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PROFESSOR T. J. JEHU AND DR ROBERT CAMPBELL ON 
fig. 6, and Plate IV, fig. l) curve round the mosaics of albite or albite and epidote 
which constitute the “ eyes,” showing that the movements which induced the mole- 
cular change from augite to hornblende and from labradorite to albite and epidote 
were the movements which produced the foliation. Yeinlets of water-clear albite, 
or less often chlorite, traverse the schist structures ; those were formed after the 
movements of compression had ceased. 
Locally the hornblende schists pass into massive epidiorite, in which the relations 
of the felspar to the hornblende are sometimes suggestive of the preservation of 
ophitic structure. None of the original minerals remains, however, and, as in the 
foliated types, the rocks have undergone complete reconstruction. 
The rocks of the western part of the belt are less uniform in character. They 
may. be studied best in the main branch of the Corrie Burn. There they are seen 
to include two main groups : (a) hornblende schists, (b) chlorite schists, occupying 
respectively the eastern and western portions of the stream section. 
The hornblende schists are more coarsely crystalline than those above described, 
and show greater variation in their mineral composition. On the whole they are 
distinctly less felspathic. One narrow band near the Jasper Boundary Fault is an 
actinolite schist (Plate IV, fig. 2) made up entirely of amphiboles, which are pale 
green in hand specimens and colourless in thin section ; sometimes, again, the rocks 
consist essentially of green hornblende along with much epidote and zoisite, and in 
these veins and segregations of epidote are common ; biotite and iron ores occur as 
occasional additional accessories, and locally the rock is so rich in the former mineral 
as to become a biotite-hornblende schist. Felspar, although present, is largely 
replaced by colourless micas. Where those coarse hornblende schists appear 
again further south-west in a small tributary of the Corrie Burn they are rich in 
accessory rutile, and at one point they are traversed by pegmatitic veins of pink 
microcline. 
In only one instance has a massive band been observed in the Corrie Burn. It 
consists of an epidiorite (Plate IY, fig. 3) richly charged with anhedral pink garnets 
and crossed by numerous quartz veins. When the rock is decomposed, both the 
garnets and the hornblende are replaced by chlorite. Iron oxides and apatite are 
rather abundant as accessory minerals, and the rock is much richer in quartz than 
any of the associated types. 
The chlorite schists are paler in colour and finer in texture, and under the 
microscope they are seen to be much more felspathic than the hornblende schists. 
Hornblende is absent, the rocks consisting of an aggregate of albite, chlorite, 
carbonates, and iron oxides. In the field they recall the spilites, from which 
they are distinguished by the presence of fine foliation. For the most part, like 
the hornblende - schists, they have undergone complete reconstruction. Locally, 
however, they contain narrow lath-shaped felspars, and those, together with 
the occasional appearance of micro-porphyritic texture, indicate that the original 
