Limestone Belts of Westchester County, N. .Y. 207° 
and here the junction of the schist with the granite looks more 
abrupt, but partly in consequence of erosion ; above this plane 
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of junction, in the mass of the granite, distinct though fainter 
indications of flexed beds exist. The change above m from 
soda-granite to quartz-dioryte is simply a change in the substi- 
tution of hornblende for the larger part of the black mica, the 
feldspars being equally triclinic in the two, and the quartz 
equally deficient in amount. Atasmall bluff, 160 yards to the 
west of m (at 0, see map), the change is more abrupt than be- 
tween m and 7; in only six feet, the rock passes from soda- 
granite to the dioryte. 
A natural inference from the series of facts presented in this 
section, those as to the flexures in the schist as well as the 
changes at the junction of the schist and granite, would be 
that the heat of metamorphism increased from the limestone 
northward toward the granite and dioryte region, the heat be- 
ing a consequence in part, if not chiefly, of the movement and 
friction attending the flexing, and that consequently there was 
produced a more and more yielding condition in the material 
of the schist as the region mf complete fusion was approached, 
and, at the junction, perhaps a fusing and obliteration of por- 
tions of some layers of the schist; and that a bed of schist 
existed in the granite which approached somewhat the granite 
in character, but which, owing to the nature of its material, 
was not wholly obliterated. 
ut, are not these flexed portions of beds fragments that 
were broken off and carried up by the fused or plastic material 
as it rose from depths below? They lie so conformably to the 
flexures of the schist as to suggest a negative reply to this 
query. 
_ Sections 2 and 3 (at p, and gq r s, on the map) show inclu- 
sions on a grander scale, 
