IÇO IKIDIJOI' NAN.SKN. M.-N. Kl. 



for as an effect of tlie frost action, in a similar way as th • fact tliat the 

 rocks of the shore-lerlj^'es cut in solid rock are also shariJ-erlj:(ed, with very 

 few traces of wave-erosion. .Some stones have obviously also fallen down 

 on these ledj^es after tliey were raised ahoxc sea-level. 



It is striking;- that these led^a's, wherever I have observed them, 

 always occurred at the foot of very steep mountain sides, where stones 

 may be expected to liaxc been perpetually falling;, especially when the 

 shore erosion worked at the foot of the mountain. The probability is. 

 how-ever, that the inner part of these ledt^es are more or less cut in .solid 

 rock, but this is often difficult to examine, as their inner margin is 

 generally covered ])\ a talus (scree). 



I had no opportunitx' of measuring tlie heiglit of these stone-ledges 

 on Prince Charles Forelanrl, but estimate it to be about 50 metres above 

 sea-level. 



At the foot of the ledges accumulations of snow are now eroding 

 small cir(|ues in their steep slope, oversteepening them (cf. Fig. 140). 



Along a part of the east coast of Prince Charles Foreland, from 

 J. IVIurray Point southwards, the strandfiat is now covered by flat gla- 

 ciers, Murray Glacier and Buchanan Glaciers (Fig. 9 and 10). The rocks 

 of the strandfiat project in several places along the outer edge of the 

 glacier. I agree with Hoel, that the strandfiat was obviously formed 

 during periods wdien the glaciers had less extent than at present. They 

 have afterwards extended over this flat plane, and form a nearly hori- 

 zontal ice-sheet, to some small extent fed by the small glaciers of the 

 mountain slopes behind. 



The glaciers to the south, Geikie Glaciers, form thin sheets extending 

 from the mountain slopes over the undulating lower land (Fig. 137). 



The strandfiat of Prince Charles Foreland is continued outside the 

 shore in a siihiiicrgcd strand flat (see Fig. 133) the contours of wdiich 

 may be approximately traced along the east coast by the soundings of the 

 Isachsen Expeditions of 1909— 1910 in the Foreland Sound [cf. Isachsen, 

 19 1 2, chart], and along the west coast by the soundings taken by the 

 Hoel Expeditions in the years 19 13 to 1921. By Hoel's kind permission 

 I have been able to study the detailed charts with these soundings. In the 

 map Figs. 133 & 134 is drawn the isobath for 30 metres below sea-level. 

 The edge of the submerged strand flat seems to be very near this isobath 

 at depths between 20 and 30 metres or often near 20 metres. In some 

 places the edge seems to be quite sharply defined, whilst in other places 

 the side slope of the submerged plateau is more gentle, making the edge 

 less distinctly marked. 



Along the northern part of the west coast of the island, north of 

 Cape Cold, the submerged strandfiat is mostly about 2 kilometres broad, 

 the width decreasing north of Cape Cold to about i kilometre. Off Cape 



