Vinde. Saaledes er Tilfældet ved Norges og Grønlands 
Kyster, saaledes ogsaa ved Islands Sydkyst, Vestkyst og 
Østkyst. Paa Islands Nordkyst ligge Forholdene anderledes. 
Havet mellem Nord-Island og Grønland er ikke varmt nok 
eller bredt nok til at fremkalde en Lufttrykseenkning mellem 
begge Lande. Island kommer derfor til at træde frem 
som et fremskudt Udenverk foran det grønlandske Continent 
og slutte sig til dettes Lufttryksmaximum (Pl. XXXI). 
De herskende Vinde paa Nordkysten af Island blive østlige. 
Men paa denne Kyst er det, at alle Islands største Bræ- 
elve udmunde i Havet. Her hæve de Vandspejlet og frem- 
bringe en Heldning mod Nord 1 dette, som Tæthedsfladen 
viser (Pl. XLIT). Den Heldning mod Syd, som de her- 
skende østlige Vinde give Vindfladen, mere end opvejes af 
Tæthedsfladens Heldning i modsat Retning. Stromfladen 
faar en Heldning mod Nord, og Strømmen løber mod Øst 
tvertimod de herskende Vinde. Den ostgaaende Strom 
vedligeholder Continuiteten mellem Vestkystens nordgaaende 
og Østkystens sydgaaende Strøm. Mellem Island og Gron- 
land bliver der en Indsænkning i Strømfladen, der danner 
Grændsen mellem Polarstrømmen og den atlantiske Strom. 
Den første løber, efter Kartet, med en Fart af 5 å 6 Kvm. 
(0.12 m) til 14 Kym. (0.3 m); den sidste med en Fart af 
4 Kvm. (0.1 m). 
Udenfor Islands Østkyst gaar Strømmen. paa Yder- 
siden, i Følge med den fra Polarstrømmen kommende Arm, 
mod Syd med en Fart af 14 Kvm. (0.8 m). Sondenfor 
den 65. Breddegrad svinger den mod Sydost og Øst ind 1 
det norske Hav paa venstre Fløj af den directe Atlanter- 
havsstrom. 
Man legge Isothermkartet, Pl. X VI, paa Stromkartet, 
Pl. XLITT, og man vil med et Øjekast se Aarsagen til Iso- 
thermernes Tungeform. 
fl. Strømningerne i Dybet. 
Til Vejledning for Studiet af Vandets Bevægelse i 
Havets Dyb undersøger jeg først, hvorledes de af Tæt- 
hederne og Overfladens Form afhængige statiske Tryk ere 
fordelte i Niveaufladerne i forskjellige Dybder. Det er 
den samme Methode, som man benytter i Meteorologien, 
naar man construerer Isobar-Karter. 
a, S(1 + b H) 
1— np : 
beregnes Trykket i et Punkt i en Niveauflade, hvis Dybde 
under den normale Havflade under 45° Bredde er H Favne. 
Adderer man hertil Strømfladens verticale Coordinat for 
samme Punkt, udtrykt i Atmosfære-Tryk, faar man det 
statiske Tryk i Punktet i Niveaufladen. 
Efter Formelen 5 Jat 
I= 
171 
at the coast; and both of these causes produce together 
a current in the direction of the prevailing winds. Such 
is the case off the coasts of Norway and Greenland, 
likewise, too, along the south, and east coasts 
of Iceland. On the north coast of Iceland, the condi- 
tions are different. The sea between North Iceland 
and Greenland is neither warm enough nor broad enough 
to produce a barometric depression between the two 
countries. Hence, Iceland stands as an advanced outwork 
in front of the continent of Greenland, bounding off the 
high pressure of that country (Pl XXXI). The pre- 
vailing winds on the north coast of Iceland are easterly. 
But on this coast it is that all the largest glacier-rivers 
of Iceland disembogue. Here they raise the level of the 
sea, and thus produce an inclination towards the north, as 
shown by the surface of density (Pl. XLII). The inclina- 
tion towards the south which the prevailing easterly winds 
give the wind-surface, is more than counterbalanced in 
the opposite direction by the inclination of the surface 
of density. The current-surface gets an inclination towards 
the north; and the current itself sets east — in direct 
opposition to the prevailing winds. The current setting 
east maintains continuity between the north-flowing current 
of the west and the south-flowing current of the east 
coast. Between Iceland and Greenland, a depression is 
produced in the current-surface, constituting the boundary 
between the Polar and the Atlantic currents. The former 
of these flows at a rate of 5 or 6 to 14 nautical miles 
(0.12 m. to 0.3m.), the latter at a rate of 4 nautical miles 
(Ose): 
Off the east coast of Iceland, the current — its 
outer side — flows in company with the arm sent off from 
the Polar current towards the south, at a rate of 14 nau- 
tical miles (0.3 m.). South of the 65th parallel of latitude, 
it bends south-east and east, entering the Norwegian Sea 
to the left of the direct Atlantic current. 
If we place the Isothermal Map, Pl. XVI, on the 
Current Map, Pl. XLIII, the cause of the linguiform shape 
of the isotherms will be seen at a glance. 
west, 
Il. The Currents in the Deep. 
As a guide to the study of the motion of the water in 
the depths of the sea, I first investigate in what manner 
the static pressure dependent on density and the form of 
the surface is distributed over the surfaces of level at different 
depths. This is precisely the method adopted in meteoro- 
logy when constructing isobaric maps. 
Op SU SE 6 220) 
1—np 
the pressure is computed at a given point of a surface of 
level, the depth of which beneath the normal surface of 
the sea, on the 45th parallel of latitude, is H fathoms. 
Now, if we add to these figures the vertical co-ordinate of 
the current-surface for the same point, expressed as pres- 
NS 
According to the formula p= 
* 
bo 
