388 DABTON GREEN POND, N. J., TO SIvUNNEMUNK MT., N. Y. 



ways clear. The anticlinal which comes in from the south brings up the 

 Oriskan}^, Helderberg and Longwood members at Milton, and the Green 

 Pond conglomerate in the central part of Bowling Green mountain. 

 The dips on the northern end of this mountain are semi-quaquaversal to 

 the east, north and northeast, but southwest of Milton there is a svnclinal 

 with steep axial pitch to the north. 



The principal anticlinal in New York is along the eastern side of 

 Skunnemunk mountain, where the flags dip eastward down the slope of 

 the mountain, but with a strong pitch to the north. This flexure 

 apparently merges into a slight overturn of the eastern limb of the 

 synclinal in the northeastern end of the mountain and about Cornwall 

 Station. 



The principal anticlinal southward is first apparent on the west side of 

 the south end of Greenwood lake, Avhere its relations are shown in section 

 VII, plate 17. It brings up the Oriskany quartzite in a small, steep ridge, 

 which continues for about a mile. The small synclinal to the eastward 

 carries lower beds of Monroe shales, but they rise on the pitch, southward, 

 and finally constitute the summit of the ridge to its southern termina- 

 tion. In this vicinity the anticlinal of Oriskany is exposed in the west- 

 ern slope of the ridge and along a small depression below. On the east 

 side of the southern end of the ridge the pitch brings up the Oriskany 

 quartzite, Helderberg limestone, Longwood red shales, and Green Pond 

 quartzite in succession to the southward. The three first dip to the 

 northwest, but the quartzite dips to the east, apparently from a small 

 fault. 



South from Greenwood lake there are two valleys, one extending along 

 the Cambrian limestone belt and the other along the Monroe shales, with 

 Kanouse mountain intervening. For some distance the structure is a 

 west-dipping monoclinal, so far as I could find, but in the western valley, 

 about half way to Newfoundland, it bears a low anticline. This flexure is 

 Avell exhibited in the extensive exposures of Monroe shales at the small 

 settlement of Postville, although its distinctness is somewhat obscured 

 by the strong slaty cleavage by which the shales are traversed. The 

 axis of the anticlinal rises to the southward, and at Newfoundland a 

 sudden increase of pitch brings up Oriskany, Helderberg, Longwood, 

 Green Pond and Archean rocks in rapid succession. This pitch of the 

 beds is finely exhibited just west of Newfoundland, Avhere the Green 

 Pond quartzite and conglomerate rise into the northern end of a spur of 

 Green Pond mountain. The dips are semi-quaquaversal and the beds 

 exposed incline to the west, north, and east around the end of the 

 mountain. A short distance south the crystalline rocks are brought up 



