Information Technology Reference
In-Depth Information
=
√
S
1
R
2
is the adjustment distance. The oscillation period
L
has a mean-
ing of the width of the structures. This critical parameter defines the intensity of
the
S
where
d
d
, we have the narrow structures with barely perceptible
leakage of the excess current. Hence we observe here the strong
S
-effect with
h
−
effect. As
L
<<
2
π
≈
S
and
Q
d
, we have the wide structures and the excess current in
the upper layer is barely perceptible due to the strong leakage. Hence we observe
here the weak
S
≈
1. As
L
>>
2
π
−
effect with
h
<<
S
and
Q
≈
0.
Figure 7.7 presents the
L
−
dependence of
Q
. The strong
S
−
effect with
Q
exceeding 0.9 shows itself at
L
≤
2
d
. The weak
S
−
effect with
Q
≤
0
.
1 is observed
10
4
at
L
≥
20
d
.
Let
1
=
10 Ohm
·
m
,
h
1
=
1 km (sediments) and
2
=
Ohm
·
m
,
h
2
=
100 km (lithosphere). In this typical geoelectric situation we have the adjust-
ment distance
d
effect is to be expected over the regional
structures (elevations, depressions) even 500-600 km wide.
Next
=
316 km and the strong
S
−
we
examine
the
TE-mode.
It
is
represented
by
the
components
E
x
(
y
,
z
)
,
H
y
(
y
,
z
)
,
H
z
(
y
,
z
). On the surface of the perfectly conductive basement
E
x
(
y
,
h
)
=
0
.
By virtue of (7.16)
E
x
(
y
,
0)
=
E
x
(
y
,
h
1
)
−
i
o
h
1
H
y
(
y
,
0)
E
x
(
y
,
h
1
)
=−
i
o
h
2
H
y
(
y
,
h
1
)
.
(7
45)
d
2
E
x
(
y
h
1
,
0)
H
y
(
y
,
0)
=
H
y
(
y
,
h
1
)
+
S
1
(
y
)
E
x
(
y
,
0)
+
.
i
o
dy
2
Eliminating
E
x
(
y
h
1
) from these equations, we get the differential
relation between the electric and magnetic fields on the Earth's surface
z
,
h
1
) and
H
y
(
y
,
=
0:
h
1
h
2
d
2
E
x
(
y
)
dy
2
−
[1
−
i
o
S
1
(
y
)
h
2
]
E
x
(
y
)
=
i
o
hH
y
(
y
)
,
(7
.
46)
Q
1
0.9
0.8
0.7
0.6
0.5
0.4
0.3
0.2
0.1
Fig. 7.7
Intensity of the
S
-effect in relation to the
width of the structure
L
and
adjustment distance
d
L/d
0
0
5
10
15
20
25
30
