GLACIAL STUDIES IN GREENLAND. 785 



gradually broadens until it is wider than the Blase valley itself. 

 At a distance of about three miles, a tongue of ice, very much 

 more massive than either of the preceding, descends from the ice 

 cap through a broader and deeper incision of the plateau face, 

 and stretches entirely across the broad terrace just mentioned, 

 and descends its face almost to the bottom of Blase Dale. At 

 the point where it emerges from the cliffs of the upper plateau it 

 develops strong lateral moraines which extend entirely across 

 the high terrace, and even down its edge into the axis of the 

 Blase valley. The outer lateral moraine on the right, bears evi- 

 dence of greater age than the terminal moraines of the two gla- 

 ciers already described. It is notably weathered and covered 

 with vegetation in the partial fashion of the region. There is 

 nothing to indicate age beyond a few hundred years, but it is 

 notably older than the exceedingly fresh moraines we have 

 already encountered, as it is also notably more ancient than the 

 fresh lateral moraine that lies within it. Its material is very 

 rocky and angular. Between it and the edge of the ice there is 

 a more complex moraine consisting of several parallel ridges. 

 The inner edge of this is so intimately associated with the mar- 

 gin of the ice, and its material extends out upon the border of 

 the ice to such an extent as to make it difficult to determine just 

 where the one ends and the other begins. 



A very notable medial moraine is borne on the back of the 

 glacier some distance out from its southern margin, but it joins 

 the lateral moraine before reaching the terminus of the glacier. 

 The crevasses of this glacier are more notable than those of the 

 preceding, and besides the true crevasses, there are numerous 

 fracture lines traversing some portions of the surface which seem 

 to be due to internal strains that do not demand the opening of 

 the crevice when once formed. They cross the laminae, or blue 

 bands, of the ice (which here run parallel to the sides) taking a 

 course obliquely forward but curving toward the center of the 

 glacier. Their course is thus seen to be the opposite of that of 

 the normal crevasses on the border of a glacier. They are obvi- 

 ously a fine subject for investigation, and I much regret that 



