Vol. 60. j GLACIAL GEOLOGY OF TASMANIA. 49 



A second glacier flowed along the King Valley, south of the 

 Eldon Range, and was continued westward along the Sedgwick 

 Valley to the north of Mount Lyell. It deposited a moraine, 

 imperfectly preserved, north of the Comstock Mine. I saw no 

 evidence that this glacier extended farther westward. Another 

 hranch of the main glacier flowed southward along the present 

 course of the King Valley, and abutted against the eastern face of 

 Mount Lyell. On the melting of the glacier, the slopes of the 

 valley were covered with a thick deposit of boulder-cla3 r . This 

 glacier continued farther southward, and deposited a terminal 

 moraine between the eastern base of Mount Owen and the Thureau 

 Hills. A lobe from the glacier flowed westward up the valley of 

 the Linda — a valley due to fault-action. The ice of this lobe flowed 

 over the schist-ridge that separates the Linda and Queen Valleys. 

 It wore the conglomerate-spurs from this ridge near the Linda 

 township into roches moutonnees, and deposited some boulder- 

 clay with diabase-boulders at Queen stown, where some of the material 

 is still preserved opposite the Mount-Lyell Company's pumping- 

 station (altitude 464 feet). During the retreat of this Linda- 

 Valley glacier, a glacial lake formed between the glaciers and the 

 Mount-Lyell ridge ; the drainage from this lake escaped southward 

 into the valley of Conglomerate Creek, cutting the Gormauston Gap 

 (altitude 1356 feet). One important stage in the retreat of this 

 glacier is marked by the deposition of the great Gormanston 

 Moraine. 



VI. The Range of the Pleistocene Glaciation. 



The extent of the Pleistocene glaciation is shown on the 

 accompanying sketch-map (fig. 2, p. 50). The localities marked by 

 asterisks are those where glacial deposits, which I regard as Pleis- 

 tocene, have been recorded. The small letters (c) indicate localities 

 of glacial deposition probably dating from the Carboniferous. The 

 correlation of the deposits to the north and west of Mount Lyell 

 rests, in part, on the lithological nature of the deposits, and partly 

 on other indications of ice-action in their localities. 



During a first visit to Tasmania I had been struck by the 

 morainic aspect of some beds near Farrell, on the Emu-Bay and 

 Zeehan .Railway. The locality is about 60 miles from Burnie, at an 

 altitude of 1300 feet. For an opportunity of examining these beds 

 I am indebted to Mr. J. Stirling, the manager of the railway, who 

 kindly stopped the train for this purpose. The evidence available 

 clearly shows that the beds are of glacial origin. They include some 

 gigantic erratics of conglomerate : one measures 25 by 18 by 12 feet, 

 and numerous smaller erratics occur beside it. They are not frag- 

 ments, left in situ by the denudation of a band of the West-Coast 

 conglomerates, for they rest on a bed of clay. Mr. Stirling tells me 

 that, during the construction of the railway, a hole was dug into 

 this clay, at a culvert a few hundred vards south of the biggest 



Q.J. G.S. No. 237. b 



