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 

 described, there appears no improbability in the suggestion that the 



