619 
The path of the glacier is traceable for a distance of two miles along the top 
of the scarped sea-cliffs at about forty feet above the sea-level ; on the north it is cut 
out from the cliff by encroachment of the sea; from this point the glaciated surface is 
continuous in a southerly direction for a distance of one mile to Black Point, the 
north headland of Hallett’s Cove. On the line of the glacier there now invervenes the 
broad but shallow bay of Ilallett’s Cove, but on the south headland the track is picked 
up on about the same trend, thougti apparently at a little higher level here again the 
glacier path is soon cut out by removal of the cliff. 
“ On the north side of the Cove the glaciated surface is beautifully displayed, 
the edges of nearly vertical strata are sheared off, and when of quartzite the surface 
shows a high polish, and when of mudstones conspicuous grooves and striae. Some 
moraine debris, including stones that have been beneath the glacier, occur here. On 
the south side moraine matter is very abundant, and includes many boulders, some 
occurring as blocs percMs. 
“ The common rocks of the morainic dibris are granites, gneiss, hornblende- 
schists, and others, which do not occur in situ nearer than the gorge at Normanville, 
about forty-six miles to the south. In all seventeen distinct varieties of rock, chiefly 
metamorphic, and foreign to the immediate neighbourhood, have been collected along 
the path of the glacier. _ 
“ The proximity of the Miocene escarpment suggests the possibility of the Pre- 
Miocene age of the glacier. The Miocene formation throughout its whole length on 
this part of the coast has a conglomerate base consisting of well-rounded pebbles of 
limestone and quartzite and flat pebbles of slaty rock, but none other than local 
material has been yet observed, though diligently searched for. It is highly probable 
that the glacier cut its way through the incoherent Miocene formation, and that some 
of the Miocene shingle furnished some portion of the moraine dibris. 
“ Some measure of the antiquity of the glacier is further afforded by the amount 
of marine erosion that has subsequently taken place. Assuming that the glacier was 
in an alignment with the two headlands of Ilallett’s Cove, then a length of three-fourths 
of a mile by a breadth of one and a-half furlongs, and a thickness of forty feet, has 
been removed since the glacier ceased to exist.” 
The correctness of Professor Tate’s observations has been called in question by 
Mr. Gavin Scoullar,* Professor IIutton,t Dr. Lindenfeld,J and others, but the two 
latter gentlemen, at least, have not seen the place. 
An opportunity having occurred, I visited the locality, in company with Professor 
Tate, in March, 1891. As it was my almost daily occupation for at least ten yea,rs, 
when engaged on the Geological Survey of Scotland, to map the direction of glacial 
strife, I may, without vanity, lay claim to some knowledge of the subject. I came to the 
conclusion that Professor’s Tate’s observation was correct in every particular, and, in 
addition, satisfied myself that the movement of the ice must have been from south to 
north. There are certain little niceties of observation which enable one to judge of 
the direction of the movement of an ice-sheet when piroducing polished surfaces and 
striations. Thus, for instance, in passing over a slight fissure, the sharp edge of 
solid angle formed by the planes of the surface and of the side of the fissure will be 
polished on the side furthest away from the motive force, while the edge on the other 
side of the fissure will not be interfered with. Professor Tate has never committed 
himself to an opinion on this point, although he expressed himself as satisfied with the 
* Proc. Koy. Soo. South Australia, 1884-5, p. 46. 
+ Quart. Journ. Geol. Soo., xli., p.213. 
JProc. Linn. Soo. N. S. Wales, x., p. 2. 
