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∞
λ
p
I
(
µ, ν, p
)=
·
J
µ
(
aλ
)
·
J
ν
(
rλ
)
·
exp (
−
λh
)
·
dλ,
0
b
r
−
b
0
r
δb
ϕ
=
b
ϕ
−
b
0
ϕ
δb
r
=
,
,
b
0
b
0
∆
=(
ρ
0
+
ρ
1
)
2
+(
δ
0
−
δ
1
)
2
and
h
is the thickness of the atmosphere.
Let us estimate the anomalous magnetic field below the center of the in-
homogeneity (
r
=0
,ϕ
=0
,δb
r
=
δb
x
,δb
ϕ
=
δb
y
). Let also assume that the
disturbances
δΣ
P
and
δΣ
H
of
Σ
P
0
and
Σ
H
0
are small. Then (13.17) can be
simplified and reduced to
a
z
2
δb
ϕ
=
q
P
4
,
a
z
2
δ
0
q
H
4
ρ
0
δb
r
=
−
,
(13.18)
where
q
P
=
δΣ
P
2
Σ
P
0
δΣ
P
+
Σ
H
0
δΣ
H
Σ
P
0
+
Σ
H
0
Σ
P
0
−
,
q
H
=
δΣ
H
2
Σ
P
0
δΣ
P
+
Σ
H
0
δΣ
H
Σ
P
0
+
Σ
H
0
Σ
H
0
−
.
(13.19)
Since
a
z
2
4
Γ
,
≈
where
Γ
is the antenna gain,
δb
ϕ
=
q
P
Γ
Σ
H
0
Σ
P
0
q
H
Γ
,
δb
r
=
−
.
(13.20)
Let us consider the variation of the conductivity near the reflection point. By
virtue of the foregoing, the disturbances of the conductivities due to high
T
e
are proportional to the electron concentration
Ne
=
N
e
(
T
e
), or
δΣ
P
=
Σ
P
0
∆
δN
e
δΣ
H
=
Σ
H
0
∆
δN
e
N
e
0
l
h
,
where
l
h
is the thickness of the heated layer near the reflection point while
Σ
P
0
∆
and
Σ
H
0
∆
are
Σ
P
and
Σ
H
of an undisturbed 1 km layer, respectively.
Then
N
e
0
l
h
and
δN
e
N
e
0
,
since
δN
e
=
δN
e
(
T
e
)or
δN
e
=
δN
e
(
E
), where
E
is the electric field of the
wave at the height
z
. So long as the amplitude
E
0
is not too high, we can
q
P
∼
q
H
∼
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