 6. Darke. 
 
 28. Clinton. 
 
 60. 
 
 Lorain. 
 
 7. Preble. 
 
 29 . Brown. 
 
 61. 
 
 Richland. 
 
 8. Butler. 
 
 30. Ottawa. 
 
 62. 
 
 Ashland. 
 
 9. Hamilton. 
 
 31 . Sandusky. 
 
 63. 
 
 Knox. 
 
 10. Fulton. 
 
 32. Seneca. 
 
 64. 
 
 Licking. 
 
 11. Henry. 
 
 33. Wyandot. 
 
 66. 
 
 Fairfield. 
 
 12. Putnam. 
 
 34. Crawford. 
 
 66. 
 
 Perry. 
 
 13. Allen. 
 
 35. Marion. 
 
 57. 
 
 Hocking. 
 
 14. Auglaize. 
 
 36. Morrow. 
 
 58. 
 
 Vinton. 
 
 15. Shelby. 
 
 37. Union. 
 
 69. 
 
 Jackson. 
 
 16. Miami. 
 
 38. Delaware. 
 
 60. 
 
 Lawrence. 
 
 17. Montgomery. 
 
 39. Madison. 
 
 61. 
 
 Cuyahoga. 
 
 18. Warren. 
 
 40. Franklin. 
 
 62. 
 
 Medina. 
 
 19. Clermont. 
 
 41. Fayette. 
 
 63. 
 
 Summit. 
 
 20. Lucas. 
 
 42 . Piclcaway. 
 
 64. 
 
 Wayne. 
 
 21. Wood. 
 
 43. Ross. 
 
 66. 
 
 Holmes. 
 
 22. Hancock. 
 
 44. Highland. 
 
 66. 
 
 Coshocton. 
 
 
 
 No 
 
 . II. 
 
 
 Adams 
 
 46 
 
 Hamilton 
 
 
 9 
 
 Allen 
 
 13 
 
 Hancock 
 
 
 22 
 
 Ashland(i2« ft. ab. sea 
 
 level) .52 
 
 Hardin (1871) , 
 
 
 23 
 
 Ashtabula 
 
 79 
 
 Harrison (1180) . . . 
 
 84 
 
 Athens 
 
 69 
 
 Henry 
 
 
 11 
 
 Auglaize 
 
 14 
 
 Highland (1136)... 
 
 44 
 
 Belmont (1170) 
 
 86 
 
 Hocking 
 
 Holmes (1235). 
 Huron (1050). . 
 
 
 
 
 29 
 
 
 . . 66 
 
 Butler 
 
 8 
 
 
 49 
 
 Carroll (1011) 
 
 83 
 
 Jackson 
 
 
 69 
 
 Champaign (1158)... 
 Clarke 
 
 26 
 
 
 85 
 
 26 
 
 Knox (1295)... 
 
 
 53 
 
 Clermont 
 
 19 
 
 Lake (1175)... 
 
 
 72 
 
 Clinton (1095) 
 
 28 
 
 
 
 60 
 
 Columbiana (1419).. . 
 
 82 
 
 Licking (1316) 
 
 
 64 
 
 Coshocton (1326).... 
 
 66 
 
 Logan (1560).. 
 
 
 24 
 
 Crawford (1176) 
 
 34 
 
 Lorain 
 
 
 50 
 
 Cuyahoga (1032) 
 
 61 
 
 Lucas 
 
 
 20 ■ 
 
 narke (1107) 
 
 6 
 
 Madison 
 
 
 39 
 
 Deliance 
 
 2 
 
 Mahoning (1208)... 
 
 81 
 
 Delaware 
 
 ....38 
 
 Marion 
 
 
 35 
 
 Erie 
 
 48 
 
 Medina (1117). 
 
 
 62 
 
 Fairfield 
 
 56 
 
 Meigs 
 
 
 70 
 
 Fayette 
 
 41 
 
 Mercer 
 
 
 6 
 
 Franklin 
 
 40 
 
 Miami -.. 
 
 
 16 
 
 Fulton 
 
 10 
 
 Monroe 
 
 
 .......87 
 
 Gallia 
 
 71 
 
 Montgomery.. 
 
 
 17 
 
 Geauga (12 -2) 
 
 73 
 
 Morgan 
 
 
 68 
 
 Greene 
 
 27 
 
 Morrow (1148). 
 
 
 36 
 
 Guernsey 
 
 77 
 
 Muskingum (1161). 
 
 67 
 
 67. Muskingum. 
 
 68. Morgan. 
 
 69. Athens. 
 
 70. Meigs. 
 
 71. Gallia. 
 
 72. Lake. 
 
 73. Geauga. 
 
 74. Portage. 
 76. Stark. 
 
 76. Tuscarawas. 
 
 77. Guernsey. 
 
 78. Noble. 
 
 79. Ashtabula. 
 
 80. Trumbull. 
 
 81. Mahoning. 
 
 82. Columbiana. 
 
 83. Carroll. 
 
 84. Harrison. 
 86. Jefferson. 
 
 86. Belmont. 
 
 87. Monroe. 
 
 88. Washington. 
 
 Noble 78 
 
 Ottawa 30 
 
 Paulding 3 
 
 Perry (1166) 66 
 
 Pickaway 42 
 
 Pike (1286) 46 
 
 Portage (1260) 74 
 
 Preble (1044) 7 
 
 Putnam 12 
 
 Richland (1400) 61 
 
 Ross 43 
 
 Sandusky 31 
 
 Scioto 47 
 
 Seneca 32 
 
 Shelby (1068) 15 
 
 Stark (1261) 76 
 
 Summit (1175) 63 
 
 Trumbull (1166) 80 
 
 Tuscarawas (1491) 76 
 
 Union 37 
 
 Van Wert 4 
 
 Vinton 68 
 
 Warren 18 
 
 Washington 88 
 
 Wayne (1276) 64 
 
 Williams 1 
 
 Wood 21 
 
 Wyandot 33 
 
16 Glacial Period in America. 
 
 manca, in New York, the change of direction is such as to 
 make an acute angle. Omitting various other deiiections in 
 Pennsylvania, you will notice several of a very marked charac- 
 ter in Ohio. 
 
 The boundary line enters Ohio near Palestine, in Colum. 
 biana county, and crosses the county in a direction a little 
 south of west, and as it enters Stark county, trends a little 
 to the north as far as Canton. Here it makes a sharp turn, 
 and runs almost south to the edge of Tuscarawas county, 
 entering Holmes county near its northeast corner, and contin- 
 uing in a southwesterly course to Millersburg, whence it trends 
 northwesterly to the southern township of Ashland county, 
 where it again takes a very sudden and decided turn to the 
 south, passing through the eastern edge of Knox county ; 
 thence through Newark, in Licking county, to the reservoir 
 in the northwestern part of Perry county, continuing in its 
 southerly course to Rushville in Fairfield county. Th:nce it 
 bends rapidly westward to Lancaster, and again, after crossing 
 the Hocking Valley, turns southward and runs along the boun- 
 dary between Pickaway and Hocking counties to Adelphi, in 
 the northeast corner of Ross county. Here again it bends 
 westward, crossing the Scioto Valley a few miles above Chilli- 
 cothe, turning again southward, near Frankfort, and bending 
 around so as to just graze the northwest corner of Pike county, 
 and cross the southeastern of Highland and the northwestern 
 of Adams, entering Brown county near Decatur, and run- 
 ning westward across the southern townships of Brown and 
 Clermont counties, and crossing the Ohio River into Kentucky 
 about two miles north of the line between Campbell and Pen- 
 dleton counties, whence it bends northward, keeping nearly 
 parallel with the river, and from three to eight miles south of 
 it, re-crossing the river near Woolpers Creek, five miles south 
 of Petersburg, and entering Indiana a little below Aurora. 
 
 In Indiana, the line still continues to bear in a southerly 
 direction through Ohio and Jefferson counties, grazing the edge 
 of Kentucliy again opposite Madison and reaching its southern- 
 most point near Charleston in Clarke county, Indiana. From 
 here it bears again to the north through Scott and Jackson 
 
"TL T I 
 
 PLATE V. Map of Southern Indiana, showing: 6laclal Boundary. 
 
18 Glacial Period in America. 
 
 counties to the line between Bartholomew and Brown, and fol- 
 lows this to the northeast corner of Brown. There again 
 it turns to the southwest, touching the northeast corner of 
 Monroe, where it again bears north for ten miles, to near Mar- 
 tinsville in Morgan coufity. Here again the line turns west 
 and south, passing diagonally through Owen, Greene, Knox, 
 and Gibson counties, and into Posey county as far as New 
 Harmony, where, for the present, I have left it. 
 
 To account for these curves is a problem to which we will 
 return a little later. 
 
 b. A second class of peculiarities to be noted in this bound- 
 ary line is its irregularity as to elevation. Nowhere is there 
 manifest any barrier such as would limit a body of water, and 
 the line rises over mountains and descends into the valleys with 
 apparent indifference. South of New England the accumula- 
 tions forming the terminal moraine are often below the level 
 of the sea, — the Elizabeth Islands and Block Island being 
 merely the surface of the moraine where it is partly buried in 
 the ocean ; so on across Long Island, Staten Island, and a good 
 part of New Jersey, the moraine is not far above the level of the 
 sea. West of the Delaware the line mounts the summit of the 
 Blue Eidge, 1,500 feet aboTC the sea, and descends in crossing 
 a transverse valley, a few miles to the north, 1,000 feet. It 
 ascends again, in a few more miles, the summit of Pocono 
 Mountain, which forms the watershed between the Delaware 
 and the Lehigh, and is 2,000 feet above the sea. Upon reach- 
 ing the east branch of the Susquehanna at Beech Haven, it has 
 again descended 1,500 feet, and it keeps on in a nearly uniform 
 course until it mounts the escarpment of the Alleghanies north 
 of Williamsport. From this point on to Salamanca the eleva- 
 vation varies from 3,000 to 2,500 feet. Once across the Alle- 
 ghanies the line works gradually to a lower level until it 
 reaches the southern partof Ohio, where it is still nearly 1,000 
 feet above the sea. 
 
 These facts by themselves clearly show that the boundary 
 line which we have traced, does not, as Dr. Dawson supposes, 
 mark the shores of an ancient sea, for if that were the case, 
 
Glacial Period in America. 19 
 
 there would have been a barrier to limit the sea, and that bar- 
 rier must have been upon the same general level, which, as we 
 have seen, is not the case. 
 
 Nor have there been any physical changes since the glacial 
 period sufficient to produce these diversities of elevation. The 
 Alleghanies were uplifted millions of years before the glacial 
 period. This is evident from the immense amount of erosion 
 which had taken place before the glacial period. Southeastern 
 Ohio and Western Pennsylvania are covered with the strata of 
 the coal measures, some outlying fragments of which are still 
 to be found as far east as the Susquehanna Valley. JSTow the 
 rivers in all this region flow along the bottoms of deep troughs 
 almost like canons, which in the course of ages have been cut 
 down by water through the parallel strata of sandstone, lime, 
 shale, and coal, which, in alternate layers, built up the great 
 structure of the carboniferous period. The extent and depth 
 of these narrow valleys of erosion are scarcely appreciated. 
 For fifty miles above Lock Haven, in Pennsylvania, the Phila- 
 delphia and Erie Railway follows up a narrow winding gorge, 
 in tlie west branch of the Susquehanna, which is ],000 feet in 
 depth. Instead of digging for the coal in this region they 
 ascend the summits of the hills. The Allegheny and the Ohio 
 rivers occupy similar troughs, which are from 300 to 500 feet in 
 depth. These are valleys of erosion, and every tributary of 
 these streams occupies a similar trough which it has cut for 
 itself. It is certain that the main lines of drainage upon this 
 continent do not now differ materially from those which have 
 existed from the very earliest time. 
 
 I say materially, because in minor respects the glaciation of 
 the continent produced many permanent changes in the drain- 
 age, and, for a temporary period, changes that were remarkable. 
 But, in the main, the watershed between the St. Lawrence 
 and the Mississippi has been, from the coal period on, a well- 
 defined and permanent feature in the physical geography of 
 the United States. The minor changes in the drainage of this 
 country have been largely due to the work of the glacial period. 
 Everywhere over the glaciated region the till, or ground mo- 
 raine, has been forced like putty into the gorges formed by the 
 
20 Glacial Feriod in America. 
 
 erosion of pre-glacial streams, so that nothing is more common 
 throughout this region than to find that the old channels have 
 been huried, and the streams forced to flow in new channels of 
 modern date. 
 
 c. A third peculiarity in the border of the glaciated region 
 is the character and amount of the accumulations marking it. 
 Along a considerable portion of this boundary line the accu- 
 mulations of glaciated material are immense. South of New 
 England the boundary is marked by a line of hills from 50 to 
 350 feet in height, and from two to three miles wide. Tiiese 
 hills are composed of loose material, thrown together in irreg- 
 ular hummocks and ridges, with many enclosed depressions to 
 which there ai'e no outlets, and which, from their shape, are 
 called "kettle-holes." Many large boulders, brought from a 
 long distance, are found scattered over these hummocks. 
 There can be no question that this is a terminal moraine, 
 marking the line from east to west, along which the ice-front 
 rested for a considerable period, and where, from century to 
 century, it deposited the burdens of rock and earth which it 
 had picked up in its journey from the north. This was the 
 line of battle between the frosts of the north and the tropical 
 winds of the south. Here, as the sun melted back the ice in 
 summer, the ice deposited its earthy material, and in the winter 
 regained its ground to repeat the process and beat a retreat the 
 following summer, and so on until these immense hills had 
 been deposited. In New England we can often trace the boul- 
 ders to ledges scores of miles to the north. Across New Jersey 
 these moraine hills continue upon a corresponding scale. 
 West of New Jersey the broken and mountainous character of 
 the country has frequently disguised the facts, so that they are 
 somewhat more diflBcult of discovery. But even here the gen- 
 uine features of a terminal moraine reappear so often that there 
 can be no question about the mode of its formation. We may 
 note especially a remarkable development of moraine hills upon 
 the level summit of Pocono Mountain. Here, for many miles, 
 and 2,000 feet above the sea, are almost exactly repeated the 
 features which we have described in Southern New England. 
 One may travel from the southward for a long distance, over 
 
Glacial Period in America. '21 
 
 an elevated plain wlin?c only covering of soil is a foot or two of 
 sand and angular fragments arising from the sub-aerial disinte- 
 gration of the underlying level strata of Pocono sandstone; 
 when suddenly, near Tobyhanna, he intersects the majestic 
 curve of moraine hills just referred to. Down to this limit 
 glaciated stones are piled in every imaginable confusion. Here, 
 in dense forests, are kettle-holes, many of which are still filled 
 with water, which slowly drains away through the loose mate- 
 rial near the rim. Here, in the debris which goes to form 
 these hills, are granite boulders which must be hundreds of 
 miles away from their native place. 
 
 Omitting for the present further reference to Pennsylvania 
 and coming to Ohio, we find in Columbiana county and the 
 eastern part of Stark county, that the accumulation of glacial 
 material along the front of the ice, is somewhat less marked in 
 quantity than farther east, but is the same in quality. Tlie 
 apparent diminution in quantity may arise from its having 
 been spread over a wider base. But, near the western part of 
 Columbiana county, at New Alexandria, two or three miles 
 back from the very extreme limit of glacial signs, the familiar 
 knobs and kectle-holes of the moraine are distinctly marked, 
 and that upon the very height of the laud. Wells are here 
 sunk from thirty to fifty feet without passing through the gla- 
 cial accumulation. A mile or two west of Canton, in Stark 
 county, the accumulations of glaciated material are upon a 
 scale equal to anything in New England. The northern part 
 of Holmes county is covered with till which is everywhere of 
 great depth, and in numerous places near the margin displays; 
 though in a molerate degree, the familiar inequalities of the 
 New England moraine. After the southern deflection in Knox 
 county, the glaciated region is entered near Danville, from tiie 
 east, on the Columbus, Mt. Vernon & Akron Kailroad, through 
 a cut in till a quarter of a mile long, and from thirty to forty 
 feet in depth. At the old village of Danville near by upon a 
 neighboring hill, wells are reported as descending more than a 
 hundred feet without reaching the bottom of the till. Through 
 Licking county, both north and south of Newark, the depth 
 of tht' glacial envelope is great up to within a short distance of 
 
22 Glacial Period in America. 
 
 its eastern edge. At the reservoir in Perry county the dis- 
 tinct features of a moraine come out. The hill upon which 
 Thornville is built is a mass of glaciated material in which 
 wells descend from thirty to fifty feet without striking rock. 
 This is upon the highest land of the vicinity. The reservoir 
 itself seems to be in a great kettle-hole or moraine basin. All 
 through Fairfield county the glacial accumulation is of a great 
 deplh down to a very short distance of its margin. But per- 
 haps the most remarkable of all the portions of this line in 
 Ohio is that running from Adelphi, in the northeast corner 
 of Boss county, to the Scioto River. The accumulation at Adel- 
 phi is more than two hundred feet, and continues at this height 
 for many miles westward. Eiding along upon its uneven 
 summit, one finds the surface strewn with granite boulders, 
 and sees stretching ofE to the northwest the magnificent and 
 fertile plains of Pickaway county, while close to the south of 
 him, yet marked by a distinct interval, are the clifEs of Waver- 
 ley sandstone rising two hundred or three hundred feet higher, 
 which here and onward to the south pretty closely approach 
 the boundary of the glaciated i-egion. 
 
