BERNARDSTON SERIES OF UPPER DEVONIAN. 279 



beds of amphibolite mentioned are represented as one f>n the map, as they 

 are near together, and the northerly slope on which they appear approxi- 

 mates their ojutcrops still more. A long slope follows, with scanty outcrops 

 of mica-schist (r/), still fine-grained and without staurolite, but with one 

 small bed of amphibolite (A), and at its foot succeeds a heavy bed of horn- 

 blendic rock, about (16 feet thick, which, by the quite abundant devel- 

 opment of feldspar, is in large part a complete quartz-diorite-schist (?). 

 Except for the appearance of feldspar in small, irregular, white spots, it 

 does not deviate from the usual type of the hornblendic rock of the area. 

 It is followed almost immediately, though the exact contact could not be 

 found, by a bed, about 50 feet thick, of a fine-grained granitoid quartzite 

 (A-). This is, indeed, in its whole extent a complete granitoid gneiss, never 

 fissile, and faintly foliated only by the parallel arrangement of the biotite, 

 or wholly lacking this even, and becoming a fine-grained, tough, granite- 

 like rock, largely feldspathic and with many striated feldspar cleavage 

 surfaces and light gray from the small amount of the biotite. It can be 

 followed for a long distance, breaking off against a fault in the northeast 

 direction and going southwest across Dry Brook. Its place between the 

 two heavy hornblendic bands then seems to be taken by a very fine- 

 grained, massive quartz rock, with abundant fine scales of muscovite and 

 with large, round plates of biotite set at every angle. It appears again 

 farther northeast, at the last road across the range, and can be followed 

 thence continuously over the high hill west of South Vernon station and 

 across the plain in Vernon, trending here directly toward the point where 

 the road to Vernon goes beneath the railroad. It is unlike the basal quartz- 

 conglomerate on the west and the feldspathic quartzite — to be described — on 

 the east, and, conforming in dip and strike with the mica-schist and making 

 all the curves with it, it seemed to me for a long time that it must be looked 

 upon as a sepai'ate band in the mica-schist and could not well be derived, 

 by folding or faiilting, from the other quartzite. On noting, however, that 

 all the beds grow more metamorphosed and more feldspathic as thev go 

 east, and that in nearly every case the eastern bands of quartzite are 

 brought up by faulting and can be proved to be the same as the basal 

 quartzite, it has seemed to me most probable that this band has been 

 brought up in the same way and is identical with the basal quartzite. It is 

 lithologically transitional between the quartzose conglomerates farther west 

 and the feldspathic quartzites farther east. 



