170 NEW YORK STATE MUSEUM 
above Schenectady, unless it contained an unmelted remnant of the 
glacier. (See Schenectady quadrangle. ) 
The overthickened ice extended to the Catskills and, in the 
Hudson valley, probably some distance southward along their 
eastern base, though south of Cairo Roundtop no effort was made 
to trace it. An extensive area of drift, originally deposited over 
thin stagnant ice, north of Broome Center (Gilboa quadrangle) 
on the divide between Schoharie and Catskill Creek drainage, 
at an elevation of from 1,960 to 2,050 feet, appears to have been 
outside its influence, but otherwise the entire basin of the latter 
stream was covered by it. The deposits along the creek between 
Cairo and Leeds, first described by Davis't as a dissected delta 
built in the Hudson estuary (Coxsackie quadrangle) are quite 
typical of the very insignificant accumulations of recessional drift 
found here and there over the drumlinized area and associated 
with the melting out of the last remnants of the ice which first 
molded and then stagnated above that area. 
Inasmuch as the field of stagnant ice surrounding the Adirondacks 
has not been traced further south at the higher levels, it will be con- 
venient at this point to begin at the New Jersey line and indicate 
the more important features connected with the shrinking of the 
motionless glacier on the west side of the Hudson valley from south 
to north. 
The Wallkill basin heads in New Jersey with a low point in the 
divide north of Augusta (Franklin Furnace quadrangle) where an 
area of till partly covered ‘by stratified sands separates the head- 
waters of Papakating creek from those of the southward draining 
Paulin’s Kill at a present elevation of 500 feet. The divide is here 
uncut and has never been the outlet of a lake ponded in the basin. 
Yet until a retreating ice front had uncovered a lower outlet some 
thirty-six miles to the northeast, this must have been the site of an 
ever lengthening body of water under the hypothesis of the gradual 
melting back of a live glacier. It will be sufficient here to state that 
the Wallkill basin was practically obliterated by a filling of stagnant 
ice until superglacial streams had carved out drainage lines north 
of Goshen. The evidences of this stagnant mass are alike both north 
and south of the State line and have been described in detail by 
Salisbury in the Glacial Geology of New Jersey. We will return 
to a consideration of the drainage (page 172) after gathering up 
certain details of importance. 
"Proc. Boston Soc. Nat. Hist. v. xxv (1892) p. 318-35. 
