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is mostly limestone. In the autumn of 1923 drilling was continued by W.
E. Thorne. Two cross-sections of bore-holes were put down, one about
700 feet east of the Yellow Lion tunnel and one 800 feet west. Both lines
of bore-holes showed approximately the same depths, the bedrock channel
being about 300 feet wide and having an average depth of about 45 feet,
and both showed some gold. There is not sufficient evidence to determine
definitely in which direction the old channel drained. The bedrock in the
bottom of the valley at the Bear dam 14 miles east is only about 5 feet
lower than at the line of bore-holes first drilled. A deeper channel, however,
probably occurs on the south side near the dam, for the present channel
has a steep gradient at this point, and, as the valley gradually widens
towards the east in the direction of the present drainage, it seems probable
that the ancient drainage was also in this direction. Two shafts were also
put down to test the value of the ground in the pass. One above the road
and 700 feet east of the Yellow Lion washing plant was 26 feet deep, but
was not to bedrock, the flow of underground water proving too great.
The other is just below the road and 350 feet west of the Yellow Lion. It
is 23 feet to bedrock. Joseph Spratt, who helped sink the shafts, states
that good prospects of gold were found in gravel at the bottom of the
first shaft and in gravel in the second shaft from the surface down to 20
feet, there being 3 feet of dry slum on the bedrock.

Cunningham Creek

The headwaters of Cunningham creek are in Snowshoe plateau
and Roundtop mountain outside the area. The main creek flows north
for about 6 miles to Cunningham Pass valley, where it turns abruptly
towards the east. The stream is one of the largest in the area and is larger,
where it joins Cunningham Pass valley, than Antler creek opposite the
upper end of the pass. The lower part of the valley is flat-bottomed
(Figure 10) for 2 miles above the junction, the alluvial flat of the present
stream being from 300 to 500 feet in width, and has a surface gradient of
1-3 per cent. The sides slope fairly steeply and are drift-covered except
near the upper end on the right bank. Here, the bedrock outcrops in the
valley bottom and a series of remarkably flat bedrock benches 20 to 80
feet above the stream have been uncovered by hydraulicking. Lower down
on the right side the drift deposits are terraced in places, probably by ice-
border drainage at a time when the valley was partly filled by a glacier, for
the terraces occur only on one side and there is no evidence that the valley
has been cut down from the level of the terraces to its present level in post-
Glacial time. The rock benches, however, must have been cut before the
deposition of the glacial drift which overlies them, and are, therefore, either
Glacial or pre-Glacial in age. A drift ridge about 100 feet high, through
which the present stream has cut a channel, extends part way across the
valley on the left side near the junction. It is a morainic deposit formed
partly by the Cunningham Valley glacier and partly by a smaller glacier
lying in Cunningham Pass valley. The ridge must have acted as a dam
for a time and caused deposition of silt in the broad part of the valley above.
Some of the lower terraces cut in the drift deposits along the left bank