REPORTS OF COMMITTEES. 275 



by tlie Crassatella and Turritdla beds of Eocene age. The junction 

 line is a slightly eroded one, and there must be also a slight uncon- 

 formity, as whereas the Eocene beds are almost horizontal, the Permo- 

 Carboniferous glacial beds dip in a general W.N.W. to N.W. direction, 

 at an angle of about from 5° to 10°. 



At a point about three miles to the E.S.E. of the mouth of the 

 Inglis Kiver the glacial beds disappear under a flow of Tertiary basalt, 

 which descends to below the level of low tide. The flow just here is 

 only about 200 metres in width, where it has filled up an old Tertiary 

 river valley. On the E.S.E. side of the flow no trace is seen of the 

 glacial beds, but in their place, occup}ang the foreshore of the coast 

 platform, are dark grey to black schistose slaty rocks, and felspathic 

 quartzites. (The latter strike from N. to N. 5° E., dipping E. at 60° 

 to 70°.) 



It is evident [from this section] that the old Tertiary river valley, 

 now filled with drift and basalt, was eroded just along the junction 

 line of the older Palaeozoic rocks with the glacial beds of the Permo- 

 Carboniferous system. 



The Permo-Carboniferous basal glacial beds are extremely hard, 

 and have a gentle angle of dip on the whole, whereas the strata of the 

 Ordovician series are much softer, and being steeply inchned, as above 

 stated, at angles of 60° to 70°, are very readily eroded. 



The existence here of this basalt-filled Tertiary valley extending 

 to below sea-leve] makes it impossible to see just here the actual pave- 

 ment on which the glacial beds rest. There can be no doubt whatever, 

 in view of the evidence in Victoria and South Australia, that such a 

 pavement when found further inland will prove to be strongly striated 

 and grooved. As will be shown presently, fortunately, striated pave- 

 ments are to be seen occasionally in the glacial beds themselves, which 

 pavements show the direction of movement of the glacier ice. 



It ^\^ll be seen from the accompanying section, taken through the 

 glacial beds between the Inglis River and the base of the formation, 

 three miles to the E.S.E.. that the glacial beds consist of at least four 

 distinct types of rock, viz. : — 



(1) The glacial till, resembling the boulder clays of late Cainozoic 



age of the Northern Hemisphere. 



(2) Conglomerates, frequently containing erratics and striated 



boulders. 



(3) Sandstones, with occasional — but rare — striated boulders. 



(4) Thin-bedded, often minutely lamellated, clay shales with inter- 



calated thin flaggy sandstones, and occasionally thin bands, 

 lin. to 2in. only, of boulder clay. The flaggy sandstones 

 and mudstones are in many cases beautifully ripple-marked. 



The following is a general description of the boulder clay proper, 

 which is very well developed immediately to the south of the entrance 

 to the Inglis River. 



The base of the boulder clay is a dark grey mudstone ; no very 

 definite stratification is visible, but there is a faint indication there of 