 Passing over the intervening space, we note that in Boone 
 county, Kentucky, the accumulation of glacial matei'ial ex- 
 tends several miles south of the Ohio River, and many feet in 
 depth, and is here at an elevation of more than 500 feet above 
 the river. At an equal elevation similar accumulations appear 
 across the river in Indiana, west of Lawrenceburg, 
 
 At every step along the line, as thus triiced through Ohio' 
 granitic boulders of every size and shape and complexion are 
 to be found. The two largest measured were one in Colum- 
 biana county, near Hanovertown, which is thirteen feet long 
 by eleven feet wide, and which stands eight feet out of the 
 ground; and another near Lancaster, in Fairfield county, 
 which is eighteen feet long, twelve feet wide, and stands six 
 feet out of ground. These are granite boulders, wliose native 
 ledges are in Canada, far to the north of Lake Erie. Boulders 
 from three feet to five feet in diameter are too numerous to 
 mention. 
 
Glacial Period in America. 
 
 SOME GBKEEAL CONCLUSION'S. 
 
 Several interesting subsidiary considerations are connected 
 with this subject: 
 
 First. The Glacial Period and the Interests of Agriculture 
 and Health. — In this State, and probably further west, the 
 prairie region is seen to have been a product of the glacial 
 period. It was the moving ice of that period which wore down 
 the prominences and filled up the depressions to produce the 
 dead level or gently rolling surface of all this prairie region. 
 The action of running streams produces fertile intervales in 
 narrow valleys, but the sheet of ice that pressed over our con- 
 tinent ground up the rocks, and spread the detritus over the 
 whole surface. In the level regions of the West the soil is 
 nearly everywhere fei tile. A noticeable quality in the soil of the 
 glaciated region is the mixture of the elements composing it. 
 All the rocks to the north have contributed to its composition. 
 In the soil of Lorain county, for example, there are found the 
 pulverized fragments of various granites from Canada, of the 
 limestones of the Sandusky group, mingled with those of the 
 neighboring shales and sandstones. All these elements have 
 been kneaded together into one homogeneous mass by the mov- 
 ing ice, as the housewife kneads her flour and yeast together. 
 
 The legislators of the Statj do not yet fully appreciate the 
 economical and sanitary bearings of glacial investigations. The 
 ice movement of the glacial pc>riod pretty much made the in- 
 habitable portions of this State. It determined the character 
 of the soil, the contour of the country, the minor lines of drain- 
 age, and thus in a thousand ways had to do with the pleasure, 
 the health, and the prosperity of the present population. As> 
 a few weeks ago, I marked off the glacial limits on a map of 
 this State, the Secretary of the Board of Agriculture at once 
 remarked to me'that that was the southern boundary of the 
 great wheat-produeing portion of the State, and expressed an 
 earnest desire that Ohio might secure as thorough an examina- 
 tion of the glacial phenomena within its bounds as has been 
 done by New Jersey. Certainly if one is to buy a farm in 
 Ohio he should pray that it be either in a river valley or north 
 of the terminal moraine. Of course this is to be taken as a 
 
24 Glacial Period in America. 
 
 general statement, to which there are exceptions; but even 
 then it will be found that the exception proves the rule. 
 
 Second. Relation to Arclimology. — Dr. 0. C. Abbott re- 
 ports that he has found palssolithic implements (one of which 
 is shown in the accompanying cut, together with one from 
 France for comparison) stratified with the gravel forming the 
 terrace of the Delaware Eiver, at Trenton, N. J. I have re- 
 peatedly visited that place with Dr. Abbott, and in company 
 
 PLATE VI. The palaeolith here shown is natural size, and is No. 3034 of the Mortillet 
 collection from Abbeville, France. The geological conditions under which this was found 
 are very similar to those of the palseolith from Trenton, N. J. 
 
Glacial Period in America. 
 
 25 
 
 PLATE VII. This palseolith i8 shortened one inch in the cut, and is proportionally nar- 
 row, the original being- 5 6-8 inches long and 8 1-8 wide. This is No. 19723 in Dr. Abbott's 
 collection from Trenton, N. J. The Mortillet and Dr. Abbott's collections are both in the 
 Archaeological .Museum, in Cambridge, Mass., where these specimens can at any time be 
 seen. No 11)7-3 is specially interesting, because Professor Putnam took it with his own 
 hands out of Trenton gravel from behind a small boulder which was firmly embedded four 
 feet below the surface of the soil. (See Proceedings of Boston Society of Natural History, 
 Vol. XXI , p. 149.) For the geological condition, see Plate II., p. 12; for a more detailed 
 account, see "Studies in Science and Religion," Chapter VI. 
 
26 Glacial Period in America. 
 
 with Professor Dawkins of England and Professor H. W. 
 Haynes of Boston, — two of the highest authorities upon palaeo- 
 lithic implements that can be found in the worlds — and they 
 testify that the implements found by Dr. Abbott, both in 
 their form and in the situations in which they occur, closely 
 correspond to those which have been so carefully studied in 
 northern France and southern England. 
 
 An examination of the terraces along the Delaware at once 
 brings these implements into definite relation to the glacial 
 period. The gravel in which they are found is glacial gravel 
 deposited upon the banks of the Delaware when, during the 
 last stages of the glacial period, the river was swollen with vast 
 fl.oods of water from tlie melting ice. Man was on this conti- 
 nent at that period when the climate and ice of Greenland ex- 
 tended to the mouth of New Yoi-k harbor. The probability 
 is that if he was in New Jersey at that time he was also upon 
 the banks of the Ohio, and the extensive terrace and gravel 
 deposits in the southern part of our State should be closely 
 scanned by archaeologists. When observers become familiar 
 with the lude form of these palaeolithic implements they will 
 doubtless find them in abundance. But whether we find them 
 Or not in this State, if you admit, as I am compelled to do, the 
 genuineness of those found by Dr. Abbott, our investigations 
 into the glacial phenomena of Ohio must have an important 
 archaeological significance, for they bear upon the question of 
 the chronology of the glacial period, and so upon that of man's 
 appearance in New Jersey. 
 
 To appreciate the bearing of glacial studies upon this ques- 
 tion we must return to study the old water courses which ex- 
 isted in glacial times. As you can see, a special interest attaches 
 to those rivers which rise in the glaciated region and in the 
 lower part of their course flow through the unglaciated. Man 
 lived first below the glacial limit, and fished upon the banks of 
 the streams which were periodically gorged with the spring 
 freshets of the glacial period, and during those floods lost his 
 spear-heads, his hammers, his axes and scrapers, where they be- 
 came mingled with the gravel brought down from up the stream. 
 The Delaware River happens to be the first stream west of the 
 
Glacial Period in America. 27 
 
 Atlantic whose source is in tlie glaciated region and wlios-o 
 month is in the unglaciated. But, in following the terminal 
 moraine westward, we are continually crossing streams which 
 are similarly situated; such are, in Pennsylvania, tiie Lehigh, 
 the east branch of the Susquehanna, the various ci'eeks which 
 empty into the west branch of the Susquehanna, and those 
 which empty into the Allegheny Eiver; all of which, I can 
 testify from personal inspection, substantially repeat in their 
 terrace formations the phenomena along the Delaware Eiver, 
 where it passes from tlie glaciated to the unglaciated region. 
 Where these streams emerge from the glacial region there are 
 uniformly immense deposits of granitic pebbles and coarse 
 gi'avel, and, for long distances below, teri'aces of finer gravel 
 far above the present high-water mark. 
 
 Ohio abounds in streams similarly situated, among which mi.y 
 be mentioned the forks of the Beaver and Sandy Creeks, in 
 Columbiana county; theNimishillin, the Tuscarawas, and Sugar 
 Creek, in Stark county; the Killbuck and Mohican, in Holmes 
 county; the Licking, in Licking county; Jonathan Creek, in 
 Perry county; the Hocking River and Muddy Prairie Run, in 
 Fairfield county; and Salt Creek, the Scioto, and the forks of 
 Paint Creek, in Ross county. To this list may also be added 
 the Ohio itself. 
 
 The Ohio is in every respect unique in its relations to the 
 glacial period. Through the whole of its course from Pitts- 
 burg to Caii'o, it is, roughly speaking, parallel with the ter- 
 minal moraine, and all along its course has received from the 
 north the contributions of water and ice and gravel which 
 poured down from the decaying ice-front but a short distance 
 away. And now the discovery of glacial deposits in Campbell 
 and Boone counties, Kentucky, adds another exceedingly inter- 
 esting feature to the problem. Here, as we have seen, the ice 
 actually crossed and projoctt'd several miles south of the Ohio 
 River. From the elevation at which these accumulations occur 
 it is certain that the ice-barrier at Cincinnati must have been 
 at least six hundred feet. This would set the water of the 
 Ohio beyond Pittsburg, far up into the Allegheny and Monon- 
 gahela rivers, submerging Pittsburg itself to a depth of about 
 
28 Glacial Period in America. 
 
 three hundred feet. This discovery helps to explain some facts 
 observed a year ago in our survey of the moraine in Pennsyl-' 
 vania. We shall expect to find this theory verified by a variety 
 of observations upon the upper course of the Ohio and its trib- 
 utaries. We shall expect to find also, in Kentucky, some indi- 
 cations of the outlet of this temporary glacial lake. 
 
 It is interesting to reproduce by the imagination the form 
 and appearance of this lake. The barrier probably was not 
 high enough to submerge all the highlands of southeastern 
 Ohio, or of northern Kentucky and of West Virginia; but long 
 bays must have stretched up on the north through all the val- 
 leys to the ice-front. Thus the glacier in southeastern Ohio 
 would for awhile seem to terminate in an archipelago. How 
 long this condition of things existed it is impossible to tell 
 with certainty, but from the limited amount of the deposit 
 south of the Ohio Eiver a relatively brief period is indicated. 
 Tlie Ohio Valley, both before and after the formation of this 
 ice-barrier, must have presented inviting haunts for paleolithic 
 man. It is of the utmost importance to archaeology that the 
 gravels of this valley should be carefully scanned. Probably 
 there is nowhere in the world so inviting a field for such inves- 
 tigation as the banks of the Ohio and its tributaries. 
 
 Thikd. Date of the Glacial Period. — I have time to say but 
 a word upon the field which is opened before us in this State for 
 making calculations as to the date of the close of the glacial 
 opoch. It is not well for the geologist to abandon his own chro- 
 nological data for the confessedly uncertain speculations of 
 astronomers upon this subject. Geologists have scarcely begun 
 the systematic study of the evidences bearing upon the date of 
 the glacial period. The evidences are three-fold: First, the 
 amount of the glacial deposit; second, the extent of erosion 
 since the glacial epoch; third, the extent to which glacial 
 depressions have been filled with sediment. 
 
 The opportunities to estimate the extent of erosion since the 
 glacial epoch are superabundant in Ohio. Each of the larger 
 streams emptying into the Ohio Eiver and into Lake Eiie, and 
 every tributary of those streams, presents a field by itself. In 
 
Glacial Period in America. 29 
 
 countless cases it is within our power to estimate with reason- 
 able accuracy the number of cubic yards of material which the 
 streams in the glaciated regions have removed from the till 
 through which they flow. This would give us the dividend. 
 It is by no means improbable that the re are also m;my streams so 
 nearly in their primitive con,dition that the rate of removal can 
 be approximately estimated. This would give us the divisor. 
 The quotient would give us the chronology of the close of the 
 glacial period. The other hopeful field for chronological inves- 
 tigation in this State is presented in the numerous lakes which 
 exist over the glaciated surface, and which, in most cases, owe 
 their origin to the irregular deposition of till. It is not beyond 
 hope that some of these may yield us the secret of their age. 
 It may be po sible to ascertain how deep a layer of sediment 
 and peat has accumulated, and we may discover more specific 
 facts concerning the rate of such accumulation. For a fuller 
 discussion, see Chapter VI, in my "Studies in Science and 
 Eeligion," Andover, W. F. Draper, 1883. 
 
 Fourth. Centers of Glacial Dispersion. — Another topic to 
 which we should give more attention relates to glacial move- 
 ment, and to the centers from which the ice was dispersed. 
 Ice, it should be remembered, behaves not like a solid but like 
 a semi-fluid. If an oblong block of ice be suspended upon the 
 ends it will gradually sag in the middle. If a strong hollow 
 sphere be filled with water, and a good-sized orifice be left 
 through which the ice may escape, and the whole be subjected 
 to intense cold, the ice will project through the hole for a con- 
 siderable distance. As a matter of fact, ice flows like cold 
 molasses or half-hardened lava. 
 
 It is not necessary (as some might suppose) to have a steep 
 declivity in order to secure glacial motion. Ice can move 
 wherever water would run. In our conceptions of glacial 
 movement we are in danger of having our ideas cramped by 
 the contemplation of Alpine glaciers. The demands made 
 upon our imagination by the glacial phenomena of North 
 America are almost staggering to reason. We are called upon 
 to believe that along a line thousands of miles in extent the 
 ice-front of the great glacier rested upon land which is no- 
 
30 Glacial Period in America. 
 
 where much lower — and in many places is actually higher — 
 than the region from which it was dispersed. Boulders, in 
 many cases, have been raised to a higher level than their native 
 ledges. 
 
 Upon reflection, however, this is not so paradoxical as at 
 a first glance it seems. It should be remembered that glacial 
 ice is formed, not by the freezii.g of water upon Likes and 
 oceans, but by the accumulation of snow, which, under its own 
 pressure, becomes converted into ice. If, now, over an exten- 
 sive level surface there should be precipitated annually six feet 
 more of snow than melted, six thousand feet of ic(^ would accu- 
 mulate after a thousand years. It is thus easy to see that after 
 a time the ice might form a mountain plateau by itself, and, 
 owing to its semi-fluid character, it would gradually move away 
 along whatever lines presented the least resistance. Such accu- 
 mulations about the north pole would everywhere move to the 
 south, and so we could get this southerly motion from the mere 
 accumulation of ice about the pole, without supposing any 
 change of level. 
 
 It is easy, also, to see that wherever — from climatic causes 
 over any particular portion of this field — there should be an 
 excessive accumulation of snow, that area would form a sub- 
 center by itself, and project the ice-front in a loop south of the 
 main line. The existence of such sub-centers I suppose to be, 
 in part, the explanation of the various loops and irregular 
 flexures which mni'k the glacial Loundary in North America. 
 
 Nor is it diflScult to conceive how boulders arc- raised in the 
 ice to a higher than their original level. Indeed, I ihink I can 
 conceive that fragments of rock can be picked up from beneath 
 the glacier, and after movement over sufBcient distance appear 
 ujion its surface; and I can easily believe that many of the 
 well-known gl.iciated boulders scattered over the surface of 
 Ohio have been repeatedly transferred from beneath the ice to 
 its surface, and thence projected to the foot of the advancing 
 ice-front, and afterwards rc-elevated and projected again. 
 This might be brought about as follows: 
 
Glacial Period in America. 31 
 
 It is well known that the upper strata of glacial ice move 
 faster than the lower, owing to the effect of friction in retard- 
 ing the movement at the bottom. The result of this is that 
 the upper side of the boulder which is imbedded in the ice is 
 constantly subjected to a greater degree of onward pressure 
 than the lower side. The effect 0/ this must be to give an 
 upward as well as an onward motion to the boulder in the ice. 
 The courseof such a boulder would beupa very gently inclined 
 plane, the slower moving strata beneath it forming the incline, 
 and the more rapidly moving upper strata being the force 
 to push it along. Once upon the surface, if the motion were 
 to continue long enough and the front were not too far away, 
 the boulder might be transferred to the front and deposited 
 befo:e the moving mass; and if the glacier were still advanc- 
 ing, it would stand a chance to be covered again with ice, and to 
 be re-incorporated in the moving mass to repeat another cycle. 
 
 CONCLUSION. 
 
 The glacial boundary line marked upon the maj) of Ohio is 
 easily drawn when yon know where to draw; but in reality it 
 is about two hundred and fifty miles in length, and its deter- 
 mination could be secured only by exploring a belt about ten 
 miles wide, and by travelling in the field a distance of more 
 than one thousand miles. I have now zigzagged this line for 
 the larger part of the distance from the end of Capo Cod to 
 Illinois, and you will pardon me for entertaining some en- 
 thusiasm upon the subject, .and for having my imagination 
 pretty well filled with the theme. The ice period of North 
 America seems to me no longer a myth, but a reality. With 
 my mind's eye I have seen it; I have walked along its front; 
 I liave beheld its glassy surface as it overlapped the mountain 
 ranges of Pennsylvania, walled up its ancient river channels, 
 filled up the depths of Lake Erie, and spread itself over the 
 fairest fields of Ohio; and again I have seen it in its retreat, 
 when its thickness was diminished, when its decaying southern 
 border was obscured by the accumulations of materials which 
 now form the moraine. I have seen it when the great streams 
 
•32 Glacial Period in America. 
 
 of water from its melting surface had worn a series of parallel 
 gorges in it along the line of the present water courses. In 
 imagination I have witnessed the enormous annual rise of the 
 streams during the declining years of the glacial period. I 
 have seen the hardy palseolithic race who fished in these streams 
 and hunted upon their banks, and were hastily driven from 
 their homes by the rise of floods whose volume we can 
 scarcely comprehend. To the mental vision of him who goes 
 over this field all these things become realities. He has seen 
 their signs: he has interpreted their handwriting. 
 
