368 PROCEEDINGS OF SECTION ©. 
Though the prevailing rocks are of granitic nature, the original 
sedimentary, but now altered, rocks are observable outcropping 
in several places. For instance, along the whole length of 
Kosciusko Valley they have been changed into highly siliceous 
and felspathic mica-schists, quartz-schists, micaceous hornfels and 
quartzites. They are much contorted, and some of them have 
veins and reefs of the white, vitreous and opaque quartz, so char- 
acteristic of schist areas. At the source of the Snowy River a 
large outcrop of very fissile, siliceous slates and quartz-schist 
occurs, and lower down the gorge these rocks are greatly contorted 
and splintered by dynamic agency. At various points in the bed: 
of the Leatherbarrel Creek, in Kosciusko Valley, rocks of a similar 
nature may be seen, all dipping to the east, with angles varying 
from 54 degrees to 85 degrees. They are greatly jointed and in 
places overlain by large transported granite boulders. On the 
lip of the gorge, near where this creek plunges into the wooded 
valleys below, are several outcrops of highly-altered siliceous 
slates, siliceous and felspathic mica-schist, quartz-schist, fine-grained 
gneiss, and fairly massive quartzites. The last contain a large 
quartz reef, 3 to 6 feet thick, having the same general northerly 
strike as the strata which dip to the east, and east 20 degrees south, 
at angles varying from 73 degrees to 84 degrees. © 
The rocks in Kosciusko Valley are apparently connected with 
those at the Leatherbarrel ford by an intermediate series such as 
is found between the ford and Monaro Gap, and which probably 
exists higher up the Leatherbarrel Valley, thus forming a gradual 
transition from foliated granite through quartz-schist and indurated 
spotted slates to the phyllites and soft, fissile, argillaceous slates 
near the Leatherbarrel ford. The resemblance between the rocks 
at the ford and some of those in Kosciusko Valley appears at first 
sight very striking, but close examination shows the latter to be 
more highly altered, and the fissility of the original slates to have 
almost completely disappeared. The quartz, again, in the two 
areas differs only in the fact that in the former it possesses thin 
jaminz of argillaceous slate, while in the latter the corresponding 
laminz consist of greenish mica, probably chlorite. In some cases 
the original sandstones have completely lost their clastic character, 
and have reached a more advanced stage of metamorphism than 
quartzites ; in other cases they are slightly spotted and micaceous. 
The altered olive-green argillaceous slates are less decided in colour, 
and much more indurated, but otherwise resemble the typical olive- 
green phyllites of the Leatherbarrel Ford and the ‘‘Gehi Wall.” 
As already pointed out,* numerous dykes intersect this area, and 
these Mr. Howitt has determined as andesites and quartz—horn- 
blende—and quartz—mica-diorites. Mr. Howitt’s examination, 
* “ Geological Notes on the Gehi and Indi Rivers,” &c. 
