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connect it with the atmospheric and surface cycles. Rough estimates show that the rates
of the sulfur cycle in the water of the seas and oceans do not play a substantial role for
the remaining parts of its global cycle. And though this speci
c feature does exist, for
the purity of the numerical experiment, in the proposedmodel the internal hydrospheric
fl
fluxes of sulfur compounds are separated in space and parameterized with the same
details like other
fluxes of sulfur in the atmosphere and on land. This excessiveness is
important for other units of the global model as well. In particular, it is important for the
parameterization of photosynthesis whose rate RFI affects the closure of other bio-
geochemical cycles. Finally, assume: H
13
=
fl
ʳ ·
RFI, H
14
= b
·
MFI, H
15
= f
·
DU,
H
16
= p
·
DD, H
17
= q
·
DD, H
18
=H
2
SOD/t
H2SOD
, H
19
= u
·
SO
4
D, H
20
= a
1
v
D
·
SO
4
D,
H
21
= b
1
v
D
·
DU,whereMFI is the mass of
dead phytoplankton, t
H2SOU
and t
H2SOD
is the time of complete oxidation of H
2
Sinthe
sea water in the photic and deep layers, respectively;
H
2
SOD, H
22
=H
2
SOU/t
H2SOU
, H
23
= g
·
ʳ
, b, f, p, q, u, a
1
, b
1
,andg are the
constants.
The anthropogenic input to the sulfur unit is realized through the prescribed
fl
uxes C
2
, C
6
, C
10
, H
1
, and H
6
in the form of the functions of the spatial coordinates
and time.
1.7.7 Global Phosphorus Cycle Modeling
The
flux diagram of the model of the global phosphorus cycle (MGBP) is presented
in the scheme in Fig.
1.45
, according to which the balance system of equations will
be:
fl
@
@
t
þ
V
u
@
P
A
P
A
@u
þ
V
k
@
P
A
@k
H
16
;
ðu; kÞ2N
O
;
¼ H
1
þ
H
19
þ
H
7
H
8
;
ðu; kÞ2N=N
O
;
@
P
U
@
t
þ
v
u
@
P
U
@u
þ
v
k
@
P
U
@k
þ
v
z
@
P
U
@
z
¼ H
11
þ
H
15
þ
H
16
H
9
H
10
;
@
t
þ
v
u
@
þ
v
k
@
þ
v
z
@
P
L
@
P
L
@u
P
L
@k
P
L
@
z
¼ H
12
þ
H
14
H
13
H
15
;
@
P
S
@
t
¼ H
2
þ
H
8
þ
H
9
þ
H
10
H
6
H
7
H
11
;
where P
U
=P
U1
+ P
U2
+ P
U3
, P
S
=P
S1
+ P
S2
. With this detailing we have:
@
P
U1
@
t
þ
v
u
@
P
U1
þ
v
k
@
P
U1
@k
þ
v
z
@
P
U1
@
z
¼ H
17
H
9
H
10
H
20
;
@u
@
P
U2
@
t
þ
v
u
@
P
U2
@u
þ
v
k
@
P
U2
@k
þ
v
z
@
P
U2
@
z
¼ H
20
H
18
;
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