ANCIENT WATER LEVELS OP CHAMPLAIN-HUDSON VALLEYS 195 



plain valley I have been unable to find along this plane north 

 of the Street Road locality traces of shore lines in exposed situa- 

 tions where an open lake would leave traces. It seems to me 

 therefore not demonstrable at present that the actual ice front 

 had retreated very far north in the Champlain valley at this 

 stage but that more likely there were glacial lakes of the Mar- 

 jaelen See type though probably larger than this example occur- 

 ring here and there along the ice margin at approximately the 

 same level and draining fromi one to another southward. 



This plane if followed northward will be found to graze the 

 northern half of the Batten kill delta, which appears to have 

 been built later than the southern half; it falls on a 580-foot 

 beachlike deposit in the southern part of the Port Henry quad- 

 rangle, and on a lake ( ?) terrace at 600 feet at Elizabethtown on 

 the quadrangle of that name, on the upper Bouquet river, a tribu- 

 tary of Lake Champlain; it touches a high terrace deposit also on 

 the Bouquet river branch in Lewis on the Ausable Forks quad- 

 rangle 2 miles north of Towers Forge at an elevation of 620 feet. 

 On Black brook (Ausable Forks quadrangle), there are broad 

 stream plains between 660 and 680 feet in elevation west of 

 Clintonville ; also plains at 700 feet at Clintonville : all in this 

 tilted plane. This plane also strikes the Saranac river at an 

 elevation between 720 and 740 feet. Cadj^ville station is 732 feet; 

 just east and slightly lower (729 feet Baldwin) is a large delta 

 probably of this series. The plane would meet the international 

 boundary between 820 and 840 feet. Just west of the Mooers 

 quadrangle is a beachlike ridge indicating some kind of water 

 action at this level, approximately that of the upper lakelet at 

 the Gulf. 



The Cadyville delta is associated with kames ; the (Street Road 

 terrace was clearly built between walls of ice on one side and 

 of rock on the other. Both deposits are below the level of the 

 Tipper part of the great spillways on the Mooers quadrangle. If 

 the land stood during these stages at anything like the attitude 

 assumed during the ensuing marine invasion, these glacial de- 

 posits may be considered as nearly contemporaneous, thus carry- 

 ing the ice down to the vicinity of Ticonderoga. 



All that can be at present stated with confidence concerning 

 Lake Vermont during the discharge at the Quakers Spring outlet 

 is that the ice appears to have been retreating and shrinking in 



