224 H. L. FAIECIITLD POST-GLACIAL TPLIFT OF X. E. AMERICA 



As tlie isobases record, negatively, tlie post-Glacial submergence, tbe}' 

 should have some suggestive relation to the glacial load, and tlie disposi- 

 tion of the ice over Nova Scotia is important. The glacial features have 

 been well described by (.*halmers (8). lie postulates several ice centers, 

 or independent bodies on tlie higher tracts, with at least the later flow 

 controlled by the large topography, and all toward the sea and larger 

 bays. He attributed many inscriptions to icebergs, which ma}' l)e true 

 (8, pages 95-97). He seems to have minimized the ice-flow of the conti- 

 nental sheet southeastward across the Chignecto Isthmus (8, pages 93- 

 95), for an area of drumlins in the Amherst region indicates a consider- 

 able current of ice from New Brunswick. This flowage probably deployed 

 some distance over the peninsula; but Chalmers was j^i'obably correct in 

 his view that the ice-sheet did not cross the Bay of Fundy, and that the 

 flow in the southern peninsula was radial from the interior. 



Chalmers found no evidence of glaciation on the Magdalen Islands nor 

 on the northern part of Prince Edward Island. He says, page 91 : 



"The Magdalen Islands are non-glaciated, and it would seem that the main- 

 land ice has gone no farther than the eastern and northeastern border of 

 Prince Kdward Island, the southeastern part having, apparently, been glaci- 

 ated by the ice which accumulated on the island itself." 



Chalmers gives in this report a tabulation of the marine beaches (pages 

 21-25), and while his figures are not always consistent among themselves 

 and are partly of inferior features, they are in general decidedly con- 

 firmatory of the isobases as drawn for Nova Scotia, and some are in 

 close or precise agreement. The 100-foot isobase has been laid in accord- 

 ance with Chalmers' levels for the Magdalen Islands, 110 to 115 feet. 

 But the map does not agree with his figures for Prince Edward Island, 

 which, are all 75 feet except one station for 80 and one for 95 feet. Per- 

 haps his 75-foot shore correlates with the strong beach in the Gaspe 

 district at 85 feet and represents a relative pause in the later uplift. 

 TyrrelFs Newfoundland terrace at 100 feet may represent the same pause 

 (see later reference to this). 



The local glaciation of the Nova Scotia region helps to explain the lack 

 of deep submergence. The piling of immense quantities of hugh granite 

 l)locks along the coastal area, at least from Liverpool to Barrington 

 Passage (Cape Sa])le), might, at first thought, suggest that the ice-body 

 was sufficient to depress the land to an extent inconsistent with the evi- 

 dence : but the drift is piled in practically block moraine along the land 

 border (plate 17). The ice did not have sufiScient depth and push to 

 sweep the drift into the sea. As stated above, only a tongue of the Labra- 