 I commend the study to the professional and business men 
 who need to seek recreation and health in outdoor pursuits. 
 Now that the buffalo is becoming scarce, and trout fishing un- 
 remunerative, we present to you for your vacation work the 
 enticing sport of hunting for the terminal limits of the great 
 American ice sheet, and for its imbedded marks of paleolithic 
 man. 
 
PLATE Vm. 
 Six miles to an Inch. 
 
 PLATE IX. 
 
DETAILED REPORT 
 
 OF 
 
 INVESTIGATIONS ALONG THE BOUNDARY 
 
 OF 
 
 The Glaciated Area in Ohio and Indiana, 
 
 ■ CONDUCTED BY 
 
 PROF. G. FEEDERICK WRIGHT, OF OBERLIN, OHIO, 
 IN THE SUMMER OF 1882. 
 
 COLUMBIAKA COUNTY. 
 
 The boundary line of the glaciated region as it enters Ohio 
 from Pennsylvania, is not so distinctly marked by large ac- 
 cumulations of till as ill many other places ; so that it might 
 create misapprehension to speak of a "terminal moraine" in 
 Columbiana county. Still the boundary is well defined, and 
 on penetrating the glaciated region a few miles, the accum- 
 ulation of till is extensive. As we approached the Ohio line 
 through the western counties of Pennsylvania, it was observed 
 that what we have called " the fringe " became more extensive 
 than in the eastern part of the State; tliat is, scattered granitic 
 boulders and occasional accumulations of till are found in 
 some places five or six miles south of the line bounding the 
 continuous accumulation of till which envelops the larger part 
 of the glaciated region. This peculiarity continues through 
 Columbiana county, from east to west, and as far as Canton 
 in Stark county. 
 
 For example: The accumulations of till worthy of being 
 called a "terminal moraine," and of being reckoned as a con- 
 tinuation of that which marks the boundary of the glaciated 
 region in New Jersey and Pennsylvania, enters Ohio at Pales- 
 tine, Coluaibiana county, near the boundary of Unity and 
 Middleton townships. The wagon road from Darlington to 
 Palestine enters a great accumulation of till, near John Harts- 
 horn's, about one-half mile south of the Pittsburgh, Ft. Wayne 
 and Chicago K. E., and one mile east of Palestine. Here, 
 
36 Detailed Report for Ohio. 
 
 upon the land of the State Line Coal Works, upon a hill 
 sloping to the north, is a striking collection of granitic bould- 
 ers, one of which measures 9x6x4 feet. In the valley to the 
 north, through which the railroad runs, the accumulations of 
 drift show the modifying action of ihe glacial currents which 
 characterized the closing stages of the glacial period. The 
 broken ridges and knobs of gravel, alternating with shallow 
 kettle-holes, remind one of the kames in Now England. Pal- 
 estine is built upon such a formation. A large granitic boulder 
 was here observed, in a freshly dug grave, five feet below the 
 surface. A well was reported as penetrating till for fifty feet 
 without striking the bed rock. Three-quarters of a mile 
 southwest from Palestine, a cut shows twenty feet of till : but 
 boulders of granite and scratched stones with an occasional 
 slight deposit of till, were found several miles further south, 
 on the summits of the hills. We walked from Smith's Ferry, 
 on the Ohio River, northward over the liills, to a point on 
 the State line east of Achor, in Middleton township, with- 
 out finding any signs of glaciation. Here granitic boulders 
 began to appear near Danison's coal bank. On the summit 
 of the hill one-half mile west of Achor, and about 200 feet 
 higher than the bed of Little Beaver creek, is a granitic boulder 
 5x3x3 feet. From this point northward to the moraine at 
 Palestine, these scattered but unmistakable evidences of the 
 presence of the glacier ice are found upon all the hill-tops. 
 
 After this description of the fringe, and its relation to the 
 moraine, we may pass more rapidly over the subject. The 
 boundary of the fringe runs south-westward from Achor to 
 Clarkson post office, thence to the southeastern corner of Elk 
 Run township; thence westward along the southern line of 
 this township to the southeastern corner of Centre township; 
 thence it bears northerly, striking the line of Hanover town- 
 ship two miles northeast of Dungannon, thence westerly and 
 bearing a little south through Hanover township, passing one- 
 half mile south of Hanoverton Post Office, continuing west to 
 Bayard. At Rochester there is an extensive kame-like deposit 
 filling the valley, which is here about; one-half mile wide, in 
 which are numerous granitic pebbles from three to six inches 
 
Detailed Seport for Ohio. 37 
 
 in diameter. One of these gravel ridges, running north by 
 south, measured a little over 30 feet in height, with a slope of 
 20°. This cluster of kames is evidently due to the glacial 
 floods pouring down the two branches of Big Sandy creek, 
 which here unite. The accumulations of gravel in the valley 
 of Big Sandy creek gradually diminish in amount and in 
 coarseness from here on to Minerva, in Stark county. The ice 
 all along here filled the valley and rose to the summit of the 
 hills on the south. One boulder was found in the north, 
 western corner of Augusta township, Carroll county, but an 
 extensive detour of several miles to the south failed to dis- 
 cover any other signs of glaciation in that county. On re- 
 turning to Bayard, till was found one-half mile southwest, 
 rising upon the hills south of the valley to a height of 50 or 
 60 feet. One-half mile northwest of Bayard is a terrace 31 
 feet above the present flood-plain, enclosing a shallow, but 
 extensive, kettle-hole between it and the hills to the north. 
 
 Eetracing now our steps we find that from three to five 
 miles north of the edge of this fringe there is a marked in- 
 crease in the accumulation of till showing itself at East Pal- 
 estine and near East Carniel Post Ofiice. Thence across Elk 
 Eun township through Elkton to New Lisbon. The north- 
 east part of Centre township is completely enveloped with till 
 of an unknown depth. Three miles from New Lisbon and a 
 quarter of a mile west, on the road to Teegarden, is a boulder 
 of gneiss 8|x6^ feet, 4 feet out of ground. At and below New 
 Lisbon, in the valley of the Middle Pork of Beaver, are the 
 extensive accumulations of pebbles and coarse gravel which 
 everywhere mark the streams as they issue from the line mark- 
 ing the terminal moraine. The terrace at New Lisbon shows 
 no distinct stratification, and contains numerous pebbles from 
 10 to 15 inches in diameter, and at the railroad station is 36 
 feet above the river. Upon the north side, this extends for 
 one mile down the stream. Still further down, similar ter- 
 races appear at intervals nearly to Elkton. The gravel in all 
 these terraces is mined for kidney ore. 
 
 Prom New Lisbon west, the moraine runs through the north- 
 ern part of Sections 33, 23, 31, 30 and 19 in Centre township. 
 
38 Detailed Report for Ohio. 
 
 In Hanover township it passes directly west, througli the 
 northern part of Sections 34, 23, 23, 21, 20 and 19. Two and 
 a half miles northeast of Hanoverton, on the farm of Mr. 
 Kinnely, the moraine is well developed, displaying its charac- 
 teristic hummocks and kettle-holes upon the summit of the 
 country. Large boulders are here very numerous, many from 
 3 to 5 feet in diameter. A mile or two farther north, near 
 the state road, on the farm of Francis BIythe, is a granitic 
 boulder 13x11 feet, 8 feet out of ground. Till is here certainly 
 16 feet deep, but how much more we could not ascertain. 
 
 Through West township the moraine bears slightly north, 
 passing through the village of New Alexandria, which is sit- 
 uated upon a height of land, and surrounded by hummocks 
 and kettle-holes of moderate size. Wells are reported 27 feet 
 and 50 feet without striking rock. This continues through 
 New Chambersburg, where wells were reported on the farm of 
 Henry Bowers as going 27 feet without striking rock, the 
 lower 6 feet in gravel an 1 sand. 
 
 STARK COUNTY. 
 
 The boundary line of the fringe in Stark county runs from 
 Bayard northwest through Paris and Osnaburg townships, 
 passing tiirough the villages of Kobertsville and Osnaburg. 
 Boulders of large size are found a little back from this line in 
 the eastern part of Paris township, some of them measuring 
 between 7 and 8 feet. Two and a half miles southeast of Paris 
 post office the last indications of ice-action are a few boulders 
 in Section 15, one measuring 4x3x3 feet. West of Osnaburg 
 the fringe becomes merged with the main accumulation. 
 
 The moraine proper passes through the northern sections of 
 Paris and Osnaburg townships. One mile east of Paris post- 
 office granitic boulders are numerous, and cuts in the till show 
 it to be at least 10 feet deep upon the hills, and probably 20 
 feet. _ Three-quarters of a mile southwest of Paris, in the val- 
 ley of Black Creek, the terrace of water-worn material is 15 feet 
 above the stream, which is here small. The terraces are par- 
 tially ridged, and cont vin shallow kettle-holes. On the farm 
 of D. P. Sell, Section 6 of Paris township, wells are reported 
 
Detailed Beportfor Ohio. 39 
 
 30 feet deep, the first 8 feet being yellow till, the remaining 22 
 feet blue till. Another, 20 feet deep, ended in quicksand. This 
 is on the high lands. Till completely envelops the southeastern 
 corner of Nimishillin and the northeastern of Osnaburg town- 
 ships. Kettle-holes are also apparent on the farm of H. Miller. 
 In Section 2, Osnaburg township, on the farm of G. Hennigs, 
 wells are reported 18, 30 and 26 feet, all in till. On a little 
 higher land, in the southwest corner of Section 2, J. Anthony 
 reported a well 14 feet through till. Till of unknown depth 
 completely envelo^js thQ region for three miles south of Louis- 
 ville post ofBce. There are kame-like ridges in Section, 3 Osna- 
 burg township, in a shallow valley along a branch of East Nimi- 
 shillin Creek. The whole appearance of the 'country is as if 
 filled up with till. Till continues on the road from Louisville 
 to Osnaburg, where it suddenly ceases, at the corner of the 
 diagonal road running to Kobertsville. Prom Osnaburg south- 
 west, for throe miles, thence northwest three miles towards 
 Canton, not a pebble or boulder was discovered. Much of the 
 way the road is on high land, deep valleys opening southward- 
 it being on the watershed between Nimishillin and Big Sandy. 
 On crossing a small branch of the Nimishillin two and a half 
 miles southeast of Canton, in the southwestera corner of Sec. 
 tion 14 in Canton township, we struck suddenly into till on the 
 north bank. Prom this point to Canton City till is continuous 
 and granitic boulders are abundant. The depth of the till is 
 unknown, but at various places cuts show it to be at least sev- 
 eral feet deep. Sections 11 and 12, north of the Osnaburg road, 
 are completely enveloped with till. A few rods northeast of 
 the cemetery, about one mile east of Canton, are shallow ket- 
 tle-holes in till. Upon the east branch of the Nimishillin the 
 terrace facing the stream and a short distance back is 41 feet 
 above the floood-plain. This contains m;iny pebbles 16 inches 
 and more in diameter. All are well rounded, and many are of 
 local material. The cemetery, 20 rods farther east, is 16 feet 
 higher, and is upon till. On the west side of the west branch of 
 the Nimishillin the terrace rises in successive stages more than 
 80 feet, and its surface is very uneven. A mile and a half south 
 of the city, below, the junction of the two branches, there are 
 
40 Detailed Report for Ohio. 
 
 two ivell-mai'ked terraces, the first of which is much the broader, 
 and is 38 feet above the bed of the stream. The upper terrace, 
 on the east side, is 36 feet higher, or 74 feet above the stream. 
 The pebbles in the upper terrace were a mixture of granite and 
 local rock, some of them a foot or more in diameter. One 
 granitic pebble was more than 2 feet in diameter. The terrace 
 on the west bank, near the Starr Mills, was by measurement 5 
 feet higher than that on the east. 
 
 A remarkable cluster of kame-like ridges covers the north- 
 western portion of Canton township and the northeastern of 
 Perry, extending an unknown distance to the north. Meyer's 
 Lake and Sippo Lake are enormous kettle-holes, and the whole 
 region has much the appearance of Plymouth township in 
 Massachusetts. Upon the south this kame-like belt is called 
 Buck Eidge, and comes to a sudden termination near the cross- 
 ing of the Fort Wayne and Chicago Kailroad, two miles south- 
 west of Canton City. Here an excellent section is made by the 
 railroad. The kame rises 85 feet above the railroad, is coarsely 
 stratified in places, contains many granitic pebbles (one of which 
 measured 55x40x18 inches), and was 31^ feet higher than the 
 railroad. There were large spaces in which no stratification 
 appeared. There were pebbles upon the summit from 3 to 5 
 inches in diameter. The section exposed shows a base of 570 
 feet, with an altitude of 85 feet. The slope upon the east side 
 varies from 18° to 25'^; on the west side it is a little more gen- 
 tle. (See cut in Geological Survey Ohio, vol. 2, p. 44.) An 
 extensive sandy plain, full of gentle swells and ridges, stretches 
 to the westward, while the space towards Canton is occupied 
 by the more nearly level terrace. About 150 yards north of 
 this section is a dry kettle-hole 25 feet deep.containing a granitic 
 boulder 51x35x31 inches. Another dry kettle-hole near by is 
 about 300 feet long, 200 feet wide, and 40 feet deep, with sides 
 sloping inward 24". The riins of these kettle-holes are at the 
 summit of the kamo. 
 
 Prom my experience elsewhere, I should expect to be able to 
 trace a series of kames northward from this point, and find it 
 enclosing the lakes in the southern part of Summit county, 
 and particularly abundant south of Akron. 
 
Detailed Seportfor Ohio. 41 
 
 From Canton westward the fringe pretty much disappears, 
 and the moraine bears rapidly southward, running across the 
 southeastern corner of Perry township, and continuing in a 
 south-southwestern course to the southern part of Bethlehem 
 township, crossing the Tuscarawas Eiver about two miles above 
 Bolivar; thence it bears more westward, crossing the southeast- 
 ern portion of Sugar Creek township, and the northwestern 
 corner of Wayne township in Tuscarawas county, entering 
 Holmes county east of Weinsburg. 
 
 It is difficult to exaggerate the sharpness of this portion of 
 the boundary line. Retracing our course, our notes show that 
 the line bounding the till passes through the middle of Section 
 29 Canton township, where it crosses a small stream running to 
 the north. This, like many other similar cases, showed signs 
 of having been dammed up, thus producing a small temporary 
 glacial lake. To the north and west the till is continuous, and 
 probably of great depth; to the east it suddenly disappears, 
 half way up a low hill. From Richville to the southeastern 
 corner of Perry township till and boulders are continuous, and 
 the deposit apparently of great depth. One of the boulders a 
 short distance beyond the till measured 6x4| feet. A detour 
 through Section 6, Pike township, and Section 32, Canton 
 township, demonstrated a total absence of glacial signs in that 
 region. The whole country to the southeast was broken and 
 hilly, in striking contrast to that in the opposite direction, 
 which seems to have been leveled up by glacial material. Upon 
 the hills in Section 1, Bethlehem township, cuts in the till 6 
 feet in depth disclose large granitic boulders lying still deeper. 
 The road running south, between Sections 11 and 12, and 13 
 and 14, is upon the very edge of the glaciated region. Detours 
 of a few rods to the east lead into a region in which there is only 
 rock in place and the soil formed by its disintegration. South- 
 westward from this point to the river, the boundary is near an 
 unfrequented road passing one-half mile north of the first 
 Moravian settlement in thiij region. 
 
 At the upper end of the great ox-bow in the Tuscarawas River 
 upon which Bolivar is built, but on the north side of the river, 
 is an immense kame-like accumulation, containing boulders 
 
42 Detailed Refortfor Ohio. 
 
 from 2^ to 3 feet in diameter. The terrace is here 36 feet above 
 the river, and the kame-like accumulation is 118 feet higher. 
 The space included in the ox-bow is occupied by a gravel deposit 
 whose surface is 51 feet above the river. Prom this point down, 
 the river occupies a narrower valley, with diminishing terraces. 
 Five miles below, at Zoar, wells in this terrace 30 feet deep do 
 not go through the gravel. Above the ox-bow, and on the west 
 side of the river — opposite the kame-like deposit just described 
 — the terrace is 61 feet, which continues up the river a mile or 
 more without change. 
 
