No. 1.] CHALMERS GLACIAL PHENOMENA. 51 



side and along the banks of the rivers where they intersect it, 

 have also chan":ed its outw.ird form in no small decree. The 

 best section of these beds is exposed at Blick Point near Dickie's 

 lun. In the railway cutting at this place the three members of 

 the modified drift occur in superposition. Here and at the shore 

 their thickness in descending order is seen to be as follows : — 



Stratified sand (Saxicava) passing into sur- 

 face gravel 10 feet '•' 



Stratified marine clay holding fossils (Leda) 5 to 10 " 

 Sand and gravel beds or kame 50 feet or more. 



These kame deposits have not been obi-erved in conact with 

 the ''till " ; but between New Mills and Black Point tiey rest on 

 glaciated rock-surfaces. 



I have already referred to the theory of the origin of kames, 

 which supposes them to be due to the efibct of oceanic currents, 

 S)rting out and redistributing the "till" and morainic debris 

 thrown down by glaciers, and liave stated that this theory will not 

 suflBce to explain the formation of the kame deposits in question. 

 In straits and along the Atlantic border where the coast is 

 exposed to the sweep of the arctic and other currents these 

 agencies have no doubt had powerful influence in modifying the 

 older drift deposits when the land stood at a lower level. But 

 the position of the Bay Ch ileur region, with a highland area to 

 the west and south-west, forbids the supposition that currents 

 from the riorth-east traversed it. Althouirh we have no data to 

 show what the hei$:;ht of the land was duriiiii; tlie formation of 

 these sand and gravel beds; yet in the period subsecjuent, 

 namely, that of the deposition of the stratified marine clays 

 (Leda clay), which in this district h.ive not been observed ..t a 

 greater height than 100 to 15') feet above the sea. we find that 

 a subsidence of 400 to 450 feet below the present level would bo 

 sufiicicnt to account for the presence of its marine fauna, that ig, 

 allowing the bathymetrical r mge of the species found fossil here 

 was the same as that of similar species existing in the Gulf 

 of St. Lawrence at the present day. Hence, it is quite probable 

 this region was not further submer<j;ed durinic the Post-Pliocene 

 epoch. A sinking of the land to the depth of 450 to 500 feet, 

 however, would not admit of currents flowing u,> tiie Kesti- 

 gouche valley, nor .over the area in the nort i-uest of the 

 Province ; nor does it seem possible that local marine currents 

 'which might have circulated within the Bay during Pose Pliocene 



