J*lr!sfori III ('/nnuji's of L/'fiJ. — Dedeer. 41 
TIk' gi-;ulieiit of tlu- dcfoniUMl (>coi(l surface was cvidcntl}' 
steepest on the Atlaiitie side of the continent, whc've tlic slope of 
the ice-sheet must also havc^ lieen on-vtoi^t ; 't is here uenerally 
1: 1,400, with the exception of the St. Lawrence valley, where 
its direction is olili((ue to its general trend against the Atlantic 
and its amount is not larger than about 1: 4,000. 
The steep gradient Avill prol)ably he found also at the coast of 
Labrador, which in many respects is analogous with the high, 
fjord-cut coast of Norway in Scandinavia. In the interior of the 
American continent, where the ice spread out over a large area, 
the isobases are far more distant and show a smalU'r gradient just 
as in Scandinavia, 'i'hus the mean gradient from (Jeorgiau litiy 
towards the southwest to the limit of the area seems about 1: 
:-).400, being much sleeper :it the border of the azoic region and 
smaller at the outside. 
The connection lietween the subsidence and the geological 
structure of the earths crust is perluqjs not ((uite so striking as 
in Scandina\ia. Still it seems i)robalile that the Canadian azoic 
or Archiean region has changed its level more than tin- surround- 
ing tracts, though this is not yet sulliciently proNcd in regard to 
Hudson l)ay. The general conformity l)etweeu the ice-covering 
and the old azoic plateau makes it dillicult in the present state of 
our knowledge in many cases to discern Itetween the iuHuence of 
these two circumstances. 'J'hus it may l>e lemarked that the 
above mentioned convexity of the isobases around the Atlantic 
peninsula may .also have sonu'connection with the Atlantic moun- 
tain ranges, and that the most uplifte<l part lies near the Adiron- 
dacks, conse([uently at quite a distaiu-e west of the iee-sheil :it 
Quebec. The fact that Newfoundland, which at least during the 
last extension of the glaciei's may have lieen only locally glaciated, 
also shared in the subniei'gence may in some degree l)e aci-onnte<l 
foi' by its gi'ological structure. 
All the above stateuu-nts conceriung the late glacial n|)heava[ 
are Itased upon the hight to which the marine deposits are up- 
liftetL but as we generally cannot tell whether this rising of the 
land has been continuous or [)art ly counteracte(l by suitsidence, 
it would be more correct to speak of it as the linal result of tlie 
<'hanges of level since the maximuni of the \\\W glacial siduner- 
gence. 
Alono- cei'taiii parts of the Atlantic coast many facts were oli- 
