^{page 215 note 1} Cf. Parker, G. H., “The Locomotion of Actinians” : Science, 03 26, 1915, p. 471.Google Scholar

^{page 215 note 2} Q.J.G.S., vol. lx, pp. 65, 316, 1904.Google Scholar

^{page 220 note 1} In the other lakes the fluviatile bars were formed by the following rivers: in the Lake of Zurich, by the Sihl ; in the Walensee (an old branch of the Rhine), by the Linth ; in the Lake of Lucerne, by the Emme, which, however, only deflected the Reuss instead of barring the lake ; in the Lake of Thun, by the Kander ; in that of Brienz, by the Lutschinen delta of Interlaken ; in the Lake of Geneva, by the Arve ; and in the Lakes of Neuchatel and Bienne, by the Aare.

^{page 221 note 1} The most formidable of these deltas is probably that of the Drance at Thonon (Savoy), which projects already 2 kilometres into the Lake of Geneva.

^{page 221 note 2} Of this, striking evidence is afforded by the interglacial gravel beds near Zurich, the material of which, being strictly fluviatile, can only have been transported across the filled-up lake by a river.

^{page 221 note 3} Heim, , Gletscherkunde, 1885, p. 542Google Scholar ; also Favre, , Récherches Géol., 1867, p. 210.Google Scholar

^{page 222 note 1} For instance, a glacier, to traverse a filled-up lake basin 40 kilometres in length, like that of Zurich, at the rate of 0·3 m. = 1 foot per day, would require over 300 years, and in the case of the Lakes of Constance and Geneva double that time.

^{page 222 note 2} The diagram refers to the area of the junctions of the sub-Alpine rivers between Zurich and Bale. In the Alpine valleys the former higher level of 400 metres would place the then valley floor, e.g. in the Linth Valley, on a level with the present Klōntal Lake, a hanging valley 400 metres above Glarus.

^{page 223 note 1} Some Swiss lowland Deckenschotter deposits at a somewhat lower level than the typical high-level ones led Mühlberg, Penck, and Brückner to assume a fourth glaciation (in the Tyrol even five), intermediate between the first and maximum glaciations ; but those lower deposits may be, like that of Teufelskeller, near Baden, west of Zurich, due to local subsidence.

^{page 223 note 2} On the other hand, a big glacier is indirectly a potent factor in valley-making and valley-shaping by the disintegrating action of frost and of the great differences between extreme temperatures on the mountain-sides as well as by its great lateral and vertical pressure. In this action lies obviously the via media between the extreme views pro and contra glacial erosion.

^{page 224 note 1} Renevier, L’Axe Anticlinal de la Molasse, 1902Google Scholar; Heim, Beitrage, xxv, p. 475, 1891.Google Scholar

^{page 224 note 2} The retreat of the glaciers must have been of very long duration, for in the Zurich sub-Alpine valley alone there are no less than four successive moraine bars across it, each of which is evidence of a long stage in the recession.

^{page 224 note 3} A similar instance of zonal subsidence appears to be that of the Cleveland (Yorks) and the Black Combe (South-West Cumberland) “ancient glacier lake” districts, both of which, according to Kendall, P. F. and Smith, B., were in pre-Glacial times at higher levels than at present (Q.J.G.S., vol. lviii, p. 471, 1902CrossRefGoogle Scholar ; vol. lxviii, p. 402, 1912).

^{page 224 note 4} In 1906 an instructive section was exposed at Clarens at a junction of roads about 60 metres above the lake, showing about 20 metres of moraine with overlying stratified gravel dipping reversely like the rock strata in the immediate vicinity.