 Going west along a road near the county line in Bethlehem, 
 a little till appeared when the higher land was reached, but on 
 ascending the hills to the left (south) it disappeared, and is 
 wholly absent in the extreme southwestern corner of Bethle- 
 hem township. But the hills in Section 30, immediately to the 
 north, are covered with till containing large granitic boulders, 
 some of which are between 3 and 4 feet in diameter. Till is 
 continuous, and of unknown depth, all the rest of the way to 
 Navarre, displaying to some extent the familiar kettle-holes 
 and knolls of the moraine belt. The small streams emptying 
 north also display the well-known signs of temporary ice-dams. 
 One of the numerous boulders of red granite over this area 
 was between 200 and 300 feet above the Tuscarawas Kiver, 
 and measured 7x5 feet, 3 feet out of ground. 
 
 The characteristics of the moraine just described continue 
 through the southern portion of Sugar Creek township, cross- 
 ing Sugar Creek below Beech City. One and a half miles below 
 Beech City, towards DeardofE's Mills, the accumulations of 
 gravel in the valley are immense. The valley is here about one 
 mile wide. The gravel is thrown up into hummocks and ridges 
 from 20 to 30 feet above the general level, enclosing many ket- 
 tle-holes. The country from this point to Wilmot, and from 
 Wilmot south to the county line, is completely enveloped in till. 
 One boulder measured 7x6 feet, 2-| feet out of ground. But on 
 the road from DeardofE's Mills, across the northern part of 
 Wayne township in Tuscarawas county, toward Weinsburg in 
 Holmes county, no till or boulders appeared for several miles. 
 The road leads over the summit of the land, and displays, to 
 
Detailed Report for Ohio. 43 
 
 good efEect on either side, the contrasts between the glaciated 
 and unglaciated region. One mile and a half east of the 
 Holmes county line granitic boulders begin to appear, and ac- 
 companied after a little with till, continue to increase to Weins- 
 burg. This east and west road enters the moraine at an acute 
 angle, the direction of the moraine being here west-southwest. 
 The northeast portion of Paint township, in Holmes county, is 
 covered with till to an unknown, but evidently to a great depth. 
 
 HOLMES COUNTY. 
 
 The glacial boundary in Holmes county is very sharply de- 
 fined, dividing the county into two nearly equal portions. It 
 enters the county on the east, in Paint township, near the cor- 
 ner of Stark and Tuscarawas counties, and passes diagonally 
 to the northeast corner of Berlin township, where it turns 
 more nearly west, passing through Hardy township, crossing 
 the Killbuck below Millersburg; thence, bearing slightly to the 
 north, it passes through the centre of Monroe and the north- 
 ern part of Knox township, to the eastern side of Hanover 
 township in Ashland county. Through all this distance the 
 contrasts between the regions north and south of this line are 
 very marked. 
 
 In Paint township there is but little till south of the diag- 
 onal road leading from Wilmot through Weinsburg to Berlin. 
 Driving one-quarter of a mile south of Weinsburg, till sud- 
 denly disappears. There is a noteworthy collection of granitic 
 boulders a few. rods southeast of the village, at the crossing of 
 the road from Slatersville. South of this there is no till. Oc- 
 casional boulders were reported, but none were seen by us in a 
 drive of half a mile. To the north and east of Weinsburg the 
 deposit of till is continuous, and evidently of great depth. 
 Weinsburg is on the watershed between Sugar Creek and Indian 
 Trail Creek, and according to our barometer was 600 feet above 
 the valley of the Killbuck at Millersburg. The southwestern 
 part of Paint and the southeastern of Salt Creek townships are 
 likewise covered with till, which is evidently very deep. A 
 granitic boulder on the road between Weinsburg and Mount 
 Hope measured 7x6 feet, 3 feet out of ground. 
 
44 Detailed Beport for Ohio. 
 
 BERLIN TOWNSHIP. 
 
 A detour of several miles through the southern portion of 
 this township disclosed no sign of glaciation, except in the 
 valley of Dowdy Creek. In this valley there are extensive ter- 
 races down as far as within one mile of the southern boundary. 
 At that point the terrace is 50 feet above the stream and about 
 150 yards wide, and contains some scratched pebbles. The 
 boundary of the till runs between Sections 13 and 8, and crosses 
 the western boundary of the township one-half mile south of 
 the road running between Berlin and Millersburg. The eleva- 
 tion here is 475 feet (B) above the Killbuck. Granitic boulderg 
 are abundant all along this road. At Berlin post office it is 
 600 feet (B). On driving north from Berlin post ofiBce we strike 
 immediately into till, which seems to be very deep. Near the 
 corner of the road turning east one-quarter of a mile north, in 
 Section 6, are extensive kame-like accumulations containing 
 numerous boulders, and enclosing a large kettle-hole. Till is 
 continuous northward. 
 
 HAKDY TOWNSHIP. 
 
 On the road from Millersburg to Berlin till is found on the 
 tops of the hills all along to the township line. Going east 
 from Millersburg the first hill is 250 feet above the railroad, 
 the second 350 feet, thence rising at the town line to 475 feet. 
 The depth of the till is at least several feet. In Section 14 a 
 boulder measured 7x5 feet, 3 feet out of ground. The most 
 southerly deposit of till on the east side of the Killbuck is 
 where the north branch of Sandy Eun touches Section 16, two 
 miles and a half southeast of Millersburg. Three-quarters of 
 a mile northeast of this point a small accumulation of till and 
 boulders occur, at a height of 375 feet above the run; east and 
 south the country is entirely free from it. 
 
 The terraces upon the Killbuck are extensive, both above 
 and below the glacial limit. One mile and a half below Mil- 
 lersbui'g 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 
 
^ 
 
 PLATE X. 
 
 PLATE XL 
 
46 Detailed Ite;portfor Ohio. 
 
 the hills beyond. Two miles further south, in the northwest 
 corner of Mechanic township, near Stuart's Mills, the terrace 
 is composed of finer material, and is level topped and gradu- 
 ally descends towards the south, being here but 71 feet above 
 the flood-plain. Still further below the glacial limit at Ox- 
 ford is a terrace on the east side of the creek, extending across 
 the open ends of the ox-bow which the stream here forms. 
 The intervale is here about one-third of a mile wide, and 25 
 feet above low-water mark. The terrace is 76 feet higher. 
 On the west side of the creek, between Shimplin's Run and 
 Black Creek, and one-quarter mile west of the Killbuck, are 
 terraces of fine material containing some granitic gravelj 
 which are 61 feet above the flood-plain. 
 
 Driving up from Millersburg, on the west side of the Kill- 
 buck, there are no terraces for the first mile. The valley is 
 about one-half mile wide. But just above where a small 
 stream comes in from the west is a kame-like accumulation of 
 coarse material, 50 feet in height, extending about one-eighth 
 of a mile. On the north side of this small stream the mate- 
 rial is finer, and the surface much more uneven, extending to 
 the road running over the hills to HoJmesville. 
 
 Near Holmesville — five miles above Millersburg — Paint, Kill- 
 buck, and Martin's Creek come together nearly at right angles. 
 About their junction there is an extensive intervale not far 
 from two miles in diameter. The village is built upon a ter- 
 race about 25 feet above the intervale. Between the Killbuck 
 and Martin's Creek, which comes in from the east, there is a 
 kame-like accumulation of rather fine material (the pebbles 
 being ordinarily not more than three inches in diameter) ex- 
 tending about one-eighth of a mile N. W. by S. B. The sur- 
 face is very much broken, displaying many kettle-holes. A 
 railroad cutting through it shows some scratched stones in the 
 material, and a depth of 61 feet at the railroad; but it rises 
 about 40 feet higher to the north. Prom this point to Millers- 
 burg, on the east side, there are no terraces, the intervale being 
 about one-sixth of a mile wide. One-half a mile north of 
 Millersburg, as the road rises over the hill, a fresh cut in the 
 till of 20 feet disclosed no bottom to it. 
 
Detailed Report for Ohio. 47 
 
 On the west side of the Killbuck, in Hardy township, till 
 ceases, two miles and a-half southwest of Millersburg, on the 
 farm of William Lisle. There is here a small stream, and 
 the till appears upon the north side of the stream, but 
 not upon the south. The general elevation of the country 
 (which is much broken) is 350 feet above the Killbuck. 
 Southeast, for two miles, till is totally absent, while to the 
 north it is abundant, and boulders are numerous. It contin- 
 ues west to the works of the Hardy Coal Company, from 
 which place to Oxford no till appears. 
 
 MONROE TOWNSHIP. 
 
 From Oxford we drove in a northwest direction up a small 
 stream which rises in the centre of Monroe township. No 
 boulders or till appeared below Centreville; but there were 
 terraces of fine material containing some granitic pebbles, and 
 diminishing in height as we ascended the stream. North 
 from Centreville granitic boulders began to appear, and were 
 frequent all along up the valley to the watershed, where, near 
 W. S. Cam's, a large deposit of till appeared, enveloping 
 everything and forming large dome-shaped hills. Cuts from 
 10 to 15 feet disclose no rocks. Th6 road is 300 feet (B) 
 above the Killbuck, but hills covered with till are about 150 
 feet higher. 
 
 Oak Grove Nursery, a short distance to the west, is 475 (B) 
 above the Killbuck. One-quarter of a mile farther west, on 
 lower ground, the deposit of till and boulders is very marked: 
 one of granite measured 10|^x6^ feet, 3^ feet out of the ground. 
 Elevation 430 feet (B). Till is continuous one mile west, and 
 south to the farm of E. Martin. For the next mile and 
 a half there were occasional boulders, but no till. On the 
 next road west, struck suddenly into till by a school-house, 
 whose elevation is 610 (B) above the Killbuck. Beyond this 
 there were occasional boulders to the road near the western 
 line of the township, leading to Napoleon. Some boulders 
 were seen half a mile farther south. This is about five miles 
 northeast of Napoleon, which is situated in the valley of 
 Black Creek, which is about one-eighth of a mile wide, and 
 
48 Detailed Report for Ohio. 
 
 from 400 feet to 500 feet below the general level. A striking 
 feature along this creek, and especially in the vicinity of 
 Napoleon, is the great blocks of sandstone, formerly occupy- 
 ing the summits of the hills, Avhich have been broken ofE, and 
 have gradually crept down towards the bottom as the under- 
 lying shale and talus have been removed. These blocks are 
 sometimes as large as a house, and ai'e in all stages of ad- 
 vancement in their progress towards the valley. They resem- 
 ble in most respects what is to be seen in the valley of the 
 Alleghany south of Salamanca, and in the neighborhood of 
 Rock City. Instead of being due, as some have supposed, to 
 glacial action, these phenomena are pretty certain evidence of 
 the absence of any glacial movement, and exist either alto- 
 gether south of the line of glaciation, or, as here and at Rock 
 City, on the very margin, where the ice-movement ceased, 
 and where glacial abrasion was reduced to zero. 
 
 KNOX TOWNSHIP. 
 
 From Napoleon we followed up the narrow valley of Black 
 Creek on the road to Nashville. The valley continues to be 
 about one-eighth of a mile wide, and for five miles is remark- 
 able both for the abundance of the sandstone blocks referred 
 to above, which are creeping down the sides, and for the 
 absence of granitic boulders. Upon reaching the farm of 
 A. Cline, a litble south of the watershed, till appeared in 
 great quantities. This is 375 feet (B) above Napoleon. Prom 
 here to Nashville till is continuous for 3-^ miles, as also south- 
 west of Nashville to the hill south of the farm of S. H. Vance. 
 Boulders continued to the cross-roads south of the house of 
 A. Bell, where all signs of glaciation had ceased. West of 
 this there are no signs of glaciation as far as the next cross- 
 roads. Elevation 450 feet (B) above Napoleon. Turning 
 north, one mile brought us into a kame-like deposit in a shal- 
 low valley by the cross-road, near G. Uhlmiin's, one mile 
 south of Washington township, and three miles east of Han- 
 over township in Ashland county. This kame is about 35 
 feet high, and its course is nearly parallel with that of the 
 shallow valley in which it is situated, which drains into the 
 Mohican. What is marked near here, on the county atlas, as 
 
Detailed Report for Ohio. 49 
 
 an ancient mound is more ancient than the map-maker sup- 
 posed, it being not artificial, bnt a small mound of slate left 
 by erosion. Prom here northwest, to a point a little above 
 the junction of Lake Fork with Mohican River, till and boul- 
 ders are continuous. This is near the southwest corner (Sec- 
 tion 12) of Washington township. From this point down to 
 the junction and a half mile beyoud, is a terrace of very 
 coarse material, largely composed of granitic pebbles. Ele- 
 vation above the river 107 feet. No till was discovered in the 
 western projection of Knox township. From this point we 
 drove through Nashville to Millersburg, on a road parallel 
 with the glacial boundary, and about two miles nortli of it. 
 Till is continuous, and evidently deep, there being but few 
 out-cropping rocks- in the whole distance. Cuts in the till 
 frequently showed a depth of from 10 to 15 feet, with no 
 signs of bottom. Two wells were reported, on the hills 
 crossed, as going 35 feet without striking rock. Boulders 
 are everywhere abundant. To the north stretchesthe charac- 
 teristic levelled area of the glaciated region. The ice, with 
 its burdens, evidently came up to the watershed between 
 Paint Creek and Black Creek — its serrated edge barely sur- 
 mounting it. 
 
 KNOX COUNTY. 
 
 The boundary line of the glaciated region, which, in the 
 western part of Holmes county, was beaiing slightly north- 
 ward, suddenly turns to the south in the eastern part of Han- 
 over township, Ashland county; passing theuce into JefEerson, 
 the northeastern township of Knox county, and thence tlirougU 
 the western portions of Union, Butler, and Jackson townships, 
 along the eastern margin of the county. The change of direc- 
 tion was so abrupt as at first to confuse, and afterwards to 
 startle us. But, as usual, we found the departure from the gen- 
 eral law of glacial movement less than would at first seem to 
 be the case. From Salamanca, in New York, the moraine, with 
 slight variations, bears continually southward, as well as west- 
 ward. 
 
50 Detailed Beport for Ohio. 
 
 JBFFEKSOlir TOWKSHIP. 
 
 There are a few granitic boulders, and some glacial gravel, 
 on the road from Jelloway to Greersville, one-half mile east 
 of Greersville. Near the same place on the Danville road, 
 by the Methodist church, there is a larger collection of peb- 
 bles, and perhaps till. This is in a valley, on a branch of the 
 Jelloway, running south. But the hill to the west is free 
 from drift ; likewise the hill to the east, occupying Sections 
 4 and 7, is without till. But in the valley of a small tribu- 
 tary to the Mohican, a little south and east, in Sections 3 and 
 8, there are accumulations of till in ridges from 10 to 15 feet 
 high. These are best shown upon the farm of Q. Greer, in 
 Section 8. From this point to the south line of the township 
 till is continuous, but does not extend eastward into Sections 
 12 and 19. The Cleveland, Akron, and Delaware Eailroad 
 enters the glaciated region from the east through a cut in till, 
 one mile east of Danville, and very nearly upon the line 
 between Jefferson and Union townships. This cut is 375 
 paces long, and is from 20 to 36 feet in depth. The pebbles 
 average from 2 to 3 inches ; but there are a few boulders of 
 considerable size. The hills to the southeast show no till. 
 
 UNION TOWNSHIP. 
 
 The old village of Danville is built upon a hill in the ex- 
 treme northwestern part of the township. The height of 
 this hill is by barometer exactly the same as that of the depot 
 at Mount Vernon. This hill is composed of till. A. J. Work- 
 man reports a well 126 feet deep as passing through yellow clay, 
 blue clay, gravel, quick-sand, and cemented gravel, and still 
 not reaching rock. Another well of 65 feet, through similar 
 material, was reported. One and a half mile south of Dan- 
 ville, on the Millwood road, a large deposit of till forms the 
 divide between Owl Creek and Mohican Eiver. The east and 
 west line of this deposit is sharply defined, running through 
 the eastern part of Section 14, and the central part of Section 
 17, to Millwood. On the east side of the small brook, run- 
 ning into Millwood from the north, drift is absent ; but on 
 the west side it is bounded by a range of gravelly knolls and 
 
Detailed Report for Ohio. 51 
 
 kame-like ridges. These are composed of glacial material, and 
 are 117 feet above the brook on the north of the village. 
 
 BUTLER TOWHrSHIP. 
 
 On the south side of Owl Creek a thin deposit of till 
 covers the whole western range in Butler township, the boun- 
 dary line swinging a little to the east until it enters Jackson 
 township in the northeastern corner of Section 4. But the 
 deposit is nowhere so marked in this township as to deserve 
 to be called a ''terminal moraine." The limit, however, is 
 pretty sharply defined. 
 
 JACKSON TOWKSHIP. 
 
 In this township the boundary line enters upon the north, 
 two miles east from Clay township, and continues in a south- 
 easterly direction to the south line, about three miles east of 
 Clay township. At the cross roads in Section 8, we turned 
 east into till of considerable evident depth. This disap- 
 peared in three-fourths of a mile, and did not reappear until 
 we had gone one mile south to tlie church in Section 12, and 
 turned west one-half mile. Here, on turning the summit of 
 the hill, two miles north from the south, and 3f miles east of 
 the west line, we struck into a continuous deposit of. till 
 stretching westward. This is upon the watershed, and is 300 
 feet (B) above Wakatomaka Creek. Upon crossing this creek, 
 and striking the Zanesville road in the northeast corner of 
 Eden township. Licking county, and driving northwest to 
 Martinsburg, found till of great depth all the way. Occasion- 
 ally the tops of the hills exposed rock in place, but Paul Run 
 is nearly filled with till. 
 
