Geoscience Reference
In-Depth Information
Fig. 3.2.
Vertical profile of net, downward, and upward fluxes of solar radiation in the
cloud for three wavelengths.
Solid lines
are the original measurements;
dashed lines
are
the smoothed values. Observation 20th April 1985, overcast stratus cloudiness. Cloud top
1400 m, cloud bottom - 900 m, solar incident zenith angle
ϑ
0
=
µ
0
=
49
◦
(
0. 647), snow
surface
The substituting of (3.3) to (3.2) provided the conditions for obtaining weights
β
j
1
1
1
−1
β
j
(
f
↓
(
z
i
+
j
)−
f
↓
(
z
i
−1+
j
))
≥
−1
β
j
(
f
↑
(
z
i
+
j
)−
f
↑
(
z
i
−1+
j
)) ,
−1
β
j
=
1.
=
=
=
j
j
j
(3.4)
The equation system(3.4) was solvedwith the iterationmethod. Firstly, weights
β
j
for measured values
f
↓
(
z
i
),
f
↑
(
z
i
) were obtained after the conversion of the
inequality to the equality in (3.4). Only three spectral points in the interval cen-
ters (UV- 370 nm, VD- 550 nm, NIR- 850 nm)wereconsideredasasmoothing
condition for all other wavelengths. Equation system (3.4) was solved using the
Least-Squares Technique (LST) (Anderson 1971; Kalinkin 1978). The formulas
and features of the LST in applying to atmospheric optics will be considered
in Chap. 4 and here we are presenting the results only.
Then values
F
↓
(
z
i
),
F
↑
(
z
i
) were calculated using (3.2), and conditions (3.3)
were verified for all wavelengths and altitudes. The iterations were broken in
the case of satisfying the conditions, otherwise the above-described procedure
was repeatedafter substitutingvalues
F
↓
(
z
i
),
F
↑
(
z
i
)to
f
↓
(
z
i
),
f
↑
(
z
i
) in (3.4). One
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