NEWARK ROCKS OF ROCKLAND COUNTY, N. Y. 47 



ently toward the older rocks, but these beds do not belong to the 

 same horizon as the Suffern exposures. Southwest of Ladentown 

 (fig. 9, c,) the conglomerates dip away from the older rocks. 



For several miles northeast of Ladentown, the exact location 

 of the contact and fault is rendered uncertain by high hills 

 of glacial drift which not only conceal all rock exposures, but also 

 obscure the rock topography. It apparently swings more to the 

 east, passing near Camp hill and just east of the village of Thiells. 

 Its position can be exactly located in the bed of Cedar Pond brook 

 near the Stonypoint waterworks, where nearly horizontal cal- 

 careous conglomerates belonging to the Newark series are ex- 

 posed within 10 or 15 feet of the paleozoic limestone. The contact 

 is apparently a vertical one, the conglomerates abutting against 

 the older rocks, though the actual contact is not shown. A few 

 feet down stream the conglomerates have a distinctly marked 

 westward dip, i. e. toward the older rocks. It is difficult to believe 

 that the Newark beds rest undisturbed on the limestone. The 

 more natural conclusion from the relations there exposed is that 

 they have been faulted against it. A black, crumpled shale out- 

 crops a few feet upstream from the limestone exposure, which is 

 very narrow, and for a mile or more southward a belt of shale at 

 least a quarter of a mile in width lies between the crystallines on 

 the west and the Newark conglomerates on the east. 



The conglomerates here adjoining the older rocks belong to a 

 horizon undoubtedly many hundred feet below those exposed 

 south of Ladentown, and still farther below those near Suffern. 

 In fact I believe they are nearer to the base of the entire forma- 

 tion than to the top. . The fact that beds belonging to such widely 

 different horizons adjoin the older rocks is the strongest proof 

 that faulting has occurred along this border. 



Another indication of faulting is found in the composition of 

 the sedimentary beds along the border as compared with the older 

 adjoining ro^ks. I have already pointed out the absence of 

 granite or gneiss pebbles in the conglomerate, the two constitu- 

 ents most to be expected, if the conglomerates had been formed in 

 their present position relative to the older rocks. The presence 



