1884.] 43 [Shaler. 



the turnpike that leads to Lake George — this point demands 

 a more careful study than I have been able to give to it. 



If, with the result of the study of the Chesterton Kame in mind, 

 we turn to the sea-shore structures of this nature we perceive 

 that they are more easily interpretable by means of the clue 

 which we have obtained in this mountain region. We readily per- 

 ceive that the presence of these Karnes in the shore district of 

 New England is explained by the fact that the subglacial 

 streams would certainly find their way to the sea along this 

 ice front. The general limitation of the Karnes to the shore-belt 

 which was below the level of the post glacial submergence is 

 explainable from the fact that it requires the submergence of the 

 exits of the under ice streams to give the conditions for the 

 formation of Kame ridges. When these discharge points of the 

 subglacial streams are above the drainage, the materials thrown 

 out have a much more irregular distribution, they are more 

 scattered, they would generally take on the form of low detrital 

 cones composed of only the coarser part of the glacial waste. 



There is further confirmation of this hypothesis in the fact that 

 Karnes are generally, if not usually surrounded by terrace drift 

 which is unquestionably the result of water action as before men- 

 tioned. I have never found distinct Kame deposits entirely apart 

 from areas of terrace drift. It should be said, however, that these 

 opinions require a careful reviewing in the light of studies made 

 in a great variety of positions before they can be deemed to be 

 fully proven. 



In connection with my study of shore Karnes I have been 

 led to certain important inferences concerning the rate of eleva- 

 tion of our shores at the close of the glacial submergence. In the 

 first place I must note the fact that the glacial submergence along 

 the southern New England coast was much greater than is com- 

 monly assumed. Very distinct cross-bedded sands in extensive 

 sheets occur at points as much as one hundred and seventy feet 

 above high tide in positions where owing to the contour of the 

 ground one cannot believe that they were formed in any inclosed 

 basin of fresh water. As it is not my present object to discuss 

 this question, I will only note the fact that such a deposit occurs at 

 Randolph station on the Old Colony Railway about ninety miles 

 north of Acton at a height of 190 to 200 feet. They are also 



