GILANCIUANE, SIMONDNUES JIN GHUSISINULAUNIO, ~ WALT 
The Krakokta Glaciery.—Of the glaciers that descend north- 
erly from Redcliff Peninsula, the Krakokta is the most impor- 
tant and instructive. It takes its rise in the north central portion 
of the nevé field of the plateau and descends a relatively long 
valley by a series of moderate cascades, rather than the single 
one which characterizes the descent of the glaciers previously 
described. The last of these cascades lies opposite the head of 
Bowdoin Bay, at the point where the plateau gives place to the 
lowland that connects it with the mainland. On descending 
this, the glacier spreads out upon the lowland into a broad, flaring 
foot, the right-hand portion of which immediately overlooks the 
head of the bay, while the central portion is forced into direct 
contact and conflict with the Tuktoo glacier which descends into 
the same lowland from the main ice-cap on the north, and the 
left-hand side spreads out upon the flats toward the head of 
McCormick Bay. In descending this lower cascade the ice is 
much broken and presents a very ragged aspect, but I did not 
observe that it differs in any notable way from the analogous 
ice cascades of southern glaciers. 
The collision of the Krakokta and the Tuktoo glaciers, 
gives rise to a very interesting joint moraine. The Krakokta 
glacier coming from the south carries chiefly red sandstone in 
its basal layers. The Tuktoo glacier coming from the north 
carries chiefly gray crystalline rock. This contrasted material 
has been heaped up into a single sharp ridge, the south side of 
which is red from the dominance of the sandstone, while the 
north side is gray from the dominance of the crystalline rock. 
The contribution of each glacier is thus strikingly displayed. 
The dividing line between these contributions runs essentially 
along the crest of the moraine. Each glacier seems to have 
done an equable share of the work of forming the moraine. It 
should be said, however, that I only examined the eastern part of 
833 
