has led to a concentration of its stony contents. It consists 

 of two main beds : — 



(a) An upper bed of loosely-cemented sand 22 ft. 



(b) A lower bed of stony clay (till) ... 78 ft. 

 The upper bed (a) might be classed as a sand-rock — 



argillaceous in part and of various colours — white, yellow, 

 and red. Usually, it is either a dark-red colour or mottled 

 arising from the presence of iron oxides, which by segrega- 

 tion has led to the formation of ferruginously-cemented 

 sands, either in layers or local segregations — a very common 

 feature of the glacial sandstones and conglomerates of this 

 period as they occur to-day in South Australia. The bed 

 contains a few stones of small size, and these are usually 

 more or less water-worn. Infiltration has led to the forma- 

 tion of a great number of stalactitic pipes in the upper part 

 of the bed, probably following the occurrence of roots and 

 other organic matter in the subsoil. 



The wind and rain have deeply eroded this bed, which 

 forms the cap of the moraine. Some parts have been ex- 

 cavated to the level of the underlying clay, and there are 

 outliers of the same material scattered over the summit, with 

 glacial clay exposed between them (plate xii.). At the land- 

 ward end, where the moraine gently rises to higher ground, 

 there is a continuous cliff of the sand-rock, 20 ft. in height. 

 Here the bed gives some slight indications of being stratified. 

 It is possible that this upper member of the section had its 

 origin in the redistribution of morainic material, under the 

 action of water, at a period subsequent to the ice-flood. On 

 the other hand, this bed closely resembles the glacial sand- 

 stones which occur interstratified with glacial clays in other 

 parts of South Australia. If it were of contemporary date 

 with this particular glacial period, it certainly suggests 

 altered conditions from those which prevailed during the 

 deposition of the underlying boulder clays. The power of 

 vigorous transport had ceased, and only fine material could, as 

 a rule, undergo carriage. It may represent a late stage of 

 the glacial period when, along the face of the retreating ice- 

 sheet, water became the chief agent of deposition. 



The lower bed (h) exhibits the features of a typical 

 glacial till or boulder clay. The clay generally carries a 

 certain proportion of sand and is very stony, the stones 

 ranging from the size of pebbles to many feet in diameter. 

 The summit of the moraine is nearly flat, except for the 

 unevenness which is the result of erosion. Where the surface 

 has been worn down to the underlying clay bed an extra- 

 ordinary assemblage of large and small boulders strew the 



