Klamath Mouiitaiiis, California. — Hcrshcy. 141 
discussion, I will assume that a single elephant was wrecked 
on that spot. 
THE DEPOSITS AT AND IN THE VICINITY OF THE NASH MINE. 
Coffee creek, along this section of its course, has a general 
direction from west to east. About seven miles from its head, 
it is joined on the south by an important tributary. Union 
creek. In the main valley, several hundred yards above the 
junction of the two creeks, a point projects from the north 
slope. On its down-stream side is situated the present hy- 
draulic mine. This point covers a remnant of an old channel. 
The channel gravels resting on the bed-rock at the foot of the 
bank and constituting the ''pay streak" are a rather coarse, 
well water-worn creek deposit, five to fifteen feet thick.* It 
includes a considerable number of cobbles and small boulders 
of the Courtney granite. This rock is a peculiar coarse- 
grained, non-hornblendic granite which cannot be confused 
with any other and which is confined in place to Mt. Court- 
ney at the head of the present South Fork of Salmon river. 
In a paper on "Ancient Alpine Glaciers of the Sierra Costa 
Mountains in California,"! I showed how, largely through 
the operations of the Salmon River glacier, the upper four or 
five miles of the original Coffee creek was cut oft" and added 
to the Salmon river system. Before this beheading, Coffee 
creek rose at the foot of Mt. Courtney and the Courtney gran- 
ite was distributed along the valley to and below the site of the 
Nash mine. At the time of the maximum extension of the 
Salmon River glacier as described in the above mentioned pa- 
per, it was carrying Courtney granite to the headwaters of the 
present Coffee creek but its overwashed gravels are fine and 
there is no reason for believing that the Courtney granite at 
the Nash mine was derived from that source. The size of this 
first channel and the abundance of Courtney granite in small 
boulders make it reasonably certain that the deposit was 
formed by Coffee creek before its shrinkage through behead- 
ing, and it may be considered essentially pre-Glacial so far as 
California glaciation is concerned. However, it is not nearly 
as old as the "high-level channels" of the Sierra Nevada rc- 
* Nearly all the figures in this paper are given from memory andmay not 
he quite accurate, but the discrepancy will not be sufficient to vitiate the 
arguments. 
f Journal of Geology , vol. viii. No. 1, pp. 42-5 7. 
