OUT WASH FROM THE MIAMI LOBE. 339 



on rock at a level about 60 feet below the river bed. The well at the 

 Hotel Emory penetrated 160 feet of drift and is thought to be on rock at 

 the bottom 40 to 50 feet below low-water mark. A well on Sixth street, 

 between Horn and Harriet streets, in the midst of the valley, struck rock at 

 only 10 feet below low- water mark. On the Kentucky side, west of the 

 Licking River, the rock comes down to the river bank, and the middle pier 

 of the Ludlow^ bridge rests on the rock at the level of the present river bed 

 (J. F. James). 



No accin-ate records were obtained between Cincinnati and Lawrence- 

 burg, Ind., along the supposed new course of the Ohio. Rock is struck in 

 Lawrenceburg at about 40 feet below the river, the rock floor being reported 

 by the State geologist of Indiana to have an altitude 368 feet above tide. 



The valley of Mill Creek afforded a line of escape for waters from the 

 point of the glacial lobe, but it seems to have been less A'igorous than that 

 along the Little Miami. Well sections at Ivorydale and Cumminsville, and 

 observations along the creek, show that with the exception of a few feet at 

 the surface the drift is largely clay. There is a deposit of surface gravel 

 along the west side of the creek as far north as Hartwell, above ^vhich, 

 in the villages of Wyoming and Lockland, there is till. On the east side 

 of the creek the gravel extends up at least to Reading. Not far above this 

 village the whole width of the valley is occupied by a deposit of till. The 

 gravel, therefore, appears to head in the moraine. Sandy deposits on the 

 east border of Mill Creek Valley, in the vicinity of Bond Hill, as above 

 noted, may prove to be the product of flooded stages of the glacial stream 

 that issued from the ice sheet near Reading. 



In the Great Miami Valley there is a heavj^ accumulation of gravel, 

 having' a breadth of 1 to 3 miles, and a depth, in the deepest part of the 

 valley, of about 200 feet. The surface portion of this g-ravel probably was 

 deposited during the formation of later moraines and the deep portion at the 

 Illinoian or earlier Wisconsin. Similarly, on the Whitewater River, there 

 is a great accumulation of gravel whose surface portion apparently was 

 deposited in large part at the time when later moraines were being formed, 

 since the gravel plain extends to these later moraines. However, there has 

 been found no evidence that the escape of waters was not copious in each 

 of these valleys at the time the outer moraine was forming. If the valley 

 was built up to a higher stage at this time than when later moraines were 

 forming the remnants of its terraces have escaped notice. 



