22 NEW YORK STATE MUSEUM 



thickness of approximately 600 feet in the southern part of the 

 Little Falls district is given by Gushing. The record of the Camp- 

 bell well near Utica shows 710 feet of the shale there. The deep 

 well at Rome shows a thickness of only 300 feet of shale. Thus 

 there seems to be a notable thinning of the Utica shale in passing 

 northwestward . 



Lorraine beds. The Lorraine beds of the Hudson River group 

 appear at only one place within the map limits, namely at the top 

 of Starr hill. The beds there show a thickness of about 200 feet 

 with the top not reached. As is usually the case in central New 

 York these lower beds appear to be destitute of fossils. Penn 

 mountain and other high hills just west of the Remsen quadrangle 

 are capped by the same formation. 



There is no sharp line of demarcation between the Utica and 

 the Lorraine and thus an exact boundry line can not be drawn. 

 Passing upward the Utica black shales give way to generally lighter 

 colored, rather more sandy shales containing frequent thin beds 

 of gray sandstone. At times, however, the Lorraine shales closely 

 resemble the Utica shales. Good exposures may be seen on the 

 western side of Starr hill and also near the top of Penn mountain 

 at about the 1700 foot level. 



STRUCTURAL FEATURES 

 Folds 



The Paleozoic formations show a very perceptible southwest- 

 erly dip but it is by no means uniform. *For instance to the north 

 of Remsen and in the vicinity of Honnedaga the limestone beds 

 show very little departure from horizontality, while to the north 

 of Steuben Valley they show a dip of approximately 100 feet per 

 mile to the south westward. Again in the bed of Mill creek, about 

 a mile above Gravesville, the limestones show a very sharp dip 

 of 15° to the southwest. In other cases the southwestward dip 

 is just enough to be noticeable in the outcrops. Thus we see that 

 strata which in a given locality He almost horizontal may within 

 a short distance show a comparatively steep dip giving rise to low 

 folds whose axes extend northwest and southeast. 



Another set of folds whose axes extend northeast and southwest 

 are also more or less clearly distinguishable. Such are the folds 

 accompanying the Trenton fault and fold (below described). A 

 low anticlinal fold with similar strike has been observed to the 

 northeast of Steuben Valley where along one stream the limestone 



