med 
cirkulerer is- 
men staar i aaben Forbindelse 
det indre Ishav. I Færø-Shetland Renden 
koldt Vand, saaledes som Pilene antyde. Udenfor Norges 
Vestkyst bringer den nordgaaende og opstigende Bevægelse 
Vand af —19 Temperatur op langs Banken (Pl. XXI). 
Omkring den 70, Breddegrad gaar det varme Vand vest- 
over og nedover, idet det følger Draget fra de dybere 
Lags bariske Maximum. TI Sydvest for Beeren-Hiland, hvor 
det bariske Minimum støder op til Banken, løfter ogsaa 
koldt Vand fra Dybet sig op. Langs denne Banke og 
Spidsbergbanken gaar, i Overensstemmelse med Isobarer- 
Lige ved Banken 
fra Atlanterhavet, 
nes Retning, en varm Tunge nordover. 
suger Bevægelsen dog noget koldere Vand op langs denne. 
I Polarstrømmen gjenfinde vi de samme Hovedtræk i Tem- 
I Station No. 52 
yttrer Dybets bariske Maximum sig ved den noget højere 
Temperatur i Modsetning til No. 51 og No. 53. 
peraturen som 1 de højere liggende Lag. 
Strømmens Hastighed i 500 Favnes Dyb er gjennem- 
gaaende lidt mindre end i 300 Favne. F. Ex. ved Jan 
Mayen 0.09 m. p. S. (4 Kvm. i 24"). Udenfor Norge 
findes den samme Hastighed. 
I 1000 Favnes Dyb er Trykkets Fordeling (Pl. XL VI) 
en ganske anden end i de højere Lag. Istedetfor et cen- 
tralt Minimum have vi flere Minima og flere Maxima. 
Som ovenfor paapeget, komme de verticale Bevægelser her 
til at gjøre sig mere gjældende end 1 de højere Lag. 
I Norskedybet læner et barisk Maximum sig til den 
sydlige Rand af dette. Den deraf flydende nedadstigende 
Bevægelse giver (Pl. XXIII) et Temperatur-Maximum. 
Man vil bemerke, at 1 dette Bækken pege Gradienterne 
mod Nord. Men de ere sterkere paa Østsiden end paa 
Vestsiden. Den horizontale Bevægelse maa derfor adlyde 
de første og blive nordgaaende paa Østsiden, sydgaaende 
paa Vestsiden, østgaaende paa Sydsiden. Paa Vestsiden, 
hvor Bevægelsen gaar mod Gradienten, vil den blive ned- 
stigende. Saavel Pl. XXIII som Pl. XXV viser, at det 
er det kolde Vand fra Jan Mayen Renden, som her søger 
nedover langs Bunden. Paa Østsiden gaar Bevægelsen med 
Gradienten, kanske med Acceleration, og med Opstigning 
mod Trykkets Minimum i 68° Bredde. En sterk Opsug- 
ning fra neden af koldt Vand er Folgen, og samtidig der- 
med en Sugning af Vand langs Bækkenets Sydrand. Virk- 
ningen her er dog svagere, da Trykkets Maximum tvinger 
de højere Lag her nedad, og da Vandet i Dybet maa af- 
gives for en Del tilfFærø-Shetland-Renden. Den fulde 
Virkning af Maximumstrykket kommer imidlertid først til- 
syne midt i Bækkenet, hvor Isothermen for —1° (Tver- 
snit X, Pl. X, Station No. 52 og Pl. XXVI) naar ned 
til en betydelig Dybde. 
Paa 679 til 68° Bredde kan det kolde Vand fra Jan 
The North Ocean is entirely cut off from the Atlantic, 
but in open connection with the inner tracts of the Polar 
Sea. In the Feroe-Shetland Channel, ice-cold water eireul- 
ates, as indicated by the arrows. Off the West Coast 
of Norway, the northward-setting and ascending motion 
brings up water of —1° temperature along the bank (PI. 
XXI).° At the 70th parallel of latitude, the warm water 
passes west and downward, following, as it does so, the 
suction from the baric maximum of the deeper strata. 
South-west of Beeren-Hiland, where the barie minimum 
reaches the bank, cold water rises up from the deep. 
Along this bank and that of Spitzbergen, extends, in conform- 
ity with the direction of the isobars, a warm tongue north- 
In immediate proximity to the bank, however, the 
motion draws up along it somewhat colder water. In the 
Polar current, as regards temperature, we observe the same 
principal features as in the higher-lying strata. At Sta- 
tion No. 52, the baric maximum of the deep asserts its 
influence in the somewhat higher temperature, as opposed 
to No. 51 and No. 53. 
The velocity of the current at a depth of 500 fathoms 
is somewhat less on the whole than at a depth of 300 
fathoms: for example, off Jan Mayen 0.09 m. per sec. (4 
naut. miles in 24 hours). Off the coast of Norway, the 
same velocity is met with. 
At a depth of 1000 fathoms, the distribution of pressure 
(Pl. XLVI) is totally different from that in the higher 
strata. Instead of a central minimum, we have several 
minima and several maxima. As pointed out above, the 
vertical motions here will be more prominent than in the 
ward. 
higher strata. 
In the Norway Deep, a baric maximum leans up to 
its southern margin. The downward motion proceeding 
thence results (Pl. XXIII) in a temperature-maximum. 
It will be observed that in this basin the gradients 
point, northward. But they are steeper on the east 
side than on the west. Hence the horizontal motion 
must yield to the former, and set northward on the east 
side, southward on the west side, and eastward on the south 
On the west side, where the motion proceeds against 
the gradient, it will be downward. As well Pl. XXIII as 
Pl. XXV shows it to be the cold water from the Jan- 
Mayen Channel that here seeks a downward passage along 
the bottom. On the east side, the motion goes with the 
gradient, possibly with acceleration, and with ascension 
towards the minimum of pressure in lat. 68" N. <A strong 
suction of cold water from below is the result, and simul- 
taneously a suction of water along the southern margin of the 
basin. 
side. 
The effect here however is weaker, since the maxi- 
mum of pressure ‘forees downward the higher strata, and 
since the water of the deep must in part be given off to the 
Færoe-Shetland Channel. The full effect of the maximum- 
pressure becomes first apparent in the middle of the basin, 
where the isotherm for —1° (Transverse Section X, PI. 
X, Station 52, and Pl. XX VI) reaches down to a consider- 
able depth. 
In lat. 67° to 68° N, the cold water from the Jan- 
