:230 Charles Fenver : 



tiaries or glacial deposits occur north of the scarp line in this part 

 of the State, but such are found quite common (many of them un- 

 mapped) to the south of that line. The down-throw of the fault 

 in its western part has probably been much less than at Greendale. 

 Here, too, the fault passes away into the upper Moorabool area, 

 and as the writer found it necessary to restrict detailed work to 

 the prescribed area, further work tO' the west of Egan's Hill was not 

 •done. 



In many places remarkably coarse conglomerates and gravels, 

 40-60 feet in depth, are piled up close against the scarp, notably 

 so at Garibaldi Hill and Shuter's Hill, Greendale. They are much 

 more dissected than the alluvial apron which lies along the base 

 of the Rowsley scarp, and point to the greater age of the Green- 

 dale scarp. They are no doubt relics of the early deposits along 

 the steep scarp face. The two deposits specially referred to sug- 

 gest '* fan deltas " in their shape, and in the extreme coarseness of 

 the boulders close to the scarp. 



Eastward from Shuter's Hill, the lower side of the scarp is of 

 Ordovician slates similar to those of the higher block, but there is 

 still a marked difference between the physiography above and 

 below the " fault line." Blocks of fault conglomerate are strewn 

 •on the slopes here, and the wide valleys below the fault grade into 

 the steeper-sided ones to the north. They remain, however, suffi- 

 ciently distinct to enable the line to be followed. 



Coming to Mt. Blackwood, we find that dominant hill to be a 

 •cinder cone perched on the uplifted block., near the edge; the con- 

 tour of the flow proves that the valley down which it ran had a 

 much steeper grade near the base of the hill, so that practically the 

 whole of the lava flow ran down and debouched over the plain, that 

 which remained above being mainly scoria. The exact line of 

 the fault is here less clearly defined, but it is assumed that the re- 

 markably steep descent of about 400 feet, shown in the present 

 contour of the lava flow (Fig. 21), marks the point where the fault 

 line crosses this area. Beyond this, we find the fault more 

 clearly defined, stratigraphically, and trending south-east. It 

 follows and then crosses the Korkuperrimul Creek, and we have 

 once more glacial, older volcanic, and tertiaries at a much lower 

 level than the Ordovician; where noted in the field the junction 

 was abrupt and almost straight. David (ref. 13) refers to great 

 differences (nearly 800 feet) in the levels of the known glacial pave- 

 ments here. It is accepted that the glaciers moved northwards, 

 about 12° E., and yet the Professor mentions that the base of the 



