158 
bliver krum. I de nedre Lag vil Centrifugalkraften virke 
i modsat Retning af Jordrotationen!. Afbøjningen fra 
Gradientens Retning vil øges, indtil Virkningen af Gradient- 
kraften. Jordrotationen, Centrifugalkraften og Frictionen 
frembringer en Afbojning, under hvilken disse Kreefter 
holde hverandre i Ligevægt. 
Den endelige Afbøjnings Størrelse beror væsentlig paa 
Frictionens Størrelse. Jo større denne er, desto mindre bliver 
Afbøjningen. I Havet er Frictionen liden, undtagen ved 
Kysterne og Bunden*, Afbøjningsvinkelen bliver derfor 1 
det frie Hav ret Vinkel. —Vandpartikternes 
Baner blive næsten lodrette med Gradienternes Retning. 
Efterat altsaa de første Tidsrums mere centripetale Bevæ- 
gelser i de øvre Vandlag have 1 nogen Grad udfyldt Over- 
næsten en 
fladens Huling og løftet Grændsefladen op fra Bunden mod 
Overfladen, vil den resulterende Bevægelse ende med en 
Tilstand, som nærmere kan beskrives saaledes. 
I Overfladen og de øvre Lag over Grændsetladen er 
Bevægelsen cyclonisk, 1 Spiraler, der føre Vandet med for- 
holdsvis stor tangential, men ganske ringe radial (centripetal) 
Hastighed omkring Midtpartiets Trykminimum. Den hori- 
zontale. Hastighed bliver Nul i Grændsefladen, i Midtens 
Trykminimum og ved Randen. Den er overhovedet størst 
i Overfladen og aftager mod Dybet, til den bliver Nul i 
Grendsefladen. I en og samme Niveauflade har den et 
Maximum et Steds mellem Midtens Trykminimum og Ran- 
den. Dens absolute Maximum ligger saaledes i Overfladen 
mellem Midten og Randen, nærmest den sidste. 
I de nedre Lag, under Grændsefladen, er Bevægelsen 
antieyelonisk, 1 Spiraler, der føre Vandet fra Midtpartiet 
ud mod Randen. 
galkraften virker mod Jordrotationskraften, og Frictionen 
er større, da Vandet kommer i langt højere Grad i Berø- 
Her ere Gradienterne svagere, Centrifu- 
ring med Bunden, end 1 de øvre Lag. Den horizontale 
Bevægelse bliver følgelig svagere. Den horizontale Hastighed 
er Nul i Grændsefladen, i Midtens -Trykmaximum og ved 
Bunden. I en og samme Niveauflade er den størst et Steds 
mellem Midten og Randen. 
mellem Midten og Randen i en midlere Dybde under 
Grændsefladen. De prikkede Linier m B i Fig. 
exempelvis de horizontale Maximumshastigheders Plads, og 
de horizontale Ordinater i Curven Vv deres relative Størrelse. 
Dens absolute Maximum ligger 
2 angive 
Den horizontale Bevægelse er ledsaget af vertieale 
Bevægelser, der føre Vandet i det centrale Trykminimum 
1 Se min Grundziige der Meteorologie 4. Ude. S. 231—234. 
* Se ovenfor Side 124 og 125. 
Centrifugal force adds its influence, provided the course be 
In the lower strata, centrifugal foree will act in 
an opposite direction to that of the rotation of the earth.! 
The deflection from the direction of the gradient will 
increase till the effect of the force of the gradient, the 
rotation of the earth, the centrifugal force, and the fric- 
tion produce a deflection by which these forces equilibrate 
each other. 
The extent of the final deflection will mainly depend 
on the amount of friction. The greater this is, the less 
will be the deflection. Inthe sea we have little friction, save 
along the coast and at the bottom;? hence the angle of deflec- 
a curve. 
tion throughout the open sea is well-nigh a right angle. The 
motion of the particles of water would be almost perpen- 
dicular to the direction of the gradient. Therefore, when 
the more centripetal motion of the first period in the upper 
strata of water have to some extent filled fup the hollow 
of the surface, and lifted the limiting surface from the 
bottom towards the surface of the sea, the resulting 
motion will terminate in a state that may thus be described 
in detail. 
At the surface and in the upper strata, above the 
limiting surface, the motion is cyclonic, in spirals, which 
carry the water with comparatively great tangential, but 
very trifling radial (centripetal) velocity around the pressure- 
minimum of the mid-part. The horizontal velocity is nil 
at the limiting surface, at the pressure-minimum of the 
middle, and at the margin. It is on the whole greatest 
diminishes with the depth, being nil 
at the limiting surface. At one and the same surface of 
level, it has a maximum somewhere between the pressure- 
minimum of the middle and the margin. Its absolute maxi- 
mum lies accordingly at the surface, between the middle and 
the margin, nearest the latter. 
In the lower strata, below the limiting surface, the 
at the surface. and 
motion is anticyclonic, in spirals, which carry the water 
from the mid-part towards the margin. Here the gradi- 
ents are less steep, the centrifugal foree acts in opposition 
to the force arising from the rotation of the earth, and there 
is greater friction, the water coming to a much greater extent 
in contact with the bottom than in the upper strata. Hence 
the horizontal motion is slower. The horizontal velocity 
is nil at the limiting surface, at the pressure-maximum of 
the middle, at the bottom. At the same surface 
of level, it is greatest somewhere between the middle and 
the margin. The absolute between the 
middle and the margin, at a medial depth below the limit- 
The dotted limes mB in fig. 2 might rep- 
resent the loci of the horizontal maximum-velocities, and 
the horizontal ordinates in the curve Vv, their relative 
and 
maximum lies 
ing surface. 
amount. 
The horizontal motion is attended with vertical motions, 
that carry the water downward in the central pressure- 
1 See my “Grundziige der Meterologie,’ 4th Ed.. p. 231—234. 
See above, p. 124 and 125. 
