250 KRIirrjOF NANSEN. M.-X. Kl. 



I lie 1,'iinl lias consdnuiillx nol Ixcii ilcjdcsscl 'luriiij^ llic last j^lacial 

 period in lliis coastal /one, 25 l:iloin(tres broad, in the region of Nord 

 J'\ioi-d, i'.rcnian,L;cr, and Stat, altliou^li ilic-re has been a postglacial change 

 of \() to \y nutres in tlie le\cl of the shore-line. The depression has onlv 

 occurred in tlie re.^ion inside Ku^sund, whence the njjper limit of sub- 

 nierf^ence sudden!}- begins to rise inland, as is clearlv rlenioiistrated by 

 Kaldhol's profile. 



The gradient of elevation is 1.20 jjer nulle betuen Rugsunrl t.Stroni- 

 nien, height =■• 18.2 metres) and Eikenes in Hyen Fjord (height = 61.2 

 metres), a distance of about 35.7 kilometres if measured at right angles 

 to the direction of the isobases (if we take .Strommen in Hyen Fjord, 

 height 59 metres, the distance is 33 kilometres and the gradient 1.24, 

 cf. J^'ig. 1^5) — while it is on the average 2.00 per mille in the inner 32 

 kilometres of the fjord, between Hyen Fjord (Eikenes) and Tndvik in 

 Indvik l^^jord (height = 125.3 metres), provided that Kaldhol's deter- 

 minations of the upper limit are correct in this region. They give gradients 

 which vary much in value. Between Lote (71.7 metres, see Fig. 165) and 

 Henne (95.7 metres, see Fig. 165), a distance of 6.7 kilometres, his values 

 give a gradient even of 3.6 per mille. It seems to me to be probable that 

 the highest terraces, found by Kaldho! in this region of the fjord, are 

 not marine. 



We may, however, expect some irregularities here, as the region of 

 Nord Fjord is perhaps the most prominent centre of seismic activity along 

 the Norwegian coast [cf. Kolderup, 1914, map p. iiij. 



In the innermost region e^f Nord Fjord, inside Indvik, in Stryn. 

 Olden, and Loen, Kaldhol's measurements of tlie heights of the highest 

 terraces give suddenly much lower values than in the region west of Ind- 

 vik. The explanation may he either that the formation of terraces was 

 prevented by glaciers filling the valleys and innermost parts of the fjords 

 during the time of the deepest submergence of the land, or, as suggested 

 by Kaldhol, that a later advance of the glaciers has destroyed the highest 

 terraces in that region. 



Kaldhol's detailed investigations of the lateglacial and postglacial 

 terraces in the region of Nord Fjord give most valuable information 

 about the suljmergence and emergence of the land during this period, and 

 his height measurements support, as we have seen above, the correctness 

 of my view of the relation between the horizontal level of the strandfiat — 

 indicating the level of the shore-line before the last great submergence — 

 and the tilted planes of the raised terraces and beaches — indicating the 

 submergence and the upheaval of the land. 



There is unfortunately no other region of our coast, which has been 

 subjected to similarly detailed investigations, as far as I am aware, at 

 least not in the outer coastal region. But several scattered observations 

 in various localities indicate that along those parts of the outer coast. 



