452 NEW YORK STATE MUSEUM 



odor, resembling more that of Pennsylvania gas. It burned with 

 a much redder flame and deposited carbon or lampblack more 

 abundantly. In fact, it seemed particularly rich in this last- 

 substance. 



In my visit to the well in 1897, it was impossible to verify all 

 these observations. The odor of the gas did not seem to differ in 

 a marked way from that of Pulaski gas, and certainly did not 

 suggest Pennsylvania gas. The redder flame of its burning was, 

 however, recognizable, and with this fact the greater deposition of 

 carbon could readily be seen to agree. It was not found practi- 

 cable to attach a pressure gage, but the testimony as to the fact 

 of the original figure was direct, and there seemed no reason to 

 call it in question. 



After the well had been drilled to its full depth, a small tor- 

 pedo was exploded in it. It seems that the explosive was 

 lowered a little deeper than it was intended, so that it took effect 

 on the upper part of the granite as well as on the sand rock. 

 The gas flow was somewhat increased and many fragments were 

 broken from the granite. A quantity of granite chips was left 

 lying on the ground where the sand pump was last emptied. 



This discovery is one of the most interesting that has recently 

 been recorded in the history of the petroliferous series and has 

 an important bearing on the questions pertaining to the origin 

 of the same. 



Here is a considerable volume of gas lying but a few feet 

 above the granite. It must have originated where we find it, 

 for gas can not descend in the geologic scale. The law of 

 gravitation forbids. Neither can it rise in the scale, for the 

 shaly beds that form the roof of the gas rock are impervious. If 

 they had not been the gas with its pressure of 340 pounds to the 

 square inch, which is the same as 48,960 to the square foot, would 

 certainly have risen to some higher level. 



There is no indication of temperature above the normal in 

 connection with its formation. A temperature of even 200° F., 

 acting on this series of rocks, with the alkaline liquids with 

 which they are here and there charged, would inevitably have 

 worked important changes in the rocks themselves. 



Silica is dissolved under such conditions and must have been 

 reprecipitated in the rock series. Such quartzitic sheets would 



