der sig store ,Bleker” og Opkommer af Vand til visse 
Tider, naar den store Flodbølge passerer gjennem denne 
Rende mod Nordost. Bergarter fra Ryggen ere, i Smaa- 
stykker, meget talrigere og større i det iskolde end i det 
varme Strøg, og de pege saaledes paa den Retning, i hvil- 
ken Strømningerne feje Bunden. De større Stene ligne 
Bergarterne fra Orkenøerne*. 
Langs Norges Kystbanker tør Hastigheden af Strøm- 
men i 300 Favnes Dyb gaa op til 0.12 m. p. S. (5 a 6 
Kvm. i 24"), i Polarstrømmen ved Jan Mayen til 0.16 m. 
p. S. (7 å 8 Kvm.), under Grønland til 0.08 m. p. S. (4å 
5 Kvm.). I den centrale Del ere Hastighederne meget 
ringe. 
Efter at have studeret Bevægelserne i 300 Favnes Dyb 
kunne vi nu med fuldere Forstaaelse gaa over til at betragte 
Bevægelserne i de Dybder, der ligge mellem denne Niveau- 
flade og Overfladen. 
TI de øverste Vandlag fylder Strømmen fra Atlanter- 
havet nordenom Skotland Nordsøen. Den bringer det salte 
Vand fra Oceanet ind over Nordsøens Flak (Pl. XXXV) 
og fylder den norske Rendes Dyb* med ægte salt Atlanter- 
havsvand. I den sydlige Del af Nordsøen er Vandet mere 
opspædet af Elvene, navnlig i de øvre Lag. 
I 100 Favnes Dyb (Pl. XVII) se vi Virkningen af 
Strøm 
I Færø-Shetland Renden suges aaben- 
den nordgaaende varme langs Nordsobanken og 
Norges Kystbanker. 
bart Vand langs den nordre Bred sydover fra det norske 
Hav. 
gjældende. 
koldere Vand imellem begge. 
Langs Norges Banker gjør endnu Landkulden sig 
Varmetungerne ligge løsrevne fra Banken med 
I Østhavet driver Strømmen varmt Vand ind til om- 
trent Midten af Havet i 100 Favnes Dyb. I dets østlige 
og nordlige Del formaa Vindene og Tæthederne ikke at 
føre Vandmassen i dens hele Mægtighed med. Bunden er 
dækket af iskoldt Vand fra Havets nordlige Del. Dette 
Vands øvre Lag rives med af Overfladestrømmen, og maa 
erstattes af Vand, der langs Bunden finder sin Vej norden- 
fra, fra Eene. hvor Havets Vand altid har en lav Tempe- 
ratur gjennem hele sin Dybde. 
Den kolde Storfjord paa Spidsbergen sender koldt 
i den Indbugtning, som Banken har østenfor 
Paa Vest-Spidsbergens Banker se vi i 100 Fav- 
Vand ned 
Sydkap. 
nes Dyb Landkuldens Virkning. 
I den grønlandske Polarstrøm gjenfinde vi den afkjø- 
lende Virkning af Dybets Trykminimum under 73°—74° 
Bredde og Strømningerne omkring Jan Mayens Banke. 
@ 
1 Pommerania Expeditionen 1872. 
to the north-east. Over the ridge large smooths and wellings 
up of water take place at certain times as the great tidal wave 
passes through this channel into the North Sea. Mineral 
particles from the ridge are much more numerous and larger 
in the cold than in the warm area, thus indicating the di- 
rection in which the currents sweep. The stones resemble 
those of the Orkneys.” 
Along the coast banks of Norway, the velocity of the 
current at a depth of 300 fathoms may reach 0.12 m. per 
sec. (5 or 6 naut. miles in 24 hours); the velocity of the Polar 
current off Jan Mayen, 0.16 m. per sec. (7 or 8 naut. miles), 
off the coast of Greenland 0.08 m. per sec. (4 or 5 naut. 
miles). In the central part the velocities are very trifling. 
Heaving investigated the motion at a depth of 300 
fathoms, we can now with fuller comprehension pass on 
to consider those in the depths between that level and. 
the surface. 
In the upper strata, the current from the Atlantic 
north of Scotland fills the North Sea. It brings with it 
the salt water from that ocean over the flat of the North 
Sea (Pl. XX XV), and fills the deep of the Norwegian Chan- 
nel! with genuine salt Atlantic water. In the south part 
of the North Sea, the water is more diluted with the 
outflow of the rivers, more especially throughout the upper 
strata, 
At a depth of 100 fathoms (Pl. XVII), we see the 
effect of the warm current setting north along the North- 
Sea bank and the Coast Banks of Norway. In the Færoe- 
Shetland Channel, water is manifestly drawn south by suc- 
tion along the northern margin from the Norwegian Sea. 
Along the Norwegian banks, the land-cold still asserts its 
influence: the tongues of heat lie quite isolated from the 
bank, with colder water intervening. 
In the Barents Sea the current forces in the warm 
water to well-nigh the middle of that tract of ocean, at 
the depth of 100 fathoms. In its eastern and northern 
parts, the winds and the densities combined are unable to 
carry along the water in its entire depth. The bottom is 
covered with ice-cold, water from the northern part of the 
sea. The upper stratum of this water is carried along 
with the surface-current, and has to be compensated by 
water which finds along the bottom its way southward 
from regions where the water of the sea has always a low 
temperature throughout its entire depth. 
The Storfjord, Spitzbergen, its cold 
water into the recess which the bank exhibits east of 
South Cape. On the banks of West Spitzbergen, we 
perceive at a depth of 100 fathoms the effect of the 
land-cold. 
sends down 
In the Greenland Polar current, we again fall in with 
the cooling influence resulting from the pressure-minimum 
of the deep in-lat. 73°—74° N and the currents flowing. 
round the banks of Jan Mayen. 
1 The Pommerania Expedition 1872. 
