GLACIAL Gl-:OLOGV OF NORril GREENLAND 807 



\'isil)lc stream of any size issues from beneath a glacier at its 

 end. That water realh' issues from the end of the glacier and 

 flows on beyond can hardly be doubted, but in general it escapes 

 beneath or through debris, rather than over it. In some cases, 

 indeed, in crossing the embankment sloj)e in front of the end of 

 a glacier the motion of the water in the drift beneath one's feet 

 can be heard. 



As before noted, the sides of a glacier rarely rest against the 

 vallcN" in which the ice-stream lies, and in the ororof-e between the 

 ice on the one side, and the valley wall on the other, there is 

 usually a stream. These lateral streams are tolerably constant 

 accompaniments of the glaciers, as Chamberlin has already 

 pointed out. 



Surface ablation does not give rise to many considerable 

 streams on the surface of the ice. The surface is usually so 

 crevassed that the water plunges beneath it soon after its forma- 

 tion, and the stream which continues for more than a few rods on 

 the surface is the exception rather than the rule. Cases were 

 however seen where superficial streams were continuous for some 

 miles. The longest seen was on the surface of the largest gla- 

 cier on the north side of Herbert Island. Here, in the summer 

 of 1895, a stream was essentially continuous from the head of 

 the differentiated portion of the glacier to a point near its 

 terminus. 



Englacial drainage does not show itself so long as the drain- 

 age is englacial, but the fact of englacial drainage was shown at 

 several points. The most conspicuous example seen is shown 

 in the accompanying figure, which represents the end of a large 

 glacier on the south side of Olriks Bay. Here, as will be seen, 

 a huge spout of water issued from about the middle of the 

 vertical face at the end of the glacier. The diameter of the 

 stream as it issued from the ice was about five feet, Issuing 

 approximately horizontally, it showed that there was an englacial 

 stream of similar proportions behind it. In such a case there is 

 of course no means of knowing the length of the englacial 

 stream, or how nearly it maintains its horizontal position. The 



