706 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. 



cited, has applied the name "Lincoln Park kame area." It consists of a 

 series of low gravel and sand knolls distributed in a belt 1^ miles long from 

 north to south and less than one-half mile wide. The largest are but 20 to 

 30 feet in height and from 200 yards to about one-fourth mile in length. 

 These knolls are recognized b}' Fairchild to be inside the frontal moraine. 



STKtJCTURE OF THE DRIFT. 



The main ridge of tlie Albion moraine apparently contains a much 

 larger percentage of till than is found in the moraines outside of it. It is 

 a clayey till, thickly set with small stones, and bears a close resemblance 

 to the ordinary till of the plains to the west of Lake Erie. Its surface is 

 liberally strewn with bowlders and so is the inner slope of the moraine. 



The small knolls and ridges on the inner slope also contain much till, 

 but the large knolls are in many instances composed chiefly of sand and 

 gravel. 



Fairchild has given a detailed description of several sections in the 

 Pinnacle Hills ridge from which it appears that the north slope and crest 

 carry a large amount of till, but the south slope and basal portion of the 

 ridge are com]wsed chieiiy of gravel and sand. The dip of the beds is not 

 westward, or lengthwise of the range of hills, nor is it from the crest toward 

 each border, as is common in eskers. In general it is southward and east 

 of south, or across the trend line. The southward dip is foimd to be most 

 pronounced in the gravels upon the north side of the range, and there is an 

 approach to horizontality in passing toward the south flank. There are 

 many local exceptions, but these have seemed to Fairchild to be in lai-ge 

 part due to disturbances by ice thi-ust, to which should pi'obably be added 

 disturbances from settling of the beds. 



Large blocks of Lockport (Niagara) limestone abound on the surface 

 and in the till of the Pinnacle Hills ridge. Their altitude reaches more 

 than 200 feet above the outcrops of this limestone in the districts to the 

 north, and yet they seem to be derived from that district within a distance 

 of 5 miles. 



In the esker near Holley there are two gravel pits near its northeast 

 end. The bedding is imperfect in the surface portion to a depth of several 

 feet, there being earthy or clayey material commingled with sand and gravel. 

 Below this depth the bedding is distinct, but it is variable, for the beds 



