REPORTS OF COMMITTEES. 277 



casts of Pentamerus, Crinoids, and Rhynchonella. Rarely blocks of 

 reddish limestone are met with exhibiting similar fossils. Mr. W. H. 

 Twelvetrees informs me that similar rocks of Upper Silurian age occur 

 at Heazlewood and Zeehan. 



The above are the only fossiliferous rocks observed by me in the 

 boulder beds. A greenish-brown felspathic quartzite is extremely 

 common, and is almost invariably intensely glaciated. A fine-grained, 

 reddish-brown quartzite exhibits strise well, but is less often grooved. 

 Hard, dark-grey quartzites and whitish quartzites weathering ocherous 

 are not uncommon. White marble occurs sparingly ; one block, shown 

 on the longitudinal section and in the photograph, measures about 

 5ft. X 4ft. X 4ft. Occasional boulders may be noticed of a tough quartz- 

 grit, as well as of a curious quartzite (?) with red orthoclase, and of a 

 dark greenish conglomerate, which Mr. Twelvetrees compares with the 

 conglomerates of the Dial Range. 



Ancient crystalline schists and gneiss — a red orthoclase gneiss — 

 are met with here and there, but the metamorphic crystallines are not 

 so much in evidence as the sedimentary rocks just described, and the 

 eruptives about to be described. The latter are represented by con- 

 spicuous blocks of red granite, often rendered porphyritic by ortho- 

 clase ; these are frequently in blocks from Gin. to 2ft., or even 3ft. long. 



Granite-porphyry and orthoclase-porphyry, with veins of tourma- 

 line and pseudomorphs in tourmaline after orthoclase, are less frequent 

 but fairly numerous. A few boulders of serpentine, usually in small 

 fragments, but in some cases 18in. long, are to be seen at wide intervals. 

 Mr. Twelvetrees considers that this serpentine resembles some of those 

 which occur in situ near the township of Forth and at the Bald Hill, 

 Heazlewood. 



With regard to the probable parentage of these rocks, Mr. Twelve- 

 trees has kindly supplied me with the information contained in the 

 note at the end of this report. 



As a rule striated pavements were not observed in the boulder 

 clay, where it was of considerable thickness ; such striated pavements 

 as were noticed appeared to be restricted to thin patches of boulder 

 clay interbedded with conglomerate. As shown in the Section, three 

 such striated pavements were observed by me. 



1. As shown in the Section, the trend of the grooves and strise on 

 these pavements in the boulder clay varies from N. 30° to 35° E. to about 

 N. 20° E. In most cases the grooving and striation is about N. 30° E., 

 that direction being the lee side, so that the ice in this locality evidently 

 moved from about S. 30° W. towards N. 30° E. The lie of the longest 

 axes of the large boulders agrees fairly well with the same direction. 



2. As regards the evidence of the locale of the parent rocks of the 

 boulders in the clay, Mr. Twelvetrees considers that their parent rocks 

 may be to the S., the S.S.W., or the S.S.E. At all events there is 

 nothing in this part of the evidence inconsistent with the view that 

 the ice which caused the glaciation moved from a general S.S.W. or 

 S. 30° W. direction. 



