st. JOHN.| MORAINAL DEPOSITS EAST FOOT WIND RIVER RANGE. 265 
terraces vicinity of Warm-Spring Creek to the undoubted glacial de- 
posits. They appear in terraces along the south side of the river, at 
elevations of 150 feet or more. The deposit is composed of well-rounded 
fragments of volcanic rocks, limestone, quartzite, and occasional granitic 
pebbles, obscurely bedded, with thin sheets of sand. ‘The impression 
derived in the course of hastily made examinations was that these de- 
posits antedate the glacial epoch, in which event they might properly 
be relegated to the Pliocene. Their consolidation might have taken 
place at a much later date from caleareous matter deposited by perco- 
lating spring-water. 
in the vicinity of Jake’s and Torrey’s Creeks, the morainal deposits 
are on a scale of great magnitude, presenting all the characteristic phe- 
nomena usually associated with glacial accumulations. The outlying 
terraces are strewn over a wide area with this vast accumulation of 
erratic materials, reaching from the river back to the mountain where 
they occur at an elevation of several hundred feet above the valley. In 
the constitution of the deposit metamorphic bowlders largely predomi- 
nate, with which are sparingly associated fragments of limestone and 
quartzitic sandstone belonging to readily recognizable formations plating 
the neighboring mountain flank. The region occupied by these deposits 
forms a sort of high bench either side of the debouchures of the streams, 
the surface roughly furrowed just as the material was discharged from 
the glacier. Remnants of the glacial deposits occur on the north side 
of Wind River below the mouth of Torrey’s Creek, where they are seen 
clinging to the steep bluff slopes over the variegated Tertiary formation. 
Yo the southeast the mountain slope is again unmasked until reaching 
Campbells Fork, where similar morainal deposits are met with, though 
on a less extensive scale. At the latter locality the erratic materials are 
piled up in well-defined lateral morains on either side of the stream as 
it leaves the mountain, and which extend all the way to Wind River a 
distance of nearly 4 niles, where they are spread out in irregular low 
benches. The moraines rise up on the foot of the mountain attaining an 
elevation of near 8,400 feet, or 1,000 feet above Wind River. In the 
gorge across the sedimentary ridge the Carboniferous limestones at one 
point form a natural bridge, and everywhere in the barred surfaces the 
rock still retains in legible characters the record engraved by the glacier 
in the smoothed and polished ledges. This is the more remarkable con- 
sidering the exposure to which these rock surfaces have been subjected. 
The cation has been swept clean of these materials, but within the rugged 
mountain basin they recur under a variety of local aspects. 
The streams to the south that rise in the more elevated portion of the 
range all exhibit in their debouchures interesting evidence of former 
glacial occupancy. But none of the smaller streams show morainal de- 
posits of near the magnitude of those above noticed. This is evidently 
due to the fact that the present streams do not penetrate so deeply into 
the more elevated regions, and hence the glaciers that once descended 
along their valleys were smaller and derived their products from less 
abundant sources. The lateral moraines on Dry Creek below the de- 
bouchure are quite as perfect examples of their kind as any to be met 
with on this side of the range. They reach well out into the sloping 
plain, presenting in their surface contour the several bench levels in the 
steep valley declivities marking the stages in diminution in the volume 
of the glacier and on the opposite side the furrowed gentler slopes de- 
scending to the general upland level. Between these streams the 
mountain side reveals the sedimentary formations in great upraised 
benches which form a characteristic feature in the surface configuration 
of the flank of the range. 
