REPORT OF THE DIRECTOR IQIJ IO5 



or semiviscous state. A primary foliation independent of any 

 crushing is indicated by the frequent parallel alignment of slender, 

 unbroken, dihedral zircon crystals, by the segregation of the com- 

 ponent m'nerals in individualized streaks, and by the flattened, 

 uncrushed character of the quartz. 



11 The evidence of a preexisting protoclastic foliation in the 

 cataclast'c-protoclastic gneiss of the northwest zone is: the presence 

 of a transition into the protoclastic gneiss of the central zone through 

 a disappearance of the superimposed cataclastic features, and the 

 presence of slm'lar characters to those of the latter band. Quartz is 

 normally the first mineral to fracture in the process of rock crushing. 

 In these gneisses the quartz is less mashed than the feldspar, which 

 indicates that it was not affected by crushing until after the feldspar 

 had already been pulverized. Such a phenomenon might happen in 

 the case of a magma undergoing pressure in which the quartz had 

 not yet crystallized out, whereas the other minerals constituted a 

 continually growing and falling meshwork. The continuation of the 

 pressure after complete consolidation then granulated the quartz in 

 its turn. 



12 The grains resulting from the crushing of any rock from within 

 the central zone will, with only rare exceptions, average over o.i mm 

 in size, those of the northwest zone (quartz excluded) under o.i mm 

 in diameter, but the proportion of the minerals in the rock of either 

 zone which is reduced to these respective sizes is very variable in 

 different streaks, often sharply delimited and parallel to the 

 foliation. 



13 The forces which resulted in the production of the foliation 

 were not attendant upon a shouldering influence against the Grenville 

 exerted by the magma during intrusion, but were the result of 

 orogenic stresses exerted from without, because 



a Later intrusive dikes of hornblende syenite, hypersthene syenite, 

 hyperite, grano -syenite and pegmatite all exhibit the same degree 

 of metamorphism as the country rock of the zone of metamorphlsm 

 in which they occur. This is best exemplified by the case of the 

 hyperite dikes. According to the usual mode of geological reasoning, 

 these dikes mist all be of essentially the same age. They are uni- 

 formly slm'lar in character" where 7er found, have a tendency to 

 cluster more abundantly around local stocks of gabbro, and always 

 bear analogous relations to all rocks with which they are found in 

 contact. There is nothing to suggest that we are dealing with 

 dikes of more than one epoch of intrusion. Yet where these dikes 



