55 
this and the Mornington districts. The rock from Harkaway—of which the 
pin tonic rock herein referred to is the southern extension—he speaks of as 
“ fine-grained syenite, showing a white felspar (both monoclinic and triclinic), 
biotite, hornblende, and much quartz”; while the rocks from Frankston and 
Mount Martha are referred to as granitite and syenite respectively.] 
Leaf-beaeing Clays. Eocene ? 
In the entrance to Wilson’s quarry, Berwick, lying on the Silurian and 
overlain by basalt, there is an interesting: occurrence of rocks, as shown in 
the accompanying section. The bed next to the Silurians consists of argil¬ 
laceous breccia-conglomerate, containing angular and sub-angular pebbles, 
and pieces of claystones and sandstones, apparently derived from the subjacent 
Silurian rocks. Conformably on these lie white sandy clays, then white pure 
clays containing indistinct remains of plants. These beds show a steep slope, 
against which lies basalt in the same way as is the case at Landslip Point, 
near Frankston. 
The contiguous clays are hardened for from 4 to 5 inches from the contact. 
Whether this induration has in both cases been caused by the basalt or bv 
V t. 
heated waters percolating through them is not by any means clear. 
Overlying both them and the Silurians is a thin covering of volcanic soil, 
containing pieces of basalt, which has been brought over by subaerial 
denudation. 
The Eocene? beds have no definite dip showing, but judging by their 
appearance it seems to be a rather high one. They are almost identical in 
general appearance and succession with the similar beds near Frankston, and 
may be correlated with them. 
Further particulars regarding this locality and others referred to later may 
be obtained from my report* on the district. 
Underlying the basalt in the floor of the quarry are small exposures of 
yellow, white, black, and brown soft clays and sandy clays, some of them 
containing leaves of dicotyledonous plants in great abundance. The yellow 
clays especially are very rich, but they are so much jointed that seldom can 
a good specimen be preserved. The white clays and sandy clays do not 
contain so many impressions, or show them so distinctly, but they are in a 
much better state of preservation. The black clay is very much jointed, and 
in physical appearance is somewhat like kerosene shale. The joint planes 
are filled with carbonate of lime, derived probably from the overlying basalt. 
The thickness of these clays was not observable, but Mr. J. Duncan, foreman 
of the quarry, informed me they were a few feet thick, while underlying 
them is a bed of white “ pipeclay,” 15 feet thick. The visible clays appa¬ 
rently dip about N.E. at about 14°, but as their surface is very uneven, this 
dip, which was taken on a small outcrop, may be unreliable. 
In some places basalt may be seen in depressions up to 10 feet deeper 
than the level of the floor of the quarry. Though the beds lying against 
the steeply eroded Silurian face contain indistinct remains of plants, ap¬ 
parently similar to those in the clays in the floor of the quarry; and though 
there is a resemblance between the two clays, still there does not seem 
to be sufficient evidence to regard them as portions of the same bed. As 
work progresses in the quarry more light may be thrown on the matter. 
* Kitson, Report on the Coast Line and Adjacent Country between Frankston, Morning- 
ton, and Dromana. Geol. Surv. Viet., Monthly Prog. Rept., No. 12, March, 1900. 
