M ^^^ YORK STATE MUSEtJM 



that were built in the marine waters that occupied the valley as 

 the ice gave way. This water plane rises from zero in the vicin- 

 ity of New York to at least 350 feet at Schenectady, or at the 

 rate of 2.2 feet a mile. 



The practical continuity and correspondence in level of the 

 highest water plane on both sides of the Hudson-Champlain val- 

 ley proves that the waters hlled the entire breadth of the valley 

 and that the shore phenomena are not the product of ice-border 

 lakes. It also appears that the waters were not held up by any 

 moraine dam or any barrier of land uplift. 



Over the Fort Edward divide the waters Avere more than 300 

 feet deep, and all the phenomena in the Fort Edward-Schuyler- 

 viile district are those of static waters, slowly lowering and ter- 

 racing the copious detrital deposits on both sides of the valley. 

 There is found no evidence of any glacial stream flow below the 

 summit w^ater plane. 



As the ice front melted back the ocean followed it and flooded 

 the valley. The Avaters v.^ere at first the Hudson inlet; later the 

 Hudson-Champlain inlet ; and finally the Hudson-Champlain strait. 



The minimum amount of continental uplift on the Canadian 

 boundary is approximately determined by the deformation of the 

 Iroquois plane. In the former report (page 32) it was shown 

 that if we assume the Covey gulf outlet of Lake Iroquois to 

 have been no lower than the original Rome outlet, then the dis- 

 trict must have been lifted at least 665 feet. This makes the 

 Covey hill bars 140 feet below the marine summit. The total 

 uplift must have been as much more than 665 feet as the gulf 

 outlet was beneath the plane of the Rome outlet. The study of 

 the high-level shore phenomena leads to the confident belief that 

 the Covey hill district has been uplifted at least 750 feet since 

 the ocean waters displaced the ice sheet. This would carry the 

 gulf channel only 85 feet beneath the Rome outlet. 



Summary. Heavy and conspicuous static water phenomena 

 occur with practical continuity on both sides of the Hudson- 

 Champlain valley from New York City to Canada, rising steadily 

 from zero at New^ York to 750 feet at the north edge of the State. 

 Above this plane the land is cut by glacial drainage. All the 

 facts now knowm and the relationship of the beaches to the to- 

 pography of the valley walls indicate that the waters were con- 

 fluent with the ocean. The absence of marine fossils in the 



