440 STRATIGRAPHICAL GEOLOGY. 



distance, 50°, then 5° S. 20° W. and 75° W. Then we have on the west 

 side of Bald mountain the dip 15° S. 50" E., and above Shattiick brook, 

 in the valley of Fall river, 50° S. 40° E. 



The quartzites are supposed to be continuous from South Vernon 

 to the north-west part of Gill, passing through the south-east corner 

 of Bernardston. At the railroad crossing, in the south-west corner of 

 Northfield, the quartzite (No. 14) dips 25° S. E. immediately adjacent to 

 hornblende schist (No. 16) supposed to have the same dip. Near Pur- 

 ple's house, in the east part of Bernardston, we find a gneiss (No. 13) and 

 a conglomeratic feldspathic quartzite (No. 65), with well-defined quartz- 

 ites, all dipping about 30° S. 30°-40° E. Thirty or forty rods north-west 

 of this house are ledges of hornblende schist, dipping 70° S. E., extend- 

 ing very near to Purple's quarry. A section line from No. 16 to No. 139 

 (Purple's quarry), a part of Fig. 72, shows the same order of rocks as along 

 the state boundary. The same order may be obtained farther south-west. 

 The eastern mass of hornblende occupies much of Gill; and its junction 

 with the quartzite appears at the crossing of the north line of the town at 

 Unadilla brook, and at a fork in the road about a mile east of Otter pond. 

 No. 15 represents quartzose gneiss, a rock physically like quartzite, and 

 shown by Prof. Dana to have feldspar in it. The dip is i5°-25° S. E. On 

 the road north-westerly from No. 1 5 are outcrops of hornblende schist, 

 graduating into sienitic gneiss, dipping 15° S. 40° E. (No. 17), In passing 

 west, the next rock is the principal mica schist range (No. 138). The 

 quartzite range continues from this last sectional line, underneath a wide 

 expanse of gravel, to the neighborhood of Otter pond in Gill. About half a 

 mile's width of it may run between this pond and Fall river, dipping south- 

 westerly. It then passes out of sight beneath the Trias. At No. 68, west 

 of Grass hill, the dip is 30° S. 40° E., agreeing with the usual dip of this 

 formation, but near Fall river, along the line of strike, it has changed to 

 north-west. This fact may indicate the ])rcscnce of an anticlinal, not 

 commonly observable because inverted. This affords data for believing 

 this quartzite is the repetition of the bands, soon to be mentioned, north 

 of the village of Bernardston. All authors have assumed the identity of 

 the South Vernon range with that connected with the fossils. If so, the 

 connection is through folding and not by continuity, since the strikes are 

 different, as exhibited upon the map. P^or the benefit of any persons 