 LICKING COUNTY. 
 
 The glacial boundary line enters Licking county in the 
 northeast corner of Eden township, passes through the north- 
 west corner of Mary Ann, the eastern sides of Newark and 
 Licking townships, nearly on the line between the latter and 
 Franklin and Bowling Green townships. 
 
52 Detailed Report for Ohio. 
 
 EDEN TOWNSHIP. 
 
 Prom Fallsburgh Post OfiBce to Simpkin's comer, in the ex- 
 treme northwestern portion of the township, the road follows 
 the watershed. Ko till or boulders whatever appear upon it. 
 At Simpkin's corner a few granitic pebbles appear, but there 
 is no till until reaching the farm of A. D. Lanason, in Eden 
 township, one-eighth of a mile south of the Knox county 
 line, and three-quarters of a mile west from the line between 
 Fallsburgh and Eden township. This is upon a height of land 
 about 350 feet above the creek, and granitic boulders three 
 and four feet in diameter are abundant. Patches of till con- 
 tinued to appear upon the road following the watershed south 
 for 2^ miles; crossed Rocky Fork near J. Elliott's ; there 
 was but little drift in this valley at this poiut. Upon ascend- 
 ing the watershed to the west, in Section 13, found a consid- 
 erable depth of till, which continued for a half mile west and 
 a quarter of a mile south ; but the diagonal road running 
 southeast, and keeping along the watershed between Rocky 
 Fork and Wilkin's Run shows no till to the town line ; but 
 a few white granitic boulders were observed. Till, however, 
 appeared 1^ miles west in the valley of Wilkin's Run. 
 
 MARY ANN TOWNSHIP. 
 
 The deposit of till is not continuous over the western part 
 of Mary Ann, but a considerable timount appears in Section 
 6, and the southwestern corner of the township is completely 
 enveloped in a deep deposit. 
 
 The terrace deposits in the neighborhood of Wilkin's Run 
 post office are noteworthy. One-half mile southwest of the 
 post office this terrace is 92 feet high, and composed of water- 
 worn pebbles with no large boulders. This continues up the 
 small branch nearly to' the line of Madison township, where 
 it merges into the deposit of till. Two miles east of Wilkin's 
 Run the deposit is still noteworthy, and presents the appear 
 ance of extensive kames. The southwest corner of this town- 
 ship, and the southeast of Newton, are deeply enveloped in 
 till. Wilkin's Run was one of the glacial outlets, and the 
 
Detailed Report for Ohio. 53 
 
 terrace deposits are such as usually 'mark the streams as they 
 emerge from the boundary of the glaciated region. 
 
 NEWARK TOWHrSHIP. 
 
 At the city of Newark the three forks of the Licking River 
 unite. All of these drain the glaciated region upon whose 
 eastern border Newark is situated. The extensive gravel 
 plain upon which the city is built is about 20 feet above the 
 river, and is the deposit of these streams in the last stages of 
 the glacial period when still swollen by the floods of the melt- 
 ing glacier; while terraces of a still higher altitude surround 
 the plain, marking the size of the floods at a somewhat earlier 
 date, when at their greatest extent. The terrace upon which 
 the city cemetery is situated is 108 feet above Licking River. 
 Southeast of the city, a terrace near the river is something 
 over 60 feet above it. The eastern limit of till in this town- 
 ship coincides in the northern part with the east line of the 
 township, though in this part of the township many of the 
 hills are free from till. As, however, you go east from the 
 North Pork, along the town-line road, between Newark and 
 Newton, the till appears to be of great depth, and stretches 
 away to the north in such hummocks and ridges as usually 
 characterize the moraine. The elevation here is 300 feet (B) 
 above the North Fork. South of the city, on the Linnville 
 road, till envelops everything to the summit of the high 
 lands, where it is evidently of great depth. The elevation is 
 about 300 (B) above Newark. 
 
 LICKING AND FEANKLIN TOWNSHIPS. 
 
 The glacial boundary follows very closely the line between 
 Licking and Franklin townships. To the west everything is 
 enveloped in till ; to the east are the familiar rocks and gorges 
 of the unglaciated region. Many boulders were found, and 
 a considerable amount of drift, along Claylick Creek, in the 
 centre of Franklin township. This, however, seems to be a 
 water deposit, formed by streams and floating ice, which 
 came over the low place between Swamp Run and Claylick 
 Creek. The gap in the watershed between these streams is 
 
54 Detailed Report for Ohio. 
 
 150 feet lower than that of the hills to the north and south, 
 and the Talley through which Claylick Creek now empties to 
 the north appears to be very narrow. There certainly is no 
 till on the hills, either to the northwest or southeast of this 
 depression. The road along the town line, from Hog Kun to 
 Amsterdam, in the southwest corner of Franklin, is all the 
 way over a deep deposit of till containing many granitic boul- 
 ders. Amsterdam is 400 feet (B) above Newark, and com- 
 mands a most extensive view of the fertile and level glaciated 
 region to the west, and of the broken region to the east. 
 Near the Presbyterian Church upon the most commanding 
 point near Amsterdam, is an Indian mound 21 feet high, and 
 124 paces in circumference. East of Amsterdam a drive of 
 three miles to Linnville disclosed no till, but south and west 
 the deposit is continuous and deep. In the southeastern part 
 of Licking township, east of the reservoir, the road runs for 
 half a mile upon the summit of a ridge of kame-like hills con- 
 taining many granitic boulders. This ridge seems to cross the 
 valley, and to be a true moraine barrier, restraining the waters 
 of Keservoir Lake. The railroad near here shows very good sec- 
 tions of this ridge, and of other ridges parallel to it. They 
 are from 15 to 30 feet above the level of the valley, but how 
 much of their base is obscured by subsequent deposits there 
 is no means of telling. Through this depression east of the 
 reservoir, on the line between Licking and Perry counties, 
 there was evidently a great overflow of glacial water, empty- 
 ing through Jonathan Creek into the Muskingum, below 
 Zanesville. 
 
 PEEEY COUNTY. 
 
 The moraine passes in this county, in a north and south 
 direction, through Thorn and Eeading townships. 
 
 THOEN TOWNSHIP. 
 
 We have already described the glacial accumulations east of 
 the reservoir, where they pass from Licking county into this 
 township. The reservoir occupies a great kettle-hole. The 
 railroad which here cuts through the moraine follows for sey- 
 
Detailed Re-port for Ohio. 55 
 
 eral miles towards the southeast an outlet for the glacial 
 floods. This occupies a Talley about a mile wide, through the 
 middle of which kame-like ridges of gravel 15 to 30 feet in 
 height extend ; but these are flanked on either side by depos- 
 its of black muck. On turning up a tributary towards Som- 
 erset, these deposits cease. The headwaters of the stream 
 are in an unglaciated region. 
 
 Thornville is upon a hill of till containing numerous gran- 
 itic boulders, and which is about 300 feet (B) above Newark. 
 A well upon this hill was reported as passing through 10 feet 
 of soil, 25 feet of blue clay. Southeast from Thornville the 
 till is, for the first mile, very deep, with very numerous and 
 large granitic boulders. Till continues a mile farther to Sec- 
 tion 23, and thence south to the northwest corner of Reading 
 townshi]). But from Section 23, Thorn township, to Somer- 
 set (seven miles southeast), and thence west to the branch of 
 Rush Creek, a mile west of New Reading, the country is wholly 
 unglaciated. 
 
 BEADING TOWNSHIP. 
 
 The northwestern section of Reading township presents a 
 level and rich expanse of territory, produced by the glacial 
 floods coming down from the southern part of Thorn' town- 
 ship. The contrast between the western sections of this town- 
 ship and. everything east of Rush Creek is very marked. The 
 road running south, near the western line of this township, is 
 through a region deeply enveloped in till, as far as the pike, a 
 little east of Rushville. A drive on the pike, of half a mile, 
 into Reading township, toward Somerset, brings one into the 
 unglaciated region. 
 
 FAIRFIELD COUNTY. 
 
 The glacial boundary enters Fairfield county, a little south 
 of the Somerset and Lancaster pike in Richland township, and 
 crosses the northwest corner of Rush Creek township, the 
 southeast corner of Pleasant township, the northwest corner 
 of Bern, through the center of Hocking township, and the 
 western sections of Madison township to the line between Pick- 
 away and Hocking counties. 
 
56 Detailed Report for Ohio. 
 
 RICHLAND TOWNSHIP. 
 
 The Somerset and Lancaster pike suddenly enters extensive 
 deposits of till, upon passing from Perry to Fairfield county, a 
 mile and a half east of East Rushville ; but a drive of a half 
 mile south carries one entirely beyond the range of till. From 
 Rushville one must drive a mile and a half south to reach the 
 unglaciated district. But here on both sides of the creek, the 
 passage from the glaciated to the unglaciated is sudden. On 
 the north part of H. G-eiger's farm, east of Rush Creek, and 
 one-half mile north of the township line, the glacial limit is 
 marked by hummocks of till, which are at least 50 feet in 
 deptli ; while on the west side of the creek the boundary is near 
 the town line in Rush Creek township, on the farm of J. D. 
 Martin. Large granitic boulders abound along the glaciated 
 margin through Richland township. Tl^e elevation is 250 
 feet (B) above Lancaster, and about 300 feet above Rush Creek. 
 There is no barrier in this vicinity to stop the southern pro- 
 gress of the ice. A detour of several miles to Bremen demon- 
 strated the aljsence of till to the southeast. 
 
 RUSH CREEK TOW^NSHIP. 
 
 The characteristics of the glacial boundary through Rush 
 Creek township are very similar to those in Richland. The 
 remnants of a boulder of dark, hornblendic rock, on the farm 
 of J. D. Martin, one-fourth south of West Rushville, measured 
 10x8x3 feet out of ground. Probably one-third had been re- 
 moved by blasting. The elevation is 250 feet above Lancaster, 
 and there is no southern barrier to account for the sudden ler- 
 mination of the till. Four or five miles to the south, across 
 the valley of the west branch of Rock Creek, an escarpment of 
 Waverly sandstone hills is a striking feature of the landscape. 
 There is no till in Sections 17 and 18 of this township. 
 
 PLEASANT TOWNSHIP. 
 
 From Rushville to Lancaster the pike bears southwest. The 
 glacial boundary enters Pleasant township, one mile south of 
 the pike, intersecting the pike again near where it passes from 
 Pleasant township to Bern. The road running to Lancaster, 
 
PLATE XII. 
 
 PLATE XIII. 
 
58 Detailed Report for Ohio. 
 
 parallel with the pike, and about one mile northwest, is through 
 a region everywhere enveloped with till, a great amount of it 
 resting upon the hills 250 feet above the city. It is at the in- 
 tersection of this road with that to Pleasantville that the cele- 
 brated granitic boulder referred to by Professor Andrews (see 
 his Geology, pp. 211, 212) is found. This is in the valley of 
 Baldwin's Eun, is hornblendic in character, and measures 
 18x12x6 feet out of ground. Boulders were left upon the 
 summit of Pleasant Mountain, a mile north of Lancaster, and 
 about 300 feet above it. 
 
 BERN TOWNSHIP. 
 
 The moraine enters the northwest corner of Bern township, 
 near the city of Lancaster, but its course is here somewhat 
 disguised by the water action in the Hocking Valley, which it 
 here intersects. The Cincinnati and Muskingum Valley Eail- 
 road, east oi Lancaster, passes through a low valley into the 
 tributaries of Rush Creek. This valley is bounded upon the 
 south by an escarpment of Waverly sandstone, rising about 
 250 feet. A drive across the country, back of this escarpment, 
 from Lancaster to Bern Station, failed to disclose any signs of 
 glaciation ; but the valley itself is partially filled with gravel, 
 brought in by the various glacial tributaries from the north. 
 This deposit of gravel is especially noticeable near Bern Station, 
 where the gravel accumulation brought down by Raccoon Creek, 
 forms a hill 50 or 60 feet in height. Till and boulders appear 
 between the- Logan and Chillicothe road, at an elevation of 
 about 50 feet, one mile south of Lancaster. 
 
 HOCKING TOWNSHIP. 
 
 The course of the Mayesville and Zanesville turnpike, through 
 Hocking township, is everywhere over a vast deposit of till. 
 This is true not only when it follows up the valley of Hunter's 
 Run, parallel with and close to the railroad, but after it crosses 
 the railroad to the south, and rises upon hills which are 450 
 feet above Lancaster, near the southwest corner of the town. 
 Here the till is piled up to a great height, upon the summit of 
 the sg,ndstone escarpment which overlooks the plains to the 
 north made smooth and fertile by glacial action. On the 
 
Detailed Beportfor Ohio. 59 
 
 farm of S. Peters, in SeAion 30, 450 feet above the canal at 
 Lancaster, a well was reported 40 feet in till ; another, near 
 by, 30 feet. The parallel road, two miles southeast, shows no 
 till from Hamburg post office toward Lancaster,for three miles, 
 to its intersection with Arney's Eun; for the rest of the 
 distance till is continuous and deep. But occasional granitic 
 boulders crown the summit of the sandstone hills running 
 parallel with these roads and half-way between them, and 
 rising 450 feet above the canal. Muddy Prairie, in the south- 
 western corner of this township, is a shallow kettle-hole of 
 great size, which has been filled by the accumulation of peat. 
 Its natural drainage is by a long circuit to the west, but by a 
 little ditching it is made to empty by a shorter course through 
 Muddy Prairie Eun. 
 
 MADISOIf TOWNSHIP. 
 
 On leaving Lancaster the glacial boundary turns rapidly 
 toward the south, and passes through Madison township nearly 
 in a north and south direction, through Sections 4, 9, 16, and 
 31. It crosses Clear Creek at Clearport, near the junction 
 with Muddy Eun, at an elevation of about 300 feet (B) above 
 Lancaster. Everywhere along this distance the glacial accu- 
 mulation abuts closely against an escarpment of Waverly sand- 
 stone ; yet covers hills to the west, in Clear Creek township, 
 of equal height with them, namely, 450 feet above Lancaster. 
 The line bends a little west as it emerges from this township, 
 and enters Hocking county. 
 
 PICKAWAY AND HOCKING COUNTIES 
 
 The moraine follows so nearly the line between Pickaway 
 and Hocking counties that we shall do best to consider them 
 together. 
 
 Driving east from Tarleton, in Pickaway, to the line of 
 Hocking, till and granitic boulders are continuous and abundant 
 to the 'Hocking line, and for nearly a mile farther east ; but 
 here they suddenly cease, and ' do not reappear on turning 
 north until reaching Section 30, in Madison township, Fair- 
 field county. Driving southeast from Tarleton, till is continu- 
 ous until crossing the county line, northwest of South Perry 
 
.60 Detailed Report for Ohio. 
 
 post oflSce. A section of till upon the county line here shows 
 at least 30 feet in depth. The elevation is 300 feet above 
 Circleville. One mile east of the county line till had entirely 
 disappeared. There is no till in the valley of Laurel Eun for 
 a mile and,a half west of South Perry. Hills of Waverly sand- 
 stone arise on every side about the village. There is no till 
 upon them, but a granitic fragment 6 in. by 4 in. was found 
 upon a hill a few rods north of the village, and 225 feet (B) 
 above it. This is 300 feet above Circleville. Across the Eun, 
 on the south side, the ridge road to Adelphi rises 375 feet in 
 one and one-half miles, and turns west upon the summit, 
 near the southern line of Perry township, and three miles 
 from its western boundary. This is by barometer 450 feet 
 above Circleville, and the level touches the tops of the hills 
 in all directions. This road continues for three miles west 
 upon the summit of a narrow ridge of sandstone, left by the 
 erosion of the streams. From it one looks down on either 
 side jnto gorges'between 300 and 400 feet in depth. On driving 
 upon this ridge about three miles westward, we struck a col- 
 lection of granitic pebbles upon the very summit, about one 
 mile northeast of the southwest corner of the township. The 
 pebbles were small, but of a variety of kinds. Three-fourths 
 of a mile farther west, while still 275 feet above South Perry, 
 began to find till. Granitic boulders continue frequent to 
 Laurelville, at the junction of Salt Creek and Laurel Creek. 
 The level of the stream is here 75 feet lower than that at 
 South Perry. 
 
 EOSS COUNTY. 
 
 Nowhere in Ohio is the glacial boundary marked by larger 
 accumulations than in Eoss County, through which it extends 
 diagonally from the northeast corner to the southwest — passing 
 through the northwest corner of Colerain, the southern part 
 of Green, the southern part of Union, the northern edge of 
 Twin, the southeastern part of Paint, and the western part of 
 Paxton townships. 
 
 COLEEAIN TOWNSHIP. 
 
