70 GLACIERS OF THE CANADIAN ROCKIES AND SELKIRKS. 



rather gradually toward the west and attains a height of about 70 feet, ending 

 abruptly, as steeply as the debris will stand and with no trace of any continuance 

 across the valley. This is so unusual a featiu-e for a terminal moraine that many 

 are disposed to consider the mass as a rock slide from the adjoining mountain 

 face. There are several varieties of rock represented in the heap and time did 

 not permit an examination of the adjoining face to see whether they might have 

 had such a source. The strata in the region, however, are so nearly horizontal 

 that, whether the feature is a moraine or a slide, the same rocks probably occur in 

 the adjoining mountain as farther up the valley. Standing upon the highest 

 crest, the ridge is seen to be double, the outer one somewhat convex down stream, 

 while from the western end there passes a short spur down the valley. The 

 writer is disposed to accept the view of Wilcox, who gave the name to the lake, 

 that we have here a moraine. It is, however, not of the bear-den type found 

 farther up the valley, but very much older than the most ancient of the two. 

 Its general lack of vegetation may be due to the scarcity of suitable soil, although 

 it does support a sparse growth of timber. The unusual features of the mass, 

 considered as a moraine, will be tmderstood when the unusual nature of the glacier 

 that formed it is considered. This represents the position of the front of the 

 easternmost ice stream, of the ancient piedmont Wenkchemna during a pro- 

 longed period of the halt. This moraine originally abutted against a wall of ice 

 at the west end, the side of the adjacent ice stream, which probably extended 

 far down the valley and may have been engaged in making a correlative moraine. 

 A relatively small amount of the debris was dragged for a short distance down 

 stream by this neighbor, forming the spur above noted. When this ice wall 

 melted away finally the debris rolled down and assumed the "angle of repose." 

 As has been pointed out the present easternmost stream is short, compared with 

 its neighbor, and were it to make a sufficiently prolonged halt there might be 

 produced, upon a smaller scale, this identical feature. 



c. Valley of Ten Peaks. The time that could be devoted to this glacier did 

 not permit of an examination of the valley from the lake to the Bow River, or of 

 the interesting Consolation Valley, which still supports a glacier at its head. 

 Observations of only a general nature from the elevated trail around Mt. Temple 

 could be made. There is evidence that the entire valley was occupied by a great 

 ice stream, a tributary of the trunk glacier that filled the Bow Valley, the glacier 

 then being of the Alpine type. The lower half of the valle}^ was altered by the 

 ice into the characteristic U-shape, while the upper half retained its flaring side 

 walls from pre-pleistocene time. In making the bend from its east-southeast 

 course to the northeast, the glacier pressed hard against the western face of 

 Mt. Babel, while upon the opposite, or concave, side there was deposited a high 

 ridge of ground-morainic material which swings around in a very regular curve 

 from the Eiffel to Mt. Temple. From the northeastern shoulder of Mt. Temple 

 there extends into the Bow Valley, curving gently down stream, a spur of ground- 

 morainic material, identical with that described for the Lake Louise Valley upon 

 page 8. This was deposited beneath the ice and along the line of junction of the 



