768 



WILBUR GREELEY BURROUGHS 



covered area, the Cleveland appears, forming the customary Cleve- 

 land shale lake-cliff. Here, where the cliff is formed of the Cleve- 

 land formation, the Cleveland shale is thin-bedded with very fine, 



knifelike edges, black and brittle. Inter- 

 bedded in this type of Cleveland shale 

 is a 5-ft. bed of soft, thin-bedded, 

 greenish-gray shale, which resembles 

 closely the gray shale beside the Berea 

 sandstone. This greenish-gray shale of 

 the Cleveland is not the same as the 

 shale beside the Berea sandstone, how- 

 ever, for where last exposed the con- 

 cretionary layer, above mentioned, at 

 this point 12 ft. vertically above the 

 beach, was dipping eastward toward the 

 greenish-gray Cleveland shale 125 ft. 

 horizontally away. But no sandstone 

 layer occurs in the greenish-gray Cleve- 

 land, nor in the black Cleveland, whatso- 

 ever. The concretionary sandstone 

 layer ceased to exist when the Cleve- 

 land was reached. Hence the two gray 

 shales are not the same. 



Going once more back to the Berea 

 sandstone, we find at the water's edge, 

 under the gray shale, a jet black, rather 

 massive Cleveland shale, harder and 

 heavier than the Cleveland shale form- 

 ing the lake-cliffs to the east. This 

 massive Cleveland shale starting 25 ft. 

 to the east of the Berea sandstone dips 

 westward toward the sandstone at an 

 angle which will cause the base of the 

 Berea to be less than 10 ft. below the 

 surface of the lake at the point where it dips under the water. 

 The Cle\ eland and Berea are within a few feet of each other 

 when the Cleveland dips beneath the lake under the Berea. No 



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