548 STRATIGRAPHICAL GEOLOGY. 



is a mixture of coarse mica schists and fine-grained granitic beds dipping 

 about 65° N. W. Half way to Wilton the mica schist dips 30° N. 25° W. ; 

 also at Wilton, No ledges appear for a mile and a quarter on the section 

 line, when we find a spotted granite by H, F. Frye's, on the north-west 

 slope of a high hill. There is gneiss higher up, and at intervals to B. 

 Gray's, On the hill west of Gray's the rock is micaceous and gneissic, 

 dipping 80° N, 70° W., and that is also the position of the quartz. This is 

 about two miles from the south-east end of Fig, 90, There is a great 

 width of gneiss here at Gray's, though its place seems to be taken by 

 mica schist on Fig, 90, The gneisses, porphyritic granite, and mica 

 schists observe the same order as on Fig. 91, in proceeding from Temple 

 towards Greenville. There is a possibility that the rocks of New Ips- 

 wich and Greenville are older than those carrying the quartz, and hence 

 cut it off by rising to the surface. We have taken other observations 

 respecting the rocks between Figs. Sy to 91, which will be presented 

 later. The mica schists of these sections are supposed to belong to 

 the Rockingham series. 



Coiichtsions. These are not altogether satisfactory, i. We think the 

 quartz bands are stratified, and connect in a synclinal manner with each 

 other, though inverted. Fig. ^% shows repetitions of a basin character, but 

 not in a decisive manner. The comparative recency of the mica schist is 

 apparent. It lies like a blanket upon the older gneiss. All the sections 

 can be explained in the same way, especially Fig, 90, where the quartzes 

 dip towards each other, 2, The southern segment of the Hooksett range 

 has a decided tendency to dip south-east., as shown through Lyndebor- 

 ough. The Manchester range invariably dips north-westerly. This fact 

 seems to confirm the theory of a synclinal connection between these 

 bands. 3, It would seem as if there had been a great fault in the strata 

 between Amherst and New Boston, so as to explain the absence of the 

 bands over so great a distance, 4, South of the break the bands are 

 much nearer each other than to the north ; yet the synclinal structure is 

 seen clearest where the compressions were most powerful, granting that 

 lateral force was the cause of the break and of the crowding together. 

 5, The Greenfield spur of porphyritic gneiss is parallel with the quartz 

 band, and extends exactly the same distance to the north-east, while 

 beyond there is an expanse of the Lake gneiss directly opposite the 



