ST. JOHNS OR SALAMONIE MORAINE. 515 



This consists of a low, nearly continuous, ridg-e whose crest and slopes are 

 scarcely more undulatory than are the adjacent plains. This inner belt 

 appears to find its continuation in a tract with morainic topography which 

 lies south of Huntington along the headwaters of Loon Creek. For several 

 miles the creek flows among a series of knolls and ridges of morainic ty^je, 

 the highest points being 12 to 15 feet in height. There are also among 

 these knolls a few basins. 



The Wabash Valley for a few miles below Huntington contains a 

 remarkably large number of bowlders. Their presence is thought to be 

 evidence that the margin of the ice sheet overhung the valley at this point 

 for a considerable period. In itself the presence of the bowlders here could 

 scarcely furnish decisive evidence of the halting of the ice sheet, but when 

 taken in connection with the morainic features which maj^ be traced to the 

 bluffs of the Wabash both from the north and the south they are of value 

 as supplementary and harmonious evidence. 



North of the Wabash, along Clear Creek Vallej^, the knolls and ridges 

 are of a subdued swell-and-sag type, the highest knolls scarcely reaching a 

 height of 20 feet. In southern Whitley County there are few knolls exceed- 

 ing 10 feet in height, but Dryer has traced a bowlder belt northward from 

 the head of Clear Creek to Eel River, and reports a well-defined smooth 

 ridge along this line,- which through a part of the distance forms a water 

 parting between the Wabash and Eel rivers. As previously remarked, it 

 is thought that this belt constitutes the continuation of the inner of the two 

 Salamonie ridges traced to the Wabash from the south. 



The combined Salamonie and Mississinawa moraines, leading from the 

 Wabash River northeastward into Michigan, have, as already noted in 

 the discussion of the Mississinawa belt, a swell-and-sag topography of 

 characteristic though subdued morainic type. 



THICKNESS AND STRUCTURE OF THE DRIFT. 



The Salamonie moraine occupies tln-oughout nearlj^ its entire length a 

 region heavily covered with drift. It includes but a small portion of this drift, 

 since it rises but little above the level of the portion of the drift sheet outside 

 it, which is evidently older than the moraine. Judging from the relief of 

 the moraine we may conclude that it consists of a sheet of drift 20 to 50 

 feet thick along- the crest. If the inner slopes be included the thickness is 



