228 The American Geologist. October, 1903. 
Ten miles farther north, at Glens Falls, I found another 
delta plain of the same character and origin, extending two 
miles northward from the Hudson river, at the estimated hight 
of 400 to 410 feet above the sea. Thence northward, on the 
railroad route to lake George, a most notable series of eskers, 
20 to 50 feet high above their hollows, reaches five or six miles,, 
inclosing Glen lake, 402 feet above the sea, and forming the 
divide crossed by this railroad, at the altitude of 575 feet. The 
gravel of the eskers has in many places plentiful stones, well 
rounded by water-wearing, as large as one and a half to two 
feet in diameter. All these extensive modified drift deposits, 
like those of Saratoga Springs, were doubtless brought by con- 
fluent drainage to a re-entrant angle of the retreating ice 
border. 
Next to the north, around Caldwell, at the south end of 
lake George, and along the entire extent of this beautiful lake,. 
323 feet above the sea, 30 miles long, and from a half mile to 
two miles wide, gemmed with many small islands and inclosed 
on each side by great mountains, the drift consists almost whol- 
ly of till, and I saw no important delta accumulations, either ■ 
at the old level of the lake Hudson-Champlain or on the present 
lake shore. The lowest pass on the divide of lake George and 
the Hudson is between French and Sugar Loaf mountains, as 
shown by the Glens Falls map sheet of the U. S. Geological 
Survey, and has an altitude of 349 feet above the sea, or only 
26 feet above the lake. Through this pass the water of the lake 
Hudson-Champlain extended with a depth of about 75 feet, 
and its depth above lake George was about 100 to 150 feet, in- 
creasing from south to north. 
Till also constitutes the principal part of the drift north- 
ward along the mountainous west side of lake Champlain, with 
no conspicuous delta accumulations of modified drift nor later 
stream deposits, for the distance of nearly fifty miles to the 
Au Sable river. Neither there nor on lake George can any 
shores of the old glacial lakes, or of the sea later and lower, be 
traced without systematic search with leveling. 
Delta plains were also accumulated in the glacial lake of the 
Hudson valley after the land had been somewhat uplifted, these 
being mainly supplied by stream erosion of earlier large deltas, 
which then, on account of the progressing elevation, stood ioo> 
