32 FRIDTJOF NANSEN. M.-N. Kl. 



a temperature of 0,32 ° C, and at 130 metres near the foot of the 

 glacier the temperature of the sea- water was 1.05° C. These observations 

 demonstrate clearly, how very little cooling effect the glacier ice has 

 upon the sea- water. If this effect had been appreciable, it was to be ex- 

 pected that the heavy water created by the cooling would have accu- 

 mulated at the bottom of the glacier; but on the contrary we find here 

 a comparatively high temperature, even higher than at the same level 

 farther out in the fjord. The salinity, 34.76 '^Iqq, seems to be the same 

 as would be found in the corresponding water-layer with a similar tempe- 

 rature farther out in the fjord; but at Station 14 this water-layer was 

 situated somewhat deeper. A temperature of 1.12° C. and a salinity of 

 34.80 °/oo were there observed at 200 metres, and only a short distance 

 above this level both temperature and salinity must have been approxim- 

 ately the same as at 130 metres at Stat. 13. At Stat. 16 on the edge of 

 the shelf, far outside the fjord, 1.07° C. and 34.74*^/00 were observed at 

 90 metres. This is evidentl}' the corresponding layer. At Stat. 12, on the 

 shelf farther south, two days before, this layer must have been situated 

 much deeper, somewhere between 200 and 240 metres. 



These observations show that there is much difference in the levels 

 of this and other layers in this region. On the other hand the obser- 

 vations indicate a fairl}' active horizontal circulation between the water- 

 layers of Cross Bay and those on the shelf outside; and in the inner end 

 of the fjord the deep water-layers are somewhat lifted along the rising 

 bottom towards the Lilliehöök Glacier. 



The surface observations at our Station 13 are also noteworthy. 

 Although a great quantity of pieces of ice, fallen down from the glacier, 

 were floating about in all directions on the sea-surface, the surface-tem- 

 perature was 0.3'' C, and what is still more remarkable, the salinity was 

 unusually high, 34.20 °'oo- At Station 14 farther out in the fjord, the 

 surface-salinity was 33.71 %o, and at Station 15 it was 32.75 %o ^^''th ^ 

 temperature of 2.5° C. The salinity of the surface-water thus rapidly 

 increased towards the inner end of the fjord and towards the glacier, 

 which is contrary to what it ought to be, if much ice were melting there. 

 It proves that the glacier-ice cannot melt very rapidly at the inner end of 

 the fjord; while there are better conditions for melting farther out where 

 the temperature of the surface-layers is higher, and where the low surface- 

 salinity may also be due to the waters with lower salinities carried in by 

 the horizontal circulation from the surface-layers outside (cf. Stat. 15, Fig. 12). 



The waters with comparatively high salinities at the inner end of the 

 fjord, must be remnants from the spring and winter when much ice was 



