268 
The great anticline, just described, is the first indication 
of approach to a very disturbed area. On the western side 
the rocks rapidly increase in dip to 60°, in a west-north-west 
to west-south-west direction. This high angle of dip once 
more brings into the section the main limestone, followed by 
the yellow dolomitic limestone, with a dip of 60°-70°. These 
beds are in all respects similar to the corresponding outcrops 
higher up the valley, and have a surface spread of thirty 
yards. 
There immediately follow, in ascending order, purple cal- 
careous slates, green slates, and quartzites. These beds mark 
the passage upwards to the purple slates division, which ‘s 
the highest member of the series. There is the strongest 
lithological contrast in the appearance of the beds belonging 
to the respective divisions, and cannot fail to be noticed. 
Near the junction a very high cliff of purple slates occurs on 
the northern side of the stream, and in the face of this cliff 
the adit of the old Worthing Copper Mine (which failed to 
secure ore in payable quantities) has been driven. As is 
common in the purple slates, the beds are much cleaved and 
jointed, and readily break up into small prismatic fragments, 
making the determination of the bedding planes somewhat 
difficult, but they are here at a high angle of dip. The suc- 
ceeding beds become more siliceous, and split up into nume- 
rous thin beds of quartzite and shale, which are greatly 
contorted by acute and inverted foldings. Тһе alternation 
of beds of unequal compressibility has, no doubt, supplied 
favourable conditions for producing these effects. (See Plate 
xxxviii.) About half a mile from the coast there is a cal- 
careous belt in the rocks which shows a wavy structure, and 
is succeeded by more purple slates, calcareous grits, greenish 
to purple slates, and quartzites to the mouth 2f the river, 
where the cliffs consist of thin bedded, dark-coloured quart- 
zites and shales, with a dip of 85? to the west. The cliffs are 
capped by glacial drift and a superficial covering of Miocene 
sands and clays. 
At Black Point, the north headland of the kay, a very 
striking anticline occurs in the purple slates, with a sharp 
downthrow to the west. The top of the cliff is strongly gla- 
ciated, and within the amphitheatre, formed by the erosion of 
the rocks between the neadlands of the bay, the glacial drift, 
a hundred feet in thickness, occupies an eroded basin in the 
purple slates. A section across the beds can be seen in a 
small watercourse, situated about midwar between the two 
headlands, and at about half a mile from the sea a very 
acute anticlinal fold in quartzite can be seen forming a 
small waterfall. 