 The village of Adelphi occupies the northeast section of 
 Colerain township, and is built upon an irregular deposit of 
 
Detailed Seport for Ohio. 61 
 
 till worthy to be compared with the terminal moraine on Cape 
 Cod in Massachusetts, and with that upon the Pocono plateau 
 in Pennsylvania, and that west of Canton in Stark county. 
 Salt Creek bursts through this moraine a few rods northeast 
 of the corner of the county, and makes ofE to the southeast, 
 through a narrow valley 450 feet deep, and for a short dis- 
 tance is bounded on the east by extensive gravel terraces. 
 The moraine accumulation upon which Adelphi is built abuts 
 upon this creek towards the east, and there is here a perpen- 
 dicular exposure of till 188 feet in depth. The creek is con- 
 stantly undermining it, and an extensive slide is in progress 
 which has already carried away a considerable portion of the 
 cemetery. The height of this cemetery was taken by level. 
 West of the village where the land is higher the barometer 
 indicated more than 300 feet. On driving south from Adel- 
 phi, up Brimstone Hollow, till continued for one mile, and 
 occasional granitic pebbles were found for two miles farther, 
 where the summit of the Waverly sandstone escarpment was 
 reached, at a height of 400 feet (B) above Salt Creek. Turn- 
 ing west upon this ridge, a little till was found upon the very 
 summit after going a mile, and just before beginning to 
 descend towards the north into the valley of Eeed's Ford. 
 On descending into this valley, a hundred feet or more, drift 
 began to appear. This was at first water-worn, and in terraces, 
 as would be natural in a valley beginning, as this does, a little 
 south of the glaciated line, and opening to the north. On 
 reaching Section 14, near the residence of Isaac Delong, till 
 appeared in large quantities, with many granitic boulders, 
 some of them from 6 to 8 feet in diameter. On going a mile 
 and a half farther north, this road reaches the turnpike, two 
 miles from Adelphi, which, over all this distance, follows the 
 summit of a true moraine deposit. To the northwest, stretch 
 the fertile plains of Pickaway county, lying fully 150 feet 
 lower than the summit_of this moraine. To the south rises, 
 near by, the escarpment of Waverly sandstone, which forms 
 the northwestei'n boundary of the great coal formations of 
 the State. The granitic pebbles which we had found upon the 
 summit of that escarpment in Ross, in Hocking, and in Fair- 
 
62 Detailed Report for Ohio. 
 
 field counties, show that the ice was at least 400 feet thick over 
 all the plains to the north. 
 
 This moraine ridge continues southwest from Adelphi in 
 about the same proportions, and in similar relations, to the 
 plain upon the north, and to the hills upon the south, until it 
 enters Green township, two miles from the southern border. 
 All along through Colerain township, in driving a mile 
 south from the pike, one strikes out of the till, and after 
 crossing a little valley, plunges into, the deep gorges which 
 everywhere characterize the sandstone regions beyond. Pro- 
 fessor Orton had noted the boundary with great accuracy. 
 (See Ohio's Geol. Keport, Vol. II, pp. 651, 652.) 
 
 GREEN TOWNSHIP. 
 
 The moraine enters G-reen township from (he east in Sec- 
 tion 24. Till continued to the northern edge of Section 35, 
 where it suddenly disappeared on the watershed. A drive of 
 two miles south into Harrison township demonstrates the 
 total absence of till over the southeast corner of Green. On 
 driving over the diagonal road northwest till appeared at the 
 watershed in Section 25, nearly one mile from the south line, 
 and a mile and a half from the east line of Green township. 
 The accumulation of till is large along the road between 
 Sections 26 and 27. The diagonal road running southwest 
 through Sections 27 seems directly upon the moraine, and 
 between this glacial accumulation and the rocky hills to the 
 south there is a space of about half a mile, occupied by a 
 small stream whose headwaters are in Section 33. In the 
 southern part of Section 29 there are enormous kame-like 
 ridges of gravel, from 100 to 150 feet (B) in height, and run- 
 ning north and south. The material of this kame is rather 
 fine, and is largely composed of limestone pebbles. The Pick- 
 away plains here contract into the valley of the Scioto, which, 
 through the rest of its course, is nowhere more than two or 
 three miles wide, and is bounded on either side by precipitous 
 hills of slate and sandstone. In the northeast corner of Sec- 
 tion 31, the water-worn material of the kame gives place to 
 till, which contains many granitic pebbles a foot or more in 
 diameter. In crossing the head of the Scioto Valley, on a 
 
Detailed Beportfor Ohio. 63 
 
 road running east and west through this point, three parallel 
 ridges are encountered, running nearly north and south, each 
 one in order toward the river extending farther south. 
 
 SPEINGFIELD TOWNSHIP. 
 
 About halfway between Hopetown, in Springfield township, 
 and Chillicothe the first terrace (over which the railroad runs) 
 is about a half mile in width. The second terrace, which occu- 
 pies the remaining space to the hills on the east, which is also 
 about a half mile in width, rises abruptly 48 feet above the 
 river. 
 
 UNION TOWNSHIP. 
 
 In driving up the Scioto, upon the west side, from Chilli" 
 cothe, the road follows ihe first terrace, which is about a mile 
 wide, and 20 feet above the river. Kame-like ridges appear in 
 Union township, nearly opposite the southwest corner of 
 Green, and just above the second toll-gate, where the Clark- 
 son pike branches ofE to the west. The cross-road leading 
 directly west from this point ascends 400 feet (B) in the first 
 mile. Granitic boulders are abundant at this elevation, and a 
 well one-half mile south passes 33 feet through what was called 
 "gravel," but is doubtless "till." Granitic boulders appear 
 upon this plateau for a' half mile or so farther south. The till 
 is of great depth, one-half mile north of the centre, on the 
 fariii of J. A. Hurst. From the centre, southwest, past the 
 houses of M. A. Pinto and W. R. Bowdle, to the Frankfort 
 pike, the road continues upon the highlands, and passes many 
 granitic boulders, and through occasional deposits of till, but 
 the till is not deep. There is considerable development of till 
 at the ci'oss-road near the house of Susan Beard, and again? 
 upon descending the hill to the turnpike near the house of 
 Jacob Plescher; but no till appears along the pike to the west 
 for a mile, where, upon descending about 150 feet, the road 
 enters, at about 150 feet above the north fork of Paint Creek 
 and about a mile and a half east of Frankfort in Concord 
 township, a deposit of till which is unbroken to the north and 
 northwest. The railroad from Chillicothe to Eoxabel strike 
 into extensive drift deposits at Anderson's, upon the north 
 fork of Paint, which is specially abundant at Musselman's. 
 
64 Detailed Report Jor Ohio. 
 
 The deposit here is at least 25 or 30 feet deep, and looks like 
 till, though the material is very fine. 
 
 CONCOED AND TWIN TOWNSHIPS. 
 
 One-half mile south of Musselman's, upon the Greenfield 
 pike, in Twin township, there is a small deposit of till, near 
 the school-house, upon the farm of C. C. Plyley. The road 
 is here 550 feet (B) above Chillicothe, and continues at this 
 height west to Lattaville, in Concord township. A mile east 
 of Lattaville, a well upon the farm of J. McConnell passed 
 through 12 feet yellow clay, 3 or 4 feet blue clay, 10 feet yel- 
 low clay, 5 feet gravel. About 13 feet fi'om the top a piece of 
 wood 3 or 4 feet long and 3 inches through was found in clay. 
 Prom this point the eye surveys a vast extent of till in the 
 valley of the North Fork of Paint, which is about 400 feet 
 lower. But the hills facing the north are here completely 
 enveloped in till. The ice seems for a long while to have 
 crowded down to this rocky escarpment, and for a short time 
 to have overlapped it upon both sides of the North Fork. 
 
 Lattaville, in Concord township, is built upon a siriking 
 development of the moraine. The turnpike follows the mo- 
 raine across the southeast corner of Concord township. The 
 general elevation is from 150 to 200 feet above the valley of 
 the creek, while knolls and ridges of till rise 50 or 60 feet 
 higher. About one mile south is the continuation of the 
 rocky hills 200 or 300 feet higher, through which the North 
 Fork of Paint Creek has cut its way below Frankfort. One 
 mile south of Lattaville till and many granitic boulders ap- 
 peared near T. M. McDonald's, upon the very summit of the 
 plateau, 625 feet (B) above Chillicothe. A mile southwest, 
 upon the other side of the watershed, in the upper valley of 
 Lower Twin Creek, there is a small amount of till near the 
 school-house. South and east of this to the valley of Paint 
 Creek there is no more till. There are some remarkable 
 kames and terraces in these two townships which deserve 
 notice. As we have said, the North Fork of Paint Creek, 
 above Frankfort, flows through a broad expanse of glaciated 
 country everywhere enveloped in till and dotted with granitic 
 boulders. Two miles southeast, near Musselman's, it enters a 
 
Detailed Report for Ohio. 65 
 
 narrow valley about 400 feet deep, and a half mile wide, in 
 which it continues for about 5 miles ; when it comes out into 
 a broader valley, and flows southeast until it unites with the 
 Scioto below Chillicothe. Before the river enters this gorge 
 separating Union from Twin Township, the valley is marked 
 by numerous kame-like ridges, running nearly parallel with 
 the stream. Between Frankfort and Roxabel numerous kettle 
 holes appear. One and a half mile south of Frankfort, on 
 the south side of a small tributary to the creek, is a kame 57 
 feet above the general level of the valley. Granitic pebbles 
 are numerous in this. One near the summit measured 3 feet. 
 This kame runs at least three-fourths of a mile to the south- 
 east. Upon emerging from the gorge below Frankfort, in the 
 eastern angle of Twin township, between Paint Creek and 
 North Fork, extensive kames are found to connect the two 
 valleys along the line of Cat Tail Eun. The material in these 
 kames is water-worn, and ranges from pebbles of granite 3 feet 
 through to fine sand. Granitic boulders 3 feet through occur 
 on the top of the gravel ridges. These ridges are more than 
 180 feet high, and descend upon each side at an angle of 25 
 or 30 degrees. Near the residence of Captain Phill. A. Eodes, 
 facing Paint Creek, near the outlet of Wilcox Run, the kame 
 is 158 feet high, and encircles a kettle-hole of great dimen- 
 sions. 
 
 It is very clear, as Professor Orton surmised (see Geological 
 Survey of Ohio, vol. II, p. 653), that Paint Creek, in pregla- 
 cial times, passed northward, and joined the North Fork, 
 near the eastern angle of Twin township ; but in glacial 
 times that outlet was obstructed by ice, and partly filled with 
 gravel, so that the creek left its broad valley, and has cut a 
 channel for three miles across the rocky escarpment, which 
 here formerly separated it from the Scioto. This post-glacial 
 channel, which it now occupies, is "not more than 200 feet in 
 width at the base, is bottomed with rock, and is bounded by 
 precipitous clifEs not less than 300 feet in height. After fol- 
 lowing a southeast course for three miles, it turns again to the 
 northeast, and regains its old valley two miles west of tlie south 
 line of Chillicothe." 
 
66 Detailed Report for Ohio. 
 
 Prom the fact that the old valley of Paint Creek is filled 
 only to about one-third the height of the surrounding hills, it 
 seems clear that the ice-front itself rested over the eastern angle 
 Twin township long enough for the creek to wear the gorge 
 just described to nearly its present depth. Perhaps this 
 would require 3,000 or 3,000 years. 
 
 9 
 
 BUCKSKIif TOWNSHIP. 
 
 The boundary of the deep accumulation of till enters Buck- 
 skin township a half mile or more south of the Greenville 
 pike, and crosses in a pretty direct line to Paint township, one- 
 half mile or more south of Salem. The road from the Green- 
 ville pike, near Henry Parrett's, to Salem, leads over a contin- 
 uous deposit of till thrown up into low hills and ridges. The 
 rocky escarpment extending from the Scioto Eiver through 
 Union and Twin township, crosses Buckskin township about 
 a mile and a half southeast of Salem. We did not ascend it 
 in this township, but from what we have described in Twin 
 township, and from what we shall describe in Paint township, 
 it is probable that the ice-sheet overlapped these hills, which 
 are all along from 400 to 500 feet above the land to the north. 
 
 PAINT TOWNSHIP. 
 
 With the exception of the northwestern corner, Paint town- 
 ship consists of sandstone ridges left from the erosion of a 
 continuous plateau, which was from 500 to 550 feet (B) above 
 the valley of Paint Creek at Bainbridge. The ice surmounted 
 these summits, and left considerable deposits of till and gran- 
 itic boulders upon them, near the residence of D. H. Pricer, 3 
 miles south of Salem, and at various places along the ridge 
 road south to Bainbridge as far as Henry Benner's. Near D. 
 H. Pricer's, at an elevation of 550 feet (B) above Bainbridge, 
 was a boulder of hornblendic rock, about 5x3x3 feet. Many 
 boulders 3^ feet through appeared at this elevation farther 
 south. 
 
 PAXTON TOWNSHIP. 
 
 No till was observed in Paxton township, except near the 
 woolen factory on Buckskin Creek, whence it appears at in- 
 tervals both on the road leading up the creek to the north. 
 
PLATE XIV. 
 
 PLATE XV. 
 
68 'Detailed Report for Ohio. 
 
 and also on the road to the right, leading upon the hill along 
 which we marked the line of till and boulders in Paint town- 
 ship. A little till also appears in the northwestern corner of 
 the town, near Rocky Fork. 
 
 Bainbridge is in a valley about a mile wide, which has been 
 cut down through parallel strata of sand rock and shale to a 
 depth of about 500 feet. The village is built upon a terrace 
 whose surface is about 25 feet above high-water mark. The 
 material varies from coarse sand to well-rounded pebbles 4 or 5 
 inches through. Limestone prevails, though granite is also 
 present. A granitic boulder 4 feet in diameter was observed. 
 One mile west of Bainbridge the terrace rises suddenly 15 feet. 
 Just below the junction of Rock Pork till appears in small 
 hillocks. The elevation is 135 feet (B) above Bainbridge. 
 From this point to Hillsboro, in Highland county, signs of 
 glaciation are continuous. 
 
 PIKE COUNTY. 
 
 Following south from Paint Creek, along the Ross county 
 line, till disappears suddenly one-quarter of a . mile north of 
 Cynthiana, in the extreme northwest corner of Pike county. 
 To the west and southwest till is abundant. 
 
 HIGHLAND COUNTY. 
 The boundary enters Highland county, near the northeast 
 corner of Brush Creek township, and continues, in a south- 
 west direction to Marshall township, about one mile north of 
 its southeast corner. The deposits are continuous along the 
 road from Cynthiana to Carmel post office, south southwest to 
 the school-house by J. West's, near the head of the middle fork 
 of Brush Creek, and three-quarters of a mile south of the road 
 from Sinking Spring to Marshall. To the southeast of this 
 line across Brush Creek township, there are hills of sand rock 
 and shale of great height. On the east side of these hills, two 
 miles south of Carmel post ofBce, near the residence of D. W. 
 Scammahorn, there is, however, an extensive deposit of till, 
 which continues on the road south nearly to Baker's Fork, but 
 there disappears. From this point around to Cynthiana no 
 till was observed. 
 
Detailed Report for Ohio. 69 
 
 MARSHALL XOWJifSHIP. 
 
 There are heavy deposits of till all over the northern part 
 of Marshall township. It is specially abundant south and 
 west of the village, with many granitic boulders 3 and 4 feet 
 in diameter. Towards the southeast part of the town the 
 spaces upon which there is no till are extensive. But at the 
 coruer, by Jacob Kesler's, is a small deposit of till, with gran- 
 itic boulders. There is none upon the road east to Brush 
 Creek, and none south to Jackson township. The distance 
 from eacii of these townships is about a mile. But a half mile 
 west from M-r. Kesler's an extensive and deep deposit of till 
 begins, and is continuous to the west for at least a mile. 
 
 JACKSON TOWNSHIP. 
 
 The moraine may be said to enter Jackson township one 
 mile northwest of Korth Uniontown. Upon the road from 
 Marshall to Belfast till is continuous to the west branch of 
 Elk Kun, and on the roiid from Uniontown to Belfast there is 
 no till for two miles. Upon descending to Elk Run, near 
 R. B. Matthew's, granitic pebbles appeared at an elevation of 
 50 feet above the bridge. Upon ascending the west bank 
 there were occasional appearances of till all along, which, at 
 the cemetery, near J. Weaver's, one-half mile northeast of 
 Belfast, was very abundant. From Belfast, upon the pike 
 towards Hillsboro, saw no till for three miles ; but there Wiis 
 an occasional boulder, one of which, a mile north of the town- 
 ship line, was between 3 and 4 feet in diameter. North of 
 this, till was continuous. West of Belfast no till appeared in 
 the valley of Brush Creek ; but two miles northwest, near 
 Joseph McCoy's, was a considerable deposit of till. Granitic 
 pebbles occurred upon the ridge a mile farther south, near the 
 school-house, by Mrs. Phoela Ford's. This is at an elevation 
 of 600 feet (B) above Cincinnati, and 400 feet (B) above Bel- 
 fast. On the Ridge road from here to Newmarket there was 
 scarcely any till, but scattered granitic pebbles. The elevation 
 is between 600 and 700 feet (B) above Cincinnati. From New- 
 market there was a continuous sheet of till, in places very 
 deep. 
 
