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Re is the Reynolds number (Re = 2vR/D), Pe
—
is the Pekle number (Pe = vR/v),
v is water viscosity, v is the velocity of the bubble
'
is motion, D is the coef
cient of
the gas molecular diffusion.
Of course, the ocean surface condition substantially affects its gas exchange with
the atmosphere. The size of the basins covered with either foam or white caps
directly depends on a combination of the parameters such as wind speed, water
temperature, and sea currents. An analysis of the statistical characteristics of the
patchy pattern of the ocean surface made by many experts makes it possible to
describe the percentage distribution of the areas covered with foam (Sf)
f
) and white
caps (S
l
) with the following binary functions of wind speed V (at a height of 10 m):
0
for V
5 m/s
;
\
for V
5 m/s
S
f
¼
76
10
2
V
5
2
0
:
65 1
þ
4
:
ð
Þ
;
0
for V
5 m/s
;
\
for V
5 m/s
S
l
¼
2
10
2
V
5
3
0
:
015 1
þ
2
:
ð
Þ
:
According to Kiseleva (1990), the relationship between Sf
f
and S
l
at V
≥
5 m/s
obeys the following rule:
S
f
=
S
l
¼ 50
3
:
4 V
5
ð
Þ
It is clear that the structure of the atmosphere-ocean border can affect the gas
exchange within widely varying values of
Unfortunately, the level of knowledge of the laws of changes of the atmosphere-
ocean border structure as a function of synoptic situations does not permit a clear
estimation of the limits of detailing the processes taking place on this border, to obtain
the values of the
fl
uxes H
2
and H
3
close to real ones. This means that at this stage of
the synthesis of the global model of the CO
2
cycle some uncertainty still exists.
fl
4.4 The Zonal Model of the Global Carbon Cycle
in the Atmosphere-Ocean System
Consider one of the versions of parameterization of the carbon dioxide global
dynamics in the atmosphere-ocean system proposed and studied by Nefedova
(1994). The spatial heterogeneity of the World Ocean is approximated by the zonal
scheme in accordance with the latitudinal dependence of the climatic processes as
well as processes of mixing in the atmosphere and in the oceans. There are 14
latitudinal zones 10
o
in size. In the vertical, there are three layers in the World
Ocean: the upper quasi-homogeneous layer (UQHL) with a time-dependent
thickness, thermocline, and deep ocean. As a result, the World Ocean is divided
into 42 volume parts. An upwelling is assumed to exist between 40
o
N and 40
o
S
along with a downwelling in high latitudes. In the UQL the water
fl
flows poleward
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