28 NEW YORK STATE MUSEUM 



Dip of the Paleozoic formations 



As the Paleozoic rocks were originally laid down nearly hor- 

 izontally movements since their deposition have caused them to have 

 a general south westward dip. The amount of the dip is usually 

 small and may be clearly demonstrated by comparing the altitude 

 of given horizons within the Trenton at different places. 



At Trenton Falls the top of the Trenton limestone is iioo feet 

 above sea level, while the same horizon was struck at 142 feet below 

 sea level in the Globe Woolen Mill well at Utica. Thus the differ- 

 ence in elevation of the same horizon between these points 1 4 miles 

 apart is 1242 feet, showing a southward dip of 90 feet per mile. 



Again, the top of the Trenton i mile south of Alder Creek sta- 

 tion is at 1280 feet, while the same horizon in the Rome well is 205 

 feet below sea level. The difference in elevation is 1485 feet and 

 the distance is 18 miles, which shows a dip of 82 feet per mile for 

 the limestone. 



At Grant, lower Trenton is exposed at 1200 feet, while at Graves- 

 ville 5 miles to the southwest the same beds lie at 900 feet, thus 

 giving a dip of 60 feet per mile. 



The difference in elevation between the top of the Trenton at 

 Bardwell Mill and Remsen, which places are 4^ miles apart is ap- 

 proximately 40 feet, thus giving a dip of 9 feet per mile. 



Over the western part of the town of Remsen the strata must lie 

 almost horizontal as shown by the outcrop of the upper Trenton 

 over such an area at practically the same elevation. 



Uppermost Trenton beds are shown at Remsen and also at a 

 point ij miles northeast of Steuben valley. The distance between 

 these points is 2 J miles and the difference in elevation is about 250 

 feet, so that here the southwestward dip is about 100 feet per mile. 



Certain marked variations from this general southwestward dip 

 due to the development of the Trenton fault and fold have already 

 been described. 



Joints 



The Precambric rocks are everywhere highly jointed and the 

 joint planes are always vertical or at high angles. After many ob- 

 servations the writer has not been able to make out any well 

 defined system. Even over short distances the directions are very 

 variable. Locally, however, two well developed joints may gen- 

 erally be seen crossing each other at rather high angles. Besides 

 these other minor and irregular joints are present. 



The Paleozoic rocks, too, are thoroughly jointed and, as in the 

 ■case of the Precambric rocks, these joints are mostly nearly verti- 



