THE MINERAL SPRINGS OF SARATOGA II 



Gravel i8' 2" 



Amsterdam limestone 16' 



Little Falls dolomite 283' 



Total 31/ 2" 



The Hathorn drilled well penetrated to a depth of 1006 feet, of 

 which the last few feet are reported as Potsdam. This rock is so 

 easy to identify that there can be little question that the drill stopped 

 in it, but the determination of the other members needs revision, 

 and the cores are unfortunately no longer available. The depth 

 of the well shows so much in excess of the general section as given 

 above that there may be repetition from faulting. 



The farther east wells are drilled at Saratoga Springs from the 

 line of Spring street, the thicker the slate will be found. At Doctor 

 Strong's sanatorium after 86 feet of gravel, nearly 300 feet of slate 

 are reported before the limestone was met. 



The drilled wells of the gas companies and the holes for mineral 

 water at the Geysers, two miles south of Saratoga Springs, begin 

 in the Canajoharie (Hudson River) slates. They find the waters, 

 however, in the underlying limestones. The holes run between 300 

 and 400 feet deep at the General Carbonic Company's wells. The 

 farther south one goes, the greater is the thickness of slate. Thus, 

 at Ballston, it is 600 or 700 feet and at Round Lake between 1300 

 and 1400 feet. 



To the north of Saratoga the Gurn spring apparently emerges 

 from the Little Falls dolomite. The vent is some feet below the 

 capping of gravel and is no longer visible, but the nearest outcrops 

 are all of the dolomite. 



Of the geological history of the district from the close of the 

 time marked by the formation of the slates — that is, from the later 

 Ordovicic period — we have but scant records, as will be set forth 

 in the report of Professor Gushing and Doctor Ruedemann. 

 Whether other sediments once covered the slates and were then 

 removed by erosion is doubtful. The lack of sediments suggests 

 land conditions at least for the greater part of the time. The strata 

 shared in the mountainous uplifts to some extent, but near the 

 springs the dips are still very flat and notable folds are not 

 immediately concerned with them. Important faulting has taken 

 ])lace and one fault in particular, as will next be descrilicd, 

 has an intimate relationship to the springs. The dips next tlio 



