THE TRANSITION SERIES. 49 



westwards towards Kirkambadi. The great eastward break must run 

 north-north-west from Yarapet to about the parallel of Kossi Konda, when 

 it turns more northerly and continues still faulted, for it is running' at 

 a good angle across the well* marked strike of the beds to the parallel 

 of Nagwaram hill. Hence, but now with the strike, there must still be 

 a faulted line running north-by- west to the parallel of Rapu*r, there 

 being too narrow a space between the quartzites and the gneiss to allow 

 of any sudden thinning out of such a thick series of rocks as is displayed 

 in the sections to the westward. At Rapur there is a wide and very 

 abrupt abutment of the ends of the transition strata against the gneiss 

 at right angles to the more general lines of fracture, on either side of 

 which the older "and newer series approach very closely. From the same 

 town, the boundary again runs north-north-west, but not always with 

 the straightness assumed, to be peculiar to a faulted edge, up to the 

 Penner. Northwards from this river, the boundary is more curved, the 

 gneiss and quartzites still, however, running so close that a natural 

 boundary seems out of the question, and this is only more clearly indi- 

 cated by the features already described in the account of the outliers to 

 the east of this part of the range. 



The rocks of the Veligondas have been described in the memoir on 

 The rocks of the Veli- ^ ne Cuddapah formation, and as they are of little 

 s° udas - interest penological ly, being merely recurring and 



succeeding, from south to north, bands of quartzites and slates, it would 

 be mere repetition to refer at greater length to them in this paper than 

 has been already done. The quartzites are everywhere seen to be true 

 sedimentary beds, great spreads of rippled sandstones being frequent all 

 over this range, and their sandstone or conglomeratic character, if not 

 seen at once, as is often the case in the wonderfully compact and dense 

 rocks, is soon evident where they are weathered. The clayey beds, on 

 the other hand, have assumed more of a schistose character than is usual 

 in the rest of the Cuddapah area, strong bands of rusty-brown and dark- 

 green talcose and chloritic schists being common in the portion of the 

 range south of Rapur, which are traceable to the westward into easy- 

 d ( 157 ) 



