440 



Repoet of the Sta te Geologist. 



Such local foldings are by no means .uncommon. The southeast dip, in the 

 region southeast of Shawangunk hill, changes to a, low western one in Mini- 

 sink and Wawayanda townships, where the slates overlie the Cambrian 

 limestones. The sandstone beds have disappeared, and the formation is rep- 

 resented by hard, black slates, with a pronounced cleavage. South of Denton, 

 the slates give rise to many steep ridges. 



From the AVallkill river southeast to Belgrave mountain, there is only a 

 narrow, wedge-shaped area of slate, which begins west of Sugar Loaf moun- 

 tain, and extends south as far as Warwick. It rests unconformably on the 

 Cambrian limestones, and, while the bedding is often obscured by the marked 

 cleavage, it st ems, in general, to be dipping to the west. Glenmere lake lies 

 just within this slate area. 



North of Goshen the sandstone members again appear, and are occasion- 

 ally fossiliferous. A mile and one-half northeast of Goshen, and just after 

 crossing the railroad, the slaty members are prominent, striking N. 60° E., 

 with a dip of 20° W. The dip is very variable, however, and about 500 feet 

 farther north it changes to 70° W. The layers here become more siliceous. 



A little beyond locality 461, at 472, the sandstone layers have a low 

 western dip, and contain abundant remains of Orthis test/udina/ria and 

 crinoid stems. 



Southwest of Neelytown (464), the slate dips 40° N. W., while north- 

 east of it (478), the dip is northeast. In general, the slate dips away from 

 the limestone area at Neelytown. 



At the north end of the iron bridge across the Wallkill river, at Mont- 

 gomery, and in the river bed, are abundant ledges of slate, with occasional 

 sandstone layers. They here strike east and west and dip 35° N. To the 

 southwest of Montgomery, however, the strike is generally northeast, with a 

 western dip. 



An examination of these and the other strikes and dips plotted on the 

 map of this region, indicates that there must be numerous and probably 

 gentle flexures. 



The Wallkil] river at Walden flows over a ledge of slate and sandstone 

 tw enty-six feet high, and then through a gorge sixty feet deep, affording line 

 exposures of the westwardly dipping shales and sandstones. 



Southeast and east of Goshen, the Hudson river slates extend to the 

 range of gneissic knobs northwest of Skunnemunk mountain, where they 

 rest unconformably on the gneiss. Their relations have been mentioned in 

 another pan of this report. 



