368 C. CALLAWAY ON THE NEWEK ONEISSTC
loch under Coniveall. Two years ago I submitted to the Society
reasons for believing that the limestone at Inchnadamff was the
highest rock in the district ; and I showed that, when followed to the
south-east, it was seen to dip away from the so-called " Upper "
Quartzite, and to form the north-eastern side of the Stronchrubie
basin. Having minutely resurveyed the ground, I beg to offer
what appears to me absolutely conclusive proof of my original view.
The western slopes of Cnoc-an-drein extend between the Burn of
Calda and the parallel stream called Poulan-drein, a breadth of over
a mile. The junction between the Dolomite and the " Upper "
Quartzite is more or less clearly exposed in the escarpment between
the two burns, and more distinctly in the burns themselves.
Section on the Burn of Calda.
Leaving the high road a little north of Inchnadamff, and ascending
the slope towards the col between Cnoc-an-drein and Glasven, we
first detect small faults in the Dolomite ; and a little higher up the
throw increases, the Brown Flags, much squeezed and contorted, re-
appearing east of the Dolomite and being followed by a repetition of
the Dolomite in regular sequence. Beyond this, the evidence at first
sight appears to favour the old view. In Calda Burn, at a water-
Fig. 2. — Section on the Burn of Calda. (Scale 5 inches to 1 mile.)
fall, the Dolomite, somewhat contorted, is seen to be succeeded and
seemingly overlain by quartzite. Two facts, however, at once suggest
suspicion of this apparent conformity. Ascending the stream, we
find the quartzite dipping regularly to the E.N.E. for nearly a
quarter of a mile ; but suddenly the dip rises and the rock is bent
back into a large overthrown fold (fig. 2). This contortion is clearly
seen on both sides of the burn, which here forms a cataract, whose
bed is in part formed by the curved surface of the strata. The
quartzite is overthrown about 20°, the strata dipping into the hill at
70°. Again, in a small tributary of the burn, close to the junction of
quartzite and dolomite, is a fragment of a bed of dolomite 18 inches
thick, evidently not far from its matrix. This block is bent in the
middle into a small overthrown fold, as clearly as could be repre-
sented in a diagram. Now the large overthrow in the quartzite higher
up proves the operation of an enormous lateral force ; and the contorted
dolomite shows that the same pressure was at work at the junction.
Taking these facts in conjunction with the graduated faults before