384 PROCEEDINGS OF SECTION C. 



glaciated aspect as well as others." This is probably due to their 

 having been subjected to more exposure and attrition in the course 

 of re-deposition. 



And their fouith reason, "the total want of arrangement" of 

 these stones, is precisely what mij^ht have been expected from the 

 manner in which they have reached, as we conceive, their present 

 position. 



There are also, as has been pointed out, the stratified Miocene 

 leaf-beds which overlie the stratified sandstones and intercalated 

 beds, but we have not found them reposing on this unstratified 

 material nor this material on them. Moreover, this material, in 

 any position, is really of only occasional occurrence, and, except 

 in a very few instances, of small extent and superficial depth, and 

 in these places it is fully accounted for. 



Reference is made in the same paper to the " rounded 

 htimmocky-loolving masses of sandstones" to be seen nearly 

 opposite the 100ft. section, the appearance of which was considered 

 suggestive of glacial action ; so we thought when first we saw 

 them from a distance, but found on examination they were only 

 suggestive. They state, " it is very probable that the glacial 

 conglomerate not long since covered these rocks and thus pro- 

 tected them during a long period from the effects of weathering." 

 They also say, " the sandstone is just the kind of roclc on which 

 the abrading and rounding effect of glacial ice would be well 

 represented." " Certainly," they observe, " strife and grooves are 

 absent." There is, however, no evidence that these small hillocks, 

 lying, as they do, at but small elevations above the present creek, 

 are anything more than isolated patches of the stratified rocks, 

 avoided by the creek and subsequently denuded into rounded form, 

 and they are of such matei'ial that they would not retain any 

 impression or even general outline, except a rounded one, for any 

 length of time. 



In the Werribee Gorge sections of rocks are seen from 200ft. to 

 300rt., 400ft. and 500ft. high, and some of the clifFs present faces 

 over 100ft. in vertical height. Mr. Dunn calculated the deposit 

 seen by him at about 100ft. in thickness. He referred to the con- 

 glomerates, probably, but in this locality the conglomerates and 

 intercalated beds attain a continuous section of 500ft. in height. 

 This has proved to the wi'iters of the paper in question " the 

 existence of a Triassic sea or lake." 



Here we are quite at one with Messrs. Officer and Balfour, but, in 

 our opinion, the loliole of the rocks were laid down under water. 

 They also consider " that the overlying sandstones are continuous 

 with the surrounding ones." In this latter observation they are 

 again undoubtedly correct. As has been before remarked, the mud- 

 stones, conglomerates, and sandstones alternate with each other in 

 repeated succession — now in thick beds, now in thin beds, now 

 highly laminated, then for short distances disturbed and distorted. 



