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is sufficiently small, we can disregard the source-effect mode and restrict ourselves
to analysis of the plane-wave modes. On this way we go back to the magnetotelluric
and magnetovariational response functions discussed in Chaps. 1 and 4. For the sake
of integrity we can consider these functions in the terms of the generalized model
examined in the present Section.
Within the inhomogeneous domain V each plane-wave mode generates the
excess current
j
ex
(
m
)
E
A(
m
)
H
A(
m
)
,
m
=
1
,
2 that excites the anomalous field
{
,
}
,
m
=
1
,
2 . Summing the normal and anomalous fields, we get
E
(
m
)
E
N(
m
)
E
A(
m
)
=
+
(5
.
25)
H
(
m
)
H
N(
m
)
H
A(
m
)
=
+
m
=
1
,
2
.
The total field on the Earth's surface is
H
x
o
E
(1)
H
y
o
E
(2)
E
=
+
,
(5
.
26)
H
x
o
H
(1)
H
y
o
H
(2)
H
=
+
,
where
E
(1)
E
(1)
(
x
E
(2)
E
(2)
(
x
E
=
E
(
x
,
y
,
z
=
0)
,
=
,
y
,
z
=
0)
,
=
,
y
,
z
=
0)
,
H
(1)
H
(1)
(
x
H
(2)
H
(2)
(
x
H
=
H
(
x
,
y
,
z
=
0)
,
=
,
y
,
z
=
0)
,
=
,
y
,
z
=
0)
.
In the full form
H
x
o
E
(1)
H
y
o
E
(2)
E
x
=
+
x
x
(5
.
27)
H
x
o
E
(1)
H
y
o
E
(2)
E
y
=
+
y
y
and
H
(1)
x
H
(2)
x
H
x
o
H
y
o
H
x
=
+
a
H
(1)
y
H
(2)
y
H
x
o
H
y
o
H
y
=
+
b
(5
.
28)
H
(1)
z
H
(2)
z
H
x
o
H
y
o
H
z
=
+
.
c
From (5.28
a,b
)wefind
H
(2)
y
H
(2)
x
H
x
−
H
y
H
x
o
=
H
(2
x
,
H
(1)
H
(2)
H
(1)
−
x
y
y
(5
.
29)
H
(1)
y
H
(1)
x
−
H
x
+
H
y
H
y
o
=
.
H
(1)
H
(2)
H
(1)
H
(2)
−
x
y
y
x
