I 



I92I. X(>. II. THE STRANDFl.AT AND ISÛSTASV. 1 23 



exaggerated in relation to thj horizontal scale. The pro.ile in black on the mainland i;!ves the natural relation 

 and length. 



many i)laces. for instance in tlie region of Kvenvær. as Scheteligf has 

 j)ointcd out to me. 



y ig. 112 is a photOL^rapli of the mountain Tonningen (231 metres 

 above sea-level) in the western granite region of Hitteren, taken bv Prof. 

 J. Schetelig. It demonstrates the abruptness with which the mountains 

 rise with tlieir steep sides above the denudation plane of the strandfiat. 

 This plane as well as the mountain is formerl of the same granite and tliere 

 is no flifference in the geological structure to account for the configuration. 

 Forms like these cannot therefore be formed solely by subaërial denudation, 

 which would necessarily give to the mountains bounding the plane less 

 abruptl}' ascending sides. They might be formed l)y glacial erosion, and 

 the ridges of the surface of this strandfiat have obviouslv been rounded 

 by glacial erosion, as Fig. 112 shows. But if this glacial erosion had lasted 

 long enough to produce mountain forms like Tonningen, the strandfiat 

 would necessarily have been deeplv dissected into a much more uneven 

 surface than we now find. The only natural explanation is that before 

 the last glacial erosion (of the last glacial epoch) the marine denudation 

 finally planed the surface of the strandfiat which rises gently from the 

 shore to the foot of the mountain slope probably at about 30 metres 

 above sea-level. 



Between the western granitic mountain area and the more extensive 

 dioritic mountainous region to the east, a broad and flat plain extends 

 across the island from the south ccjast to the northwest coast, forming a 

 continuation of the strandfiat, rising gently to somewhat more than 60 

 metres above the sea, but its greater part, especially in its northern and 

 northwestern area is less than 50 metres high. According to kind in- 

 formation from Schetelig, this low region is built up of crystalline schists, 

 mica-schists, and hornblende-schists which have been more easilv denuded 

 than the granite to the west and the more resistant diorite to the east. 



The strandfiat continues along the northern coast of Hitteren, formed 

 of pressed igneous rocks, gneisses, and some granite and amphibolite, &c. 

 The plane is well developed at heights of l)etween 20 anrl 35 metres above 

 the sea with some few hills rising to about 50 metres. The long Dolm 

 Island to the north is also a continuation of the low strandfiat with two 

 isolated hills rising to 46 metres (Storvarden) and 70 metres (Hjertås) 

 above the sea. 