70 Detailed Report for Ohio. 
 
 Along the town line south of Fairfax to Adams county 
 there is a continuous and extensive accumulation of till at an 
 elevation of 650 feet above Cincinnati. Upon the road run- 
 ning southeast from Fairfax granitic boulders are occasionally 
 found for three-quarters of a mile, but beyond that are absent, 
 and no more could be found upon the east side of Eocky Run. 
 
 ADAMS COUNTY. 
 
 The boundary line of the glaciated region enters Adams 
 county in the northwest corner of Scott township, near the 
 line between Concord and Jackson townships, in Highland 
 county. Between Winchester Post Ofl&ce and Mount Lee the 
 till is nearly continuous, though not deep. The west fork of 
 Brush Creek is remarkably free from drift material, and no till 
 appears upon the road from Mount Lee to North Liberty. 
 On the railroad from Winchester to Youngsville, on the east 
 side of Elk Run, two miles from Winchester, is a cut in till 
 from 10 to 30 feet in depth. Angular granitic boulders are 
 found near here from 3^ to 3 feet through. On the road 
 northwest from North Liberty large deposits of till occur, 
 near Elk Run, two miles southeast of Winchester Village. 
 The deposit was from 5 to 30 feet in depth. In driving from 
 Winchester to Eckmansville, on the south border of Wayne 
 township, till is continuous to within a mile of Eckmansville, 
 where it disappears. On turning southwest from Eckmans- 
 ville, across the northwest corner of Liberty township, the 
 deposit of till is re-entered near the county line. 
 
 BROWN COUNTY. 
 
 On the road from Eckmansville to Ripley till is continuous 
 through Byrd township. Two miles and a-half southwest of 
 Decatur, near the Christian Church, and not far from Jeffer- 
 son Post Ofi&ce, is a granitic boulder 3 or 3 feet through. Till 
 continued to Red Oak Post OfiBce, in Jefferson township. The 
 road from here to Ripley descended through a gorge 450 feet 
 deep. Found some small pebbles upon the summit of the hills 
 north of Ripley ; also, in Lewis township, upon the summit of 
 the hills, 3 miles north of Higginsport, found thin deposits of 
 
PLATE XVI. 
 
 PLATE XVn. 
 
72 Detailed Report for Ohio. 
 
 till. A granitic boulder, measuring 3^x2^, and 1^ feet out of 
 ground, was found in a small brook about half way up these 
 hills. Franklin and Washington townships, in Clermont 
 county, I have not examined, but I presume the glacial boun- 
 dary approaches pretty close to the river. (See remarks below 
 upon Kentucky.) Mr. Charles W. Smith informs me that 
 there are small granitic boulders on the high lands two or 
 three miles northeast of Eipley, and that on the highest hills 
 in Ohio, opposite Augusta, Ky., pebbles of diorite and jasper 
 are abundant ; but diligent search upon the Kentucky hills, 
 near Augusta, disclosed nothing but local debris of the strati- 
 fied rocks of the region, except an occasional quartz pebble as 
 large as the end of one's finger. 
 
 HAMILTON COUNTY. 
 
 At Walnut Hill Station is an extensive deposit of till from 
 10 to 20 feet in depth. Scratched stones and small granitic 
 fragments are abundant in it. This is about 350 feet above 
 the river. At North Bend the Cincinnati, Indianapolis and 
 St. Louis Railroad passes from the valley of the Ohio to the 
 valley of the Miumi by a tunnel, through an extensive deposit 
 of till. The height of this deposit above low water-mark is 
 upwards of 160 feet. No large granitic pebbles were seen in 
 it, buL the examples of striated pebbles were numerous and 
 excellent. Below North Bend the space between the Ohio 
 and the Miami is occupied by a remnant of the limestone 
 plateau through which the rivers have worn their present 
 deep channels. This is 375 or 400 feet (B) above the river, 
 and is about 4 miles long and 2 miles wide. Till and granitic 
 pebbles 2 feet through are found upon this summit. They 
 are also found in Indiana upon the summit, of equal height 
 to the west and southwest, across the broad valleys of the 
 Miami and the White Water. 
 
Detailed Report for Ohio. 73 
 
 KENTUCKY. 
 
 The glacial boundary enters Kentucky in Campbell 
 CouKTT, crossing the Ohio Eiver about two miles north of 
 the Pendleton county line. I have not examined sufficiently 
 the northern part of Campbell county, and I can only fix the 
 limit near the river. We crossed the river from New flich- 
 mond, in Ohio, and ascended through the channel of a small 
 brook to the summit of the Kentucky hills, near Carthage. 
 These hills are about four hundred feet above the river, and 
 the ascent is very steep. Granitic pebbles were numerous in 
 the bed ot this small stream, and, upon reaching the summit, 
 we found the surface covered with till to the depth of ten or 
 fifteen feet, in which granitic boulders a foot through were 
 numerous, and in which it was not difficult to find beautiful 
 specimens of scratched stones. From this point we went 
 south, keeping upon the summit of the plateau from one and 
 a half to three miles from the river. Indications of glacial 
 action continued, but in a somewhat diminishing degree, 
 until reaching Flag's Spring, where they ceased entirely. 
 But to make sure, we went on in the same direction about 
 four miles farther, and came down to the river at Metier, 
 without seeing any farther glacial marks. At Flag's Spring 
 there is an extensive accumulation of post-glacial conglom- 
 erate like that at Split Rock, soon to be described. 
 
 KENTON COUNTY. 
 
 My examination of Kenton county has been too brief to be 
 very satisfactory, but what I have seen may serve as a guide to 
 others. Three miles southwest of Covington the hills are 
 covered with loam from 15 to 40 feet deep, at an eleva- 
 tion of 400 feet (B) above the river. There are occasional 
 small quartz pebbles in this loam ; but I saw no sure signs of 
 the actual presence of ice. In my notes I have said : "This 
 seems like the bottom of a temporary lake when the ice 
 dammed the river below." On going across from the piUe a 
 little south of this, so as to strike the Licking River, two miles 
 
74 Detailed Report for Ohio. 
 
 south of Covington flats, no glacial marks were observed. At 
 Erlanger, however, the first station south of Ludlow, on the Cin- 
 cinnati Southern Railroad, a railroad cut shows clay to a depth 
 of six feet or more containing pebbles of quartzite, limestone, 
 and occasionally granite, near the bottom. All, however, 
 were small, none of them more than three inches in diameter. 
 The elevation is about five hundred feet above the river. 
 
 BOONE COUNTY. 
 
 The glacial deposits over the northern part of Boone county 
 are unmistakable in character. On ascending the hill along 
 the line of the Covington and Petersburg pike from Ludlow 
 to Hebron, we encountered about one mile east of Hebron, 
 and about 450 feet (B) above the river, a deposit of till, twelve 
 or more feet of which in depth is exposed by a little stream 
 running to the north. The whole surface of the country 
 about Hebron is covered with a loamy deposit containing oc- 
 casional scratched stones and granitic boulders. On ascending 
 the hill from Taylorsville to Hebron small granitic boulders 
 abound all along the bed of the little stream, and are found of 
 considerable size in the clay upon the summit. On the pike 
 between Florence and Burlington, and two miles west of Bur- 
 lington, where a small tributary of Gunpowder Creek, which 
 runs to the south, crosses the pike, a large number of granitic 
 boulders are collected, they having been washed out of the till 
 which caps the hills. The elevation above the river is 400 
 feet (B). Three-fourths of a mile to the east the elevation is 
 575 feet (B), and the headwaters of. this tributary, a mile and 
 a half or two miles north, near Hebron, are 500 feet (B.) I 
 counted within a few rods of each other 15 granitic boulders, 
 one of which measured 2-^ feet in diameter. There were three 
 or four boulders composed of metaphoric conglomerate, con- 
 taining the beautiful red jasper pebbles characteristic of the 
 eastern shore of Lake Superior, and of the region north of 
 Lake Huron. They are identical in composition with boul- 
 ders that are scattered over Michigan, Northern Indiana, and 
 with one in the Oberlin Museum, found by Professor Allen 
 in Brownhelm. Colonel "Whittlesey brought a mass of this 
 
Detailed Report for Ohio. 75 
 
 rock from its native ledge, near Lake Superior, on the west 
 side of St. Mary's Kiver, and has adorned the yard in front of 
 his residence with it. These boulders in Kentucky are 
 found about five miles south of the Ohio River, and south of 
 the watershed in that part of the county. 
 
 In a drive from Petersburg to Hebron, the hills were found 
 to be covered with till to a height of several hundred feet. 
 The barometer read about 400 feet above the river. The red- 
 ness of the soil was everywhere noticeable, showing that the 
 iron was thoroughly oxidized. A detour to the south, from 
 Florence to Union, and from Union across Gunpowder Creek, 
 towards Bellevue (now called Grant P. 0.), demonstrated the 
 absence of glacial deposits until reaching the headwaters of 
 Middle Creek, about half way between Burlington and Belle- 
 vue. Here the tops of the hills are covered with a gravelly 
 deposit, containing occasional grr.nitic pebbles several inches 
 in diameter. Near the headwaters of the southern branches 
 of Middle Creek, and especially at Rock Spring, the deposits 
 are of very coarse material, are of great extent, and are 
 cemented together by an infiltration of lime like that already 
 spoken of at Flag's Spring, and soon to be described at Split 
 Rock. This conglomerate consists largely of pebbles of lime- 
 stone, but contains also granitic pebbles. It, was noticed as 
 early as 1845 by Professor Locke, and described in the Cin- 
 cinnati Gazette, and more recently by Dr. Sutton, of Aurora, 
 who specially notices its great elevation above the river. Dr. 
 Sutton's paper may be found in the proceedings of the A. A. 
 A. S. for 1876, and reprinted, with additional information by 
 Prof. E. T. Cox, in the Geological Survey of Indiana for 
 1878, pp. 108-113. 
 
 The most accessible place in which to study this deposit is 
 near the mouth of Woolper Creek, about four miles north, 
 west of the headwaters of Middle Creek, and about four miles 
 south of Petersburg. The formation' is here known as "Split 
 Rock," and rises directly from the Ohio River, both above and 
 below the mouth of Woolper Creek. Professor Locke "re. 
 garded this conglomerate as evidence of the destruction of a 
 great arch of rocks which united the coal-fields of Ohio with 
 
76 Detailed Seportfor Ohio. 
 
 those of Indiana and Kentucky." Mr. Eobert B. Warder, in 
 the Geological Eeport of Indiana, for 1873, also directs atten- 
 tion to this Split Eock conglomerate, and suggests, possibly, 
 it is the terminal moraine of an ancient glacier. With this 
 view Dr. Sutton and Professor Cox substantially agree. But 
 Dr. Sutton and Prof. Cox suppose that the deposits upon the 
 highland above Middle Creek are far more ancient than those 
 in the valley of the Ohio about the mouth of Woolper Creek. 
 As we read the facts, however, now, in the light of the most 
 recent investigations, these deposits upon the highlands of 
 Boone county, and at Split Eock, are probably contempora- 
 neous, the ice of the glacial period extending down to a con- 
 tinuous line which crosses the river at Woolper Creek. The 
 vast current of water which flowed down at the melting of 
 the continental glacier, was not determined in its course by 
 the present channels as now, for these were in many cases 
 filled with ice, and for a time the southward flowing currents 
 were borne completely across the channel of the Ohio, flowing 
 in a trough of ice, whose bottom was as high as the summit of 
 Boone county. 
 
 The pebbles in the cemented mass of Split Eock are mostly 
 of limestone, and are very coarse — individual pebbles fre- 
 quently being from three to four feet in diameter. Granitic 
 pebbles are infrequent. One was found, however, measuring 
 two feet in diameter. The cliffs of this conglomerate, at the 
 mouth of Woolper Creek, rise not far from one hundred feet 
 above the river, and the material is cemented together by an 
 infiltration of lime. Kame-like ridges extend for two miles 
 south of Woolper Creek, on the way to Bellevue. These are 
 composed of rather fine material, and are 160 feet above the 
 river. The terrace upon this, the Kentucky side of the river, 
 is, for two miles or more below Woolper Creek, remarkable for 
 its height, being more than 100 feet above the river, and 56 
 feet higher than the high-water mai'k of 'January, 1883. 
 
APPENDIX. 
 
 ABSTRACT OF THE BEARINGS OF GLACIAL 
 STRI^ AND GROOVES IN OHIO. 
 
 COMPILED BY COL. CHARLK.S WHITTLESEY. 
 
 NORTHEASTERN COUNTIES. 
 
 Ashtabula County — 
 
 No observations, the rocks principally sliale. 
 
 Tbumbull County — 
 
 Farmington townsliip S. 30° West. 
 
 Vernon township S. 20° 30° and 40° East. 
 
 Brookfield S. 5° Eat. 
 
 Over the Pennsylvania line, Shenango Valley S. 5° East. 
 
 Fowler township 8. 4°, 30° and 45° East. 
 
 Braceville S. 45° and 50° "West. 
 
 Lordstown South and S. 20° East. 
 
 Mahoning County Line— 
 
 Austintown S. 30° and 35° East. 
 
 Average of four exceptional observations, S. and W. S. 31° West. 
 Average of ten observations to the East of South, 8. 22 4-10° East. 
 
 Geauga County — 
 
 Thompson 8, 40° and 50° West, and 50° East. 
 
 Hampden 8. 10° and 15° East. 
 
 Chardon S. 10° East, 
 
 Chester S. 50° and 70° East. 
 
 Russell 8. 50° and 70° East. 
 
 Bainbridge S. 49° East. 
 
 Parkman 8. 30° West. 
 
 Lake County — 
 
 Leroy 8. 45° West. 
 
78 Appendix. 
 
 Portage Countt— 
 
 Mantua S. 30° and 40° East. 
 
 Four observations W. of Soulli Mean S. 41° West. 
 
 Ten observatiODS E. of South S. 374-10° East. 
 
 Ctjtahoga County — 
 
 Solon S. 45° East. 
 
 Euclid S. 20° and 25° East. 
 
 Independence S. 20° East. 
 
 Average S 27 1-3° East. 
 
 Summit County — 
 
 Portage near Akron S. 10° to 35° East. 
 
 N. Hampton S. 30° to 60° East. 
 
 N. Hampton S. 30° and 35° East. 
 
 Middlebury, exceptional East and West. 
 
 Tallmadge Coal Hill S. 30° and 40° East. 
 
 Cuyahoga Falls 8. 45° East. 
 
 Twinsbury ' S. 40° and 45° East. 
 
 Medina County — 
 
 Copley S. 30° West- 
 Sharon S. 40° East. 
 
 Waynb County— 
 
 Doylestown West and South. 
 
 Average, not anomalous S. 36 6-10° East. 
 
 WEST END OP LAKE ERIE. 
 
 Between Buffalo at the East end of this Lake, and the Inlands, the 
 rocks near the water level are generally too soft to retain the ancient 
 ice-markings. On the lime rock at Buffalo, there are numerous and dis- 
 tinct etchings, that bear from South 25° to South 30°West, and run under 
 water. Their bearings aie nearly parallel with the axis of the trough of 
 the Lake. At the mouth of Detroit River, near Gibraltar, the limestone 
 beds are grooved andpolished.and the bearings are also South 30° West. 
 The Islands, and the limestone shores to the South and West, are every- 
 where scoured and grooved in ihe same way; but the bearing is generally 
 more to the West, differing by nearly a right angle with the general bear- 
 ing in the Northeastern Counties. 
 
 Kbllby's Island and Adjacent — 
 
 Southeast corner, ac water level, long grooves 8. 75° West. 
 
 Southeast corner, cross striae N. 80° West. 
 
 Cdlkins' Quarry, north side, deep grooves S. 80° West. 
 
Appendix. 79 
 
 Kellbt's Island, and Adjacent — Continved — 
 
 Calkias' Quarry, strise S. 70° West. 
 
 CalkiDs' Quarry, water level, striae N. 80° West. 
 
 Calkins' Quarry, one heavy groove S. 45° West. 
 
 Calkins' Quarry, one strise 8. 60° West. 
 
 Mean of twelve observations in different parts of Island, S. 80° West. 
 
 West Sister Island, mean S. 80° West- 
 
 Put-in-Bay, mean of twenty observations S. 80° West. 
 
 Sandusky City, mean of four observations S. 78° West. 
 
 Sandusky City, mean of two observations S. 80° West. 
 
 Sandusky City, mean of one observation 5. 81° West. 
 
 Erie County — 
 
 Belleville S. 75° West. 
 
 Belleville S. 65° West. 
 
 Ottawa ConNTY — 
 
 Geneva S. 65° West. 
 
 Lucas County — 
 
 Sylvanus, five observations S. 50° West. 
 
 Monclova, four observations ,S. 63° West. 
 
 Whltehouse S. 50° West. 
 
 Near Maumee River, seven observations S. 62° West. 
 
 Wood County — i 
 
 Portage, three observations S . 50° West. 
 
 Otsego, three observations S. 64° West. 
 
 Defiance S. 45° West. 
 
 Paulding County— 
 
 Junction, three observations S . 45° West . 
 
 Van Wert County — 
 
 Middlepoint, two observations S. 15° West. 
 
 Hancock County— 
 
 Findlay, three observations S. 43° West. 
 
 Putnam County — 
 
 Blanchard S. 20° West. 
 
