32 



FRI DI JOK NANSK.N. 



M.-N. Kl. 



Fig. 13. Ice-foot' (shore-ice) formed above the upper fucus-hmit, and above 

 the average sea-level, at Holstensborg, Greenland. [K.J. V. Stcenstrup, 1907.] 



(luring- a great deal of tlie time, till the sea is opened, and fogs l.ecome 

 frequent. 



The result is that the rocks are rapidly disintegrated and crumble 

 to pieces. 



The tide may also be of importance by alternately submerging some 

 part of the shore twice every day and night, even during the cold winter. 

 This may cause alternate melting and freezing of the water in the fissures 

 and depressions of the rocks, wherever the shore is not covered bv more 

 permanent layers of ice. Thus an active disintegration of the shore rocks 

 may be produced even by the sea-water. 



During the time of the year when the sea is more or less open, the 

 wave action will wash away from the shore the debris formed by the frost 

 disintegration. This is of the greatest importance for the continued shore 

 erosion by frost. The waves and the tide may also break loose the ice 

 formed on the beach, and may carry it away with the débris, accumulated 

 on its surface from the cliffs above. 



The ice formed at low water, on small water pools left by the tide 

 on the beach, may also be of some importance in this respect. Mineral 

 particles and small stones enclosed in this ice, mav be carried along with 

 it when the tide rises [cf. O. E. Schiøtz, 1894]. The waves may help to 

 break the ice loose, and thus the shore erosion may be increased. 



The socalled 'ice foot', or thick layer of solid ice, formed along Arctic 

 shores during the winter, may also carry along with it enclosed stones, 

 or stones and débris fallen from the cliff on to its surface, where it is 

 broken loose in the spring or summer [cf. Knutsen, 1889, p. 249]. But 

 according to my observations, this transport by the Mce foot' is less than 

 might l)e expected, because on the one hand, a great deal of the 'ice foot' 

 lies above the average high-tide level, and melts gradually in situ, without 

 being carried awav l)v the sea, and on the other hand, the ice on the lower 



