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(enthalpy) in the upper water surface layer. A comparison of evolutions of the heat
contents computed from the difference between temperatures of upper and bottom
boundaries of the subsurface layer with evolutions of microwave and infrared
radiation intensity is conducted.
Here, it is again necessary to remark that difference between microwave and
infrared ranges consists in their response on the atmosphere state:
•
intensity of super high frequency is de
ned by means of the product of emis-
sivity coef
cient (
ʺ
) and thermodynamic temperature (T) within the limits of
ef
cient radiation layer (l
ef
) where dT
b
/dT
≤
0.5 and l
ef
equals to the part of
centimeter; and
•
IR-range methods can be used only in the cases when the atmosphere is free
from aerosols, hydrometeors, and clouds as well as l
ef
equals to the part of
millimeter.
Usually, the values of sensible q
h
and latent q
e
heat at the air-sea boundary are
calculated by means of well known in the meteorology formulae:
q
h
¼ c
p
q
c
t
t
s
t
a
ð
Þ
V
;
q
e
¼ L
q
ð
0
:
622
=
P
Þ
c
e
e
e
o
ð
Þ
V
;
ð
2
:
10
Þ
where t
a
is the air temperature, P is the atmospheric pressure; e is the atmosphere
humidity, V is the wind speed in the near-surface atmosphere, t
s
is the ocean surface
temperature, e
o
is the the air humidity, c
t
is the numbers of Schmidt (heat
exchange), c
e
is the number of Dalton (moisture exchange), L is the speci
c heat of
evaporation, c
p
is the speci
c air heat under constant pressure, and
ˁ
is the atmo-
sphere density.
Formulae (
2.10
) can be used for calculation of sensible and latent heat
uxes
only in aquatories that are serviced by meteorological stations. Figure
2.33
repre-
sents such calculations for NDBC SMKF1 during hurricane Katrina evolution.
Capability of satellite SHF-radiometric methods to evaluate the characteristics of
large-scale heat and dynamic interaction of the atmosphere and ocean is based on
the use of resonance absorption of radiowaves 1.35 cm by atmospheric moisture. In
this case different models are used (Skou 2008; Pampaloni and Paloscia 2000). One
of such simple model is usually used:
fl
I ¼ I
1
þ
I
2
þ
I
3
where I
1
= I
s
exp[
(H)] is the intensity of natural radiation of the oceanic surface I
s
attenuated in the atmosphere;
−˄
the coef
cient exp[
−˄
(H)] is the index of the
absorption; I
2
¼
R
0
I
a
ðÞ
exp½
s
ðÞs
ðÞ
dz is the intensity of upgoing atmospheric
I
3
¼ R
R
0
radiation;
I
a
ðÞ
exp½
c
ðÞs
ðÞ
dz is the intensity of atmospheric
ðÞ
¼
R
H
0
z
ðÞ
dz
0
emission re
fl
ected from the water surface;
s
c
is the integral
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