 Sugar Creek S. 50° West. 
 
 Auglaize County — 
 
 Auglaize S. 48° West. 
 
80 Appendix. 
 
 Seneca Cottntt — 
 
 Seneca S. 5° East. 
 
 Senrca S. 23° West. 
 
 Wtaudotte County — 
 
 Crawford S.20°West. 
 
 Crane S- 5° West. 
 
 Marseilles S. 10° West 
 
 Marion County — 
 
 Grand Prairie North and South. 
 
 Miami County- — 
 
 Troy Glaciated surface: hearings not given. 
 
 Highland County — 
 
 Near Lexington, according to Professor Orton, very marked roches 
 moutonnees. Dr. John Locke, in the Second Eeport of the First 
 Geological Survey, 1838, page 230, has given a fae simile of pol. 
 ished limestone from Light's quarry, near Dayton, Montgomery 
 County. It was done by placing a surface block in a ruling ma- 
 chine, by which it engraved itself to perfection. The grooves are 
 from the 1-40 to the ^ of an inch deep, and from a line to f of an inch 
 wide. Both the grooves and tbe finer striae are in groups, or fas- 
 cicles, as high as ten in number. They were perfectly straight, and 
 covered by two feet of earth. The average bearing is about S. 26° 
 East, ranging from 19° to 21°, 31° and 33°; but the greater number 
 of the most pronounced are S. 26° East. 
 
 The above abstract is compiled from the observations of Professors 
 Newberry, Read, Winchell, and Gilbert of the Second Ohio Survey, and 
 from those of Colonel Whittlesey. Most of the irregular and exceptional 
 bearings can be accounted for by the local topograpliy turning aside tbe 
 general movement. The highest elevations are 625 to 650 feet above the 
 Lake, above which the ice sheet must have risen several hundred feet. 
 
Appendix. 81 
 
 EFFECTS OF THE GLACIAL DAM AT CIN- 
 CINNATI ALONG THE UPPER BASIN 
 OF THE OHIO. 
 
 BY PKOPESSOK I. C. WHITE, 
 
 OF THE PENNSYLVANIA GEOLOGICAL SURVEY. 
 
 Among the papers read before the geological section at the recent 
 meeting of the American Association for the Advancement of Science 
 at Minneapolis, 1883, was the following by Professor I. C. White, of 
 the University of West Virginia, on the Olacial Dam at Cincinnati, 
 and the evidences of the West Virginia portion of tlie vast lake made 
 by that dam : 
 
 "In a paper read before the Boston Society of Nafural History, March 
 7, 1883, Rev. G. F. Wright has shown that the southern rim of the great 
 northern icesheet crossed the Ohio River, near the site of New Rich- 
 mond, a few miles above Cincinnati. Mr. Wright believes that one 
 effect of this invasion of the Ohio Valley by ihe glacial ice, was to form 
 an immense dam of ice and morainic debris 500 or 600 feet high, which, 
 effectually closed the old channel way, and set hack the water of the 
 Ohio and lis tributaries, until ri.sing to the level of the Licking River 
 flivide, it probably found an outlet through Kentucky around the glacial 
 (lam. As this divide is 500 or 600 feet higher than the present bed of 
 the Ohio at Cincinnati, Mr. Wright states that the site of Pittsburgh 
 would have been submerged to the depth of 800 feet, and adds: It 
 remains to be seen how much light this may shed upon the terraces 
 which mark the Ohio and its tributaries in Western Pennsylvania. 
 
 "Having resided for nearly a score of years in the valley of the Monon- 
 gahela River, the writer is necessarily familiar with its terraces and sur- 
 face deposits in general ; and in reply to the above query of the eminent 
 glacialist, would answer that his admirable work throws a flood of light 
 upon the Monongahela terraces, and proffers for them and the deposits 
 along other tributaries of the Ohio, the only satisfactory explantion 
 that has ever been advanced. 
 
 "Of course, if the Ohio River was ever so obstructed for any consider- 
 able period of time, it would follow, as a necessary result, that many of 
 the tributary streams and the Ohio itself above the limit of the dam, 
 
82 Appendix. 
 
 would have their old valleys silted up with vast heaps of trash — clay, 
 sand, gravel, boulders, drifted logs and other rubbish — carried down by 
 the streams from the region not sheeted with ice, and dumped into the 
 great inland lalie stream which extended from Cincinnati far up toward 
 (he sources of the Monongahela. 
 
 " That the valley of the latter stream has been refilled with trash during 
 some period of its history to a height of 350 or 300 feet above its present 
 bed, the evidence is most conclusive, for the remnants of this deposit 
 still cover the surface to a great depth in long lines of terraces extending 
 from Pittsburgh, Pa , southward along the river to Fairmount, W. Va., a 
 distance of 130 miles, and very probably much further, as 1 have never 
 examined the river valley above the latter town. 
 
 "The striking peculiarity of these terrace deposits is that they suddenly 
 disappear at an elevation of 1050 or 1075 feet above tide, not a single 
 rounded and transported boulder ever being found above the latter hori- 
 zon, though occurring in countless numbers below this level. 
 
 "The hills along the river often rise 300 or 400 feet higher than the 
 upper limit of the deposits, so that there can be no mistake about the 
 elevation at which the terrace deposits disappear. The composition of 
 these great he.Tps of surface debrit is, along the immediate valley of the 
 river, a heterogeneous mixture of sand, clay, gravel, rounded boulders 
 of sandstone of every size, from an inch in diameter up to four feet, 
 pieces of coal, leaves, logs of wood, and every other species of rubbish 
 usually transported by streams. Back from the channel of the river, 
 however, and especially where the surface configuration would make 
 quiet water, there occur thick deposits of very fine, bluish white clay, in 
 which great numbers of leaves are most beautifully preserved. These 
 clays have been extensively used for the manufacture of pottery at 
 Geneva and Greensboro, Pa., and also to some' extent at Morgan town 
 and Fairmount, W. Va. Though the clay deposits occur at nearly 
 every horizon, they are purest near the upper limit of the terraces, and 
 these are consequently the only ones that have hitherto been much 
 explored. 
 
 " In the vicinity of Morgantown, terraces of transported material occur 
 at the following approximate (measured by barometer) elevations : 
 
 
 Ft. above 
 river. 
 
 Ft. above 
 tide. 
 
 
 30 
 75 
 ,17s 
 200 . 
 
 275 
 
 
 Second Terrace 
 
 Third Terrace 
 
 865 
 965 
 990 
 1065 
 
 
 Fifth Terrace 
 
 
 ' ' The first terrace is the present flood-plain of the river, consisting prin- 
 cipally of fine sand, mud and gravel. It seems to possess some respect- 
 
Appendix. 83 
 
 able antiquity, however, since Mr. Walter Hough, one of my students, 
 dug some teeth and bones from five feet below its top, which were iden- 
 tified by Professor O. C. Marsh, as the remains of a species of peccary, an 
 animal that has not inhabited the region in question within the Ameri- 
 can historic epoch. 
 
 " All of the other terraces have thick deposits of transported material, 
 wherever the original contour of the surface has favored its preservation 
 from erosion. From the top of the fourth teirace Mr. Keck dug a well 
 through 70 feet of clay, gravel and boulders without finding bed rock. 
 He also encountered logs of wood in a soft or semi-rotten condition near 
 the bottom. 
 
 "Many other wells on the third terrace have been sunk to depths of 20 
 and 30 feet without reaching bed rock. 
 
 " The fifth terrace of this Morgantown series marks the height to which 
 the pre-glacial valley of the Monongahela was silted up, partially or 
 entirely during the existence of the glacial dam at Cincinnati, since, as 
 already stated, no clay beds, rounded boulders, or other transported 
 material are ever found above its top, but instead only angular fragments 
 of the country rock, and thin coverings of surface material which has 
 accumulated, jn siiu. 
 
 "Owing to the considerable elevation — 375 feet — of the fifth terrace 
 above the present river bed, its deposits are frequently found far inland 
 from the Monongahela, on tributary streams. A very extensive deposit of 
 this kind occurs on a tributary one mile and a half northeast of Morgan- 
 town, and the region, which includes three or four square miles, is signifi- 
 cantly known as the 'flats.' The elevation of the 'fla's' is 375 feet above 
 the river, or 1065 feet above tide. The deposits on this area consist almost 
 entirily of clays and fine sandy material, there being very few boulders 
 intermingled. The depth of the deposit is unknown, since a well sunk 
 on the land of Mr. Baker passed through alternate beds of clay, fine 
 sand, and muddy trash to a depth of 65 feet without reaching led rock. 
 In some portions of the clays which make up this deposit, the leaves of 
 our common forest trees are found most beautifully preserved. Whether 
 or not they show any variations from the species growing in that region, 
 the writer has not yet had time to determine, but when a larger collec- 
 tion has been obtained, this subject will receive the attention that it 
 deserves, since if the date of the glacial epoch be very remote, the 
 Species must necessarily show some divergence from the present flora. 
 
 " Of animal remains the only fragmentyet discovered in this highest of 
 the terraces is the tooth of a mastodon, dug up near Stewartstown, 
 seven miles northeast from Morgantown. 
 
 " The other tributaries of the Monongahela, on which the writer has 
 noted the clay and other deposits of the fifth terrace, are Decker, Dun- 
 kard, Whitely, Muddy, and Ten Mile creeks, and in each case the depos- 
 
84 Appendix. 
 
 its disappear at the same absolute level at which they cease along the 
 river. 
 
 "The Great Kanawha River, another principal tributary of the Ohio, 
 draining a region that was never glaciated, also exhibits water-worn 
 boulder deposits which disappear at 300 to 300 feet above the present 
 level of that stream, though I have not determined the exact limit. 
 
 "The glacial dam at Cincinnati presents a complete explanation for the 
 origin of Teazes valley, an ancient, deserted river channel 30 miles long 
 and one or two miles wide, which leaves the Great Kanawha 15 miles 
 below Charleston, W. Va., at Scary, and passing through Putnam and 
 Cabell counties, extends to the valley of Mud River, a tributary of the 
 Guyandotte, which empties into the Ohio at Huntingfon. 
 
 "This valley, although having an elevation of 300 feet or more above 
 the Kanawha, is filled to a great depth with rounded boulders of sand- 
 stone, chert, cannel coal, and other trash, which has plainly been trans 
 ported down the Kanawha from above Charleston, so that although it 
 was clearly seen that the water of the Kanawha had once found an out- 
 let to the Ohio by way of thii valley and the Mud and Guyandotte 
 rivers, yet why this ancient channel should have beeu abandoned for the 
 present much more circuitous one had always remained a inystery uuti' 
 Mr. Wright furnished the key in the discovery of the great ice dam at 
 Cincinnati. For it is now clear that such a barrier would set back the 
 water of the Kanawha, until rising above the divide which had previously 
 .■separated it from Mud River, it sent an arm across to the Ohio by way of 
 the Guyandotte 50 miles below where the other arm and main stream 
 reached the same river at the present mouth of the Kanawba, thus con- 
 verting portions of Putnam, Mason and Cabell counties Into a large, 
 tri-ingular island, the base of which was formed by the swollen Ohio, 
 and the sides by the two arms of the Great Kanawha. The meltina; 
 away of the Cincinnati dam withdrew the water from the western or 
 Mud- Guyandotte arm of the Kanawha, leaving the abandoned valley 
 high and dry, but littered up with transported trash, as we now see it, 
 while the Kanawha continued on to the Ohio in its present and pre- 
 glacial outlet. 
 
 " A summary view of these and other facts in the writer's possession 
 seems to prove, beyond any reasonable doubt, that Mr. Wright's hypoth- 
 esis concerning the damming up of the Ohio by the glacial ice in the 
 region of Cincinnati was an actual reality ; that during the period of its 
 continuance the principal tributaries of the Ohio had their valleys filled 
 with sediment carried down and dumped into them by the mountain 
 torrents, and other streams which drained the area south from the 
 gliiciated region ; that subsequently, when the barrier disappeared, the 
 rivers recut their channels through the silt deposits, probably by spas- 
 modic lowering of the dam, in such a manner as to leave the deposits in 
 
Appendix. 85 
 
 a series of more or less regular terraces, which, in favored localities, sub- 
 sequent erosion has failed to obliterate, though from steep slopes it has 
 removed their every trace. 
 
 "The elevation of this dam at Cincinnati, as determined from the upper 
 limit of the fifth Monongahela river terrace, would be somewhere 
 between 1050 feet and 1075 feet above tide, or about 635 feet above low 
 water there in the present Ohio." 
 
 Professor White has still more recently (see The Virginias for Sept., 
 1883,) called attention to additional and confirmatory evidence, con- 
 sisting of small, rounded boulders on the summit of the knob in Sisters- 
 ville, Tyler county, West Virginia, between five hundred and six hundred 
 feet above the river. 
 
 Certain phenomena in Boyd county, Ky., which had been referred to 
 as evidence of direct glacial action I found on examination to be also 
 natural results of the supposed ice dam. 
 
 Boyd county is in Northeastern Kentucky, bordering upon West Vir- 
 ginia, and upon the remarkable bend of the Ohio River where it receives 
 the waters of the Big Sandy. Through the attention of Mr. John Camp- 
 bell of Ironton, O., and Mr. J. H. Means of Ashland, Ky., I was assisted 
 in making a pretty thorough examination of the region. Upon going" 
 back about two miles into Kentucky from the Ohio River, opposite 
 Ironton, we find ourselves in a valley two miles wide, running parallel 
 with the Ohio River, and two hundred and twenty feet above it. This 
 valley extends for many miles, reaching the river towards the west at 
 Greenup, and continuing some miles, at least, above Ashland. It is 
 known as Flat Woods. The level is remarkably uniform; and the hills 
 upon either side of it rise about two hundred feet, with numerous lateral 
 openings toward the Ohio. When upon the farther side, and looking 
 northward, one sees the reeky bluffs of the old channel rising so like 
 those facing the river itself that he can scarcely resist the illusion that 
 he is in the present valley of the stream. The supposed glacial phe- 
 nomena consist of numerous water-worn pebbles of quartz and quartzite 
 scattered along the whole range of this old valley. Most of the pebbles 
 are small, and perfectly rounded, though some were a foot or more in 
 diameter; and one observed was about two feet and a half through, 
 and only slightly worn. These pebbles are not found upon the hills 
 back from this channel, on the Kentucky side, nor, according to Mr. 
 Campbell, who is a most competent witness, anywhere in Lawrence 
 county, O., back from the river. Plainly enough they are the result of 
 water-transportation. Whether they were deposited at the very early 
 period tvhen the Ohio flowed at the level of two hundred and twenty 
 feet higher than now, and regularly occupied this old channel, or 
 whether they were brought into place during the existence of the glacial 
 dam which I have supposed at Cincinnati, 1 will not venture to say; 
 though the latter theory would seem more in accordance with the facts 
 
86 Appendix. 
 
 published by Professor White concerning the old channel followed by 
 the Chesapeake and Ohio railroad, extending from the Kanawha River 
 to the mouth of the Guyandotte in West Virginia. The elevation of the 
 Kanawba-Guyandotte channel is nearly the same as that of the one I am 
 describing, and this seems to be a prolongation of that. At any rate, 
 the pebbles can only be indirectly referred to glacial action, and would 
 be a very natural result of my theoretical ice dam at Cincinnati. 
 
 In Science for Sept. 28, 1883, Mr. G. H. Squier describes some phe- 
 nomena observed by him in the valley of the Licking and its larger 
 tributaries in Kentucky which had independently, though on less direct 
 evidence, led him to the same conclusions with myseU as to the existence 
 of an ice dam near Cincinnati. Mr. Squier has kindly furnished me 
 in a private letter many additional facts for which I gladly give him 
 credit. 
 
 In Bath county he found over an extensive region of low table land, 
 between Slate Creek and Licking River, and for some distance to the 
 north, large numbers of water-worn pebbles, composed of white quartz, 
 chert, black shale and sandstone, and most remarkable of all, fragments of 
 water-worn coal. These are spread not only over the low table land and in 
 the valleys, but over the lower hills; but do not extend vertically as high 
 as the watershed. The pebbles of sandstone and coal must have been 
 brought down the streams at least twenty miles, and it is evident that 
 they could not have been left upon this table land and these low hills 
 by running water. The Cincinnati ice dam supposed would furnish 
 the required conditions by making a temporary lake into which floating 
 ice from the east could bring and deposit the materials in the situations 
 indicated. To use Mr. Squier's own words, " The general level of the 
 area near the junction of Slate Creek and Licking River is so low that, 
 save a few hills, it must have all beea overflowed [during the existence of 
 such an ice dam] and the great body of floating ice from above must, 
 
 of necessity, have passed directly across it. " So strongly did the above 
 facts point to a temporary damming of the river, that even in the face 
 of what I regarded as improbable I was led to the conclusion that the 
 glacier must have crossed the Ohio." 
 
 In the same number of Science (Sept. 28) Professor Lesley publishes a 
 letter in which he speaks of this dam as "furnishing precisely the expla- 
 nation we need for the local drift terraces of the Monongahela and the 
 rolled nortJiern drift terraces of the lower Allegheny, Beaver, and upper 
 Ohio rivers."