PROCEEDINGS OF SECTION C. 415 
Among the felspars, some were good instances of that form of 
structure where the interior is well crystallised with a margin of 
greater or less width, less ideomorphic, and apparently of some- 
what different constitution, for the interior was mostly more con- 
verted into mica than the exterior. The quartz, which was fairly 
abundant, had the usual character of that found in such rocks. 
In this sample there was no appearance of crushing, or of the 
linear arrangement of the minerals. 
Among these more massive rocks there is a narrow band, 
having the appearance of a quartzose schist, but, on examination, 
I found it to be a prepared and very quartzose rock belonging to 
the quartz-diorite group. 
Beyond this point the rocks are more or less massive quartz 
diorites, with here and there schistose bands, and this formation 
extends westward to the upper Dargo River, of which I have 
already spoken. 
Speaking generally, I may now say that the schists of Green 
Wattle Creek are gneisses, more or less micaceous, felspathic, or 
quartzose. They are composed of the mechanically rearranged 
constituents of massive plutonic rocks, as diorites and granites, 
such as are to be found in the neighbourhood. They are not the 
metamorphosed representatives of sedimentary beds, as are the 
mica schists to the north-eastward of the Frenchman’s Hill. 
The examination shows that in the metamorphism of the 
gneisses the original minerals have differently resisted the forces 
acting upon them. The felspars have been crushed, broken and 
rounded off, but hardly, or at all, distorted or stretched. The 
quartz, on the contrary, has not only been crushed and broken, 
but it has become so plastic as to be found in long drawn out and 
eventually bent portions. The detrital material has been 
regenerated mostly as biotite, and apparently there is most biotite 
in the most disturbed portions. It has also produced muscovite, 
and more rarely intergrowths of quartz and orthoclase in the 
graphic manner, as micropegmatite. The felspars can be recog 
nised as being original crystals which existed in a rock apparently 
analogous to these massive plutonic rocks, which occur in the 
same locality. 
The quartz of the foliatures is of two kinds—original quartz 
grains which have been crushed, and, in a much greater amount, 
quartz which has been produced in the form it now has during 
the metamorphic action. 
It seems to me to be now clear that the crystallised schists 
of the Omeo district are, as I indicated before, of two kinds. 
Mica schists which have been formed by the metamorphism of 
Lower Palzeozoic sediments, and gneisses which have been formed 
by the metamorphism of quarts diorites and granites. Where 
the sedimentary rocks and the plutonic rocks have both been 
involved in the same process, the mica schists of the one and the 
