254 ANTICLINALS. 



some conclusions of importance follow. And first, if the strata have been folded by a 

 force from the southeast, crowding them northwesterly, or rather almost westerly, we 

 should expect, notwithstanding powerful denudation, to find evidence of the plica-ting force 

 in the form of anticlinals and synclinals, running nearly lengthwise of the State. Let us 

 see whether such exist. 



We begin with the section (Plate XV) , crossing the north part of Massachusetts, a little 

 south of Vermont. Towards its east end we find a distinct anticlinal at Shelburne Falls, 

 whose lowest part is gneiss, overlaid by hornblende and mica schists. Looking at the 

 first section, we see in Guilford a continuation of the same anticlinal, though smaller per- 

 haps because less denuded. So on Section II, in Brattleboro ; on Section III, in New- 

 fane; on Section IV, in Grafton; on Section V, in Windsor, (thus far the axis is in gneiss) ; 

 on Section VI, in Hartford, in calciferous mica schist ; on Section VII, in Sharon, in mica 

 and hornblende schists ; on Section VIII, between Corinth and Washington, in mica 

 schist ; on Section IX, in Orange, in mica schist, with a granitic axis ; on Section X, in 

 Peacham and Marshfield, with a broad granitic axis ; on Section X a, in Danville, in mica 

 schist ; on section XI, in Sheffield, in mica schist, with a granitic axis. In the two north- 

 ern sections the great development of granite may have destroyed this anticlinal ; but it 

 seems manifest on all the others though somewhat tortuous in its course. 



We think another important anticlinal occupies the crest of the Green Mountains, 

 mostly in gneiss. On the Massachusetts section in Florida, and Section I, in Readsboro ; 

 Section III, in Stratton ; Section VI, in Sherburne ; Section VII, in Goshen, and Roches- 

 ter; and Section VIII, in Granville, the strata all dip to the east ; but as this is probably 

 an inverted dip, the whole may be an inverted anticlinal. But the occurrence of opposite 

 dips in Searsburg ; on Section II, in Peru ; on Section IV, in Mt. Holly ; on Section V, in 

 Bolton ; on Section IX, in Duxbury ; on Section X, in Underbill and Stowe ; on Section 

 X a, and in Johnson on Section XI, all of which are along the crest of the mountain, 

 makes it almost certain that an anticlinal exists there, and that the inverted dips on the 

 other sections may be folded anticlinals. The same is probably true of Section XII, 

 between Lowell and Montgomery, although the strata lean slightly towards the east, and 

 therefore the anticlinal is not inverted; but it may be closely folded. Still more obviously 

 is there an anticlinal on Section XIII, in Jay, where the rock is talcose schist ; but it is 

 doubtless a continuation of the Green Mountain chain. 



Synclinals parallel to the above anticlinals can be traced on the sections. Most of them 

 are remarkably sharp, bringing the strata into an almost perpendicular position. One 

 may be seen along the junction of the calciferous mica and talcose schists; as in Charle- 

 mont, on the Massachusetts section, in Halifax on Section I ; between Brattleboro and 

 Marlboro on Section II ; in Wardsboro, in gneiss, on Section III ; in Grafton, in gneiss, 

 on Section IV ; in gneiss and talcose schist on Section V, in Cavendish ; in mica schist in 

 Woodstock, on Section VI; in talcose shist on Section VII, between Bethel and 

 Rochester ; in Roxbury between talcose schist and clay slate, on section VIII ; in talcose 

 schist in Middlesex, on Section IX and X; between talcose and mica schist in Hardwick, 

 and a second in Morristown, on Section X a; in talcose schist in Hydepark, on Section XI; 

 between talcose schist and clay slate in Lowell and Irasburgh, probably on Section XII; 

 and between the same belts of slate in talcose schist in Newport, on Section XIII. 



