PLEISTOCENE MARINE SUBMERGENCE 45 



tures on the east side of the Champlain valley, as they lie far 

 east in Vermont (92). 



At Port Henry is a narrow embayment or recess in the west wall 

 of the Champlain valley which holds some excellent but puzzling 

 records of standing waters. West and northwest of the village 

 good delta terraces occur, related to Alill brook. The fair ground 

 is on a plain at 600 feet, with wave erosion at the road corners. 

 The cemetery is on another plain, the higher terrace being 640 to 

 650 feet. These levels are seen both sides oi the creek valley. 

 North of the fair ground on the east-facing slope are ridges and 

 shelves that appear wave-shaped at 640 to 660 feet. 



Southwest of the village, by McKenzie brook, a good series of 

 bars occur on both the north and south roads. On the north road 

 the topmost bar is under the house of A. M. Edwards, at 620 

 feet by the map. Four other close-set ridges carry down to about 

 550 feet, with terracing on the delta to 530 feet. On the south 

 road the upper bar carries two houses at about 630 feet, with 

 moraine beyond (above) it. In the field toward the brook good 

 bars occur at 605 down to 560 feet; and terraces to 500 feet. 



The reason for the above detail is the fact that these features 

 lie much above the theoretic marine plane, which is here about 

 570 or 575 feet. The lower of the gravel bars falls within the 

 marine level, but the highest is 60 feet too high. The topography 

 of the valley wall and the small width of the embayment do not 

 favor the existence of glacial waters with wave-efficiency to pro- 

 duce the bars; and the vertical succession of the bars through 70 

 feet rules out any definite outlet or fixed control. The series of 

 close-set, well-developed bars is similar to those positively due to 

 slow rise of the land out of water; and none of several explana- 

 tions in appeal to nonmarine origin are satisfactory. It seems 

 more likely that in this region, the east flank of the Adirondack 

 mass, there has been an excessive uplift of 60 feet, with or with- 

 out Postglacial faulting. The superior height of the Crown Point 

 terraces, coupled with high features in the Peru region, to be noted 

 later, lend force to this view. In such case our theoretic or datum 

 plane does not represent quite the total rise in the Champlain 

 region. The profile, plate 10, is drawn to connect with the summit 

 shore at Covey hill. 



About Westport are conspicuous lower plains, but the summit 

 features have not been sought. 



The estuary waters penetrated far inland up the valley of Bou- 

 quet river, which has a bend on this sheet, and the primary or full- 



I 



