RELATIONSHIPS OF THE AUSTRALIAN CAINOZOlC SYSTEM. 
tlie Muddy Creek, but it abounds in the Grange Burn, not 
onlv above but also for a long way below its junction with Muddy 
Creek.” 
In a recent visit to the Hamilton district I was able to trace 
the Cainozoic beds in succession along both creeks, and at one spot, 
about three-quarters of a mile up the Muddy Creek, from the junction 
of the Grange Burn, was fortunate enough to find a small landslip 
revealing the polyzoal rock resting on the Clifton Bank beds (Bal- 
combian), and not underlying them as Mr. Dennant supposed (Fig. 
14). This occurrence of the limestone in Muddy Creek is only 
20 chains from the well-known Clifton Bank exposure. The section 
there gives 3 feet of rubble ; foraminiferal and polyzoal limestone, 
3 feet ; brown sand (fossiliferous), 20 feet ; and blue clay. 
2 feet down to the water line of Muddy Creek. The two last- 
mentioned beds are comprised in the Balcombian or Clifton Bank 
series. 
The Cainozoic strata in the Hamilton district are not perfectly 
horizontal, as Mr. Dennant believed (see loc. cit., p. 33). and conse- 
quently their irregularity does not “ only arise from denudation.” 
In fact, were the strata perfectly horizontal, the great thickness of 
the polyzoal limestone in the Grange Burn area would present an 
insurmountable difficulty. The latest data I have collected goes 
to prove that Clifton Bank itself is on the axis of an anticline, in 
which the beds dip from 2 to 5 degrees. On the west bank of the 
Grange Burn, opposite Hentv’s, there are high cliffs of Lepidocyclina 
limestone surmounted by Kalimnan beds, that is, an oyster bed 
w. E . 
Fid. 1 5. Lir^eSTortE SCARP OMqRwqt BURN AT HEnty’s, Area, of 
Axdr'ioiu FAouTmq. 
with Natica cunning hamensis . This elevated position of the middle 
series shows that the cliff at this spot represents a fault scarp ; and 
further, that the western bank of Grange Burn at Henty s has been 
uplifted for at least 40 feet (Fig. 15). Moreover, the Grange Burn 
[ 43 ] 
