Vol. 58. | SUBALPINE PLIOCENE CONGLOMERATES. 455 
between Waldshut and Laufenburg, near Doggern, Kiesbach, 
Albbruck, and Hauenstein, the contact of the Deckenschotter with 
the underlying Triassic rock and Black-Forest gneiss varying 
from contour 500 near Waldshut down to 430 metres near 
Laufenburg.! That is, they occur at practically the same altitude 
as the corresponding Deckenschotter-deposit near Leibstadt and 
Leuggern, on the left or Swiss side of the valley, as is shown in the 
cross-section (fig. 2, p. 453). The Aarberg, a hill immediately east 
of Waldshut, is also capped by Deckenschotter resting upon Triassic 
rock; and still farther east, near Dangstetten, there is another 
similar deposit. The geological maps of the district designate those 
deposits roughly as ‘ Glacial, without discriminating between them 
and the younger gravels at lower altitudes; but their position, as 
well as the fact of their being composed of Alpine material—chiefly 
grey limestone, diorite, and quartzite,—leaves no doubt as to their 
connection with the Deckenschotter-deposits on the left, or Swiss, 
side of the valley. Itis only in the deposits nearest Laufenburg 
and towards Rheinfelden that Black-Forest material, easily recog- 
nizable by the considerably larger size of the pebbles, begins to 
be extensively mixed with Alpine material on both sides of the 
valley. A notable instance on the Swiss side is an extensive 
Deckenschotter-deposit on the Berg, a hill between Rheinfelden 
and Kaiserangst, about 10 miles east of Bale, where the Decken- 
schotter (which is overlain by moraine) rests upon Triassic rock 
at about contours 360 to 370 metres, or 100 metres above the 
present river-level (263 metres). 
(6) The evidence thus furnished by the various deposits points to 
the following conclusions :— 
(i) The deposits indicate, in an almost unbroken outline, the 
former existence of a Deckenschotter-cone extending, 
at the time of the Upper Pliocene glaciation, from the 
base of the Alps in a north-westerly direction over a 
distance of about 60 miles, and radiating from an ice- 
sheet the maximum extension of which probably did not 
reach beyond a line drawn from the Uetliberg to Mount 
Irschel. 
(11) The Deckenschotter-cone, largely composed of retransported 
material derived from Miocene Nagelfluh, had a fall of 
about 6 metres per kilometre (say 32 feet per mile), 
and was formed by the waters of the western branch 
of the Rhine Glacier then emerging through the Walensee 
defile, and reinforced by the Linth, Sihl, and Lorze 
Glaciers.” 
* An interesting monograph on the Rapids of the Rhine at Laufenburg, 
showing a former canon of the river at some distance from the present bed, 
has recently been published by Dr. H. Walter (‘Stromschnelle von Laufen- 
burg’ Abbandl. Naturf. Gesellsch. Zurich, 1902, pp. 232 et seqq.). 
* The Lorze, descending from the Rossberg, formed at a later period part of 
the Reuss drainage-area. 
Tene 
