234 E. HILL AND T. G. B0IOEY OJS T THE 



sharp roll or flexure, and the general succession of beds is clear. 

 In descending order it is : — (i.) indurated slate, some extremely 

 flinty ; (ii.) coarse gritty slate of an ordinary type ; (iii.) pale ob- 

 scurely banded slates of ashy character, with a coarse grit-bed 

 several feet thick ; (iv.) a breccia containing fragments, about eight 

 inches long, of a peculiar purple slate, and overlying a slate-bed of 

 a greenish-purple tinge. Now there is a very similar succession of 

 beds at the Eorest-Rock Inn near High Towers, where we find in- 

 durated slates with one bed extremely flinty, a grit-bed in the 

 spinney followed by rather ashy slates, and on the crest of the 

 hill the great slate-breccia. The flinty slates from these two 

 localities resemble each other and are very different from most 

 others in the forest, which are usually of a paler green. The grits 

 also differ from others and have some characters in common ; for 

 both contain felspar crystals as well as quartz, and some of the 

 felspar is tinged pink. The fragments in the breccias are dissimilar 

 in nature, but a bed below the High-Towers great breccia does con- 

 tain some purple slate fragments. The Bardon-Hill section fails 

 us just where these beds might be expected to come. Thus the 

 evidence, we think, renders the equivalence of the Warren-Hill and 

 Forest-Rock-Inn groups of beds probable, but does not convincingly 

 prove it. If correct, since the space between Warren-Hill and the 

 Cadman rocks to the W. is too short to contain the whole of the 

 Peldar-Tor beds, and since an outcrop of the Sharpley rock, their 

 equivalent, occurs a quarter of a mile to the E., Warren Hill must 

 be enclosed by faults. 



The flinty slate of the quarry N. of Whitwick, resembles that 

 near Forest-Rock Inn. The possibility that they may be the same 

 bed has often occurred to us, but such evidence as we can obtain 

 does not confirm the idea. If they were the same the former 

 would be much faulted, and it does show signs of disturbance. 

 The Whitwick Breccia also seems, from its southerly dip, to be cut 

 off from the general mass of the Forest rocks by a fault. This 

 must run along the depression between the quarry ridge and High 

 Cadman, and across the W. part of Broad Hill. It is very likely 

 connected at each end with the Boundary Fault. Our uncertainty 

 as to the correlation of these rocks prevents any estimate of their 

 displacement. 



The beds of the Charley and Blackbrook series appear less dis- 

 turbed than those above them. To this series an outcrop (not 

 mentioned in Part I.), N. of Gracedieu Hill across the dry canal 

 bed, seems to belong. The eastern end is slate much jointed and 

 stained ; the western is a mottled ash, resembling a bed of the 

 outcrop near Charley Wood. It is also on the direction of a line 

 through the uppermost outcrops of these beds, a line not differ- 

 ing much from their strikes. Thus there is evidence of little dis- 

 location along a line more than three miles long. This agrees with 

 the absence of faults E. of the anticlinal, and points to the centre 

 of disturbance having lain more to the west. This was the site of 

 the principal volcanic activity during the deposition of the Charn- 



