Information Technology Reference
In-Depth Information
where
E
(1)
y
E
(2)
y
E
(3)
y
E
(1)
x
E
(2)
x
E
(3)
x
H
(1)
y
H
(2)
y
H
(3)
y
H
(1)
y
H
(2)
y
H
(3)
y
Z
xx
=
1
Q
Z
yx
=
1
Q
,
,
H
(1)
z
H
(2)
z
H
(3)
z
H
(1)
z
H
(2)
z
H
(3)
z
E
(1)
x
E
(2)
x
E
(3)
x
E
(1)
y
E
(2)
y
E
(3)
y
H
(1)
z
H
(2)
z
H
(3)
z
H
(1)
z
H
(2)
z
H
(3)
z
Z
xy
=
1
Q
Z
yy
=
1
Q
,
,
H
(1)
x
H
(2)
x
H
(3)
x
H
(1)
x
H
(2)
x
H
(3)
x
E
(1)
x
E
(2)
x
E
(3)
x
E
(1)
y
E
(2)
y
E
(3)
y
H
(1)
x
H
(2)
x
H
(3)
x
H
(1)
x
H
(2)
x
H
(3)
x
Z
xz
=
1
Q
Z
yz
=
1
Q
,
.
H
(1)
y
H
(2)
y
H
(3)
y
H
(1)
y
H
(2)
y
H
(3)
y
Inthematrixform
[
Z
]
H
E
=
,
(5
.
40)
where
⎡
⎤
⎡
⎤
E
x
E
y
Z
xx
Z
xy
Z
xz
H
x
H
y
H
z
⎣
⎦
,
⎣
⎦
.
[
Z
]
E
=
,
=
H
=
Z
yx
Z
yy
Z
yz
Taking the source effect into account, we can determine the
generalized
impedance tensor
Z
with matrix of the order 2
3 and can't determine the
Wiese-Parkinson matrix (all three components of the magnetic field become inde-
pendent, which manifests itself in the dramatic multiple-coherence drop). But it
is significant that Varentsov and his workmates in their experiments on the Baltic
shield get around this problem by selecting time intervals with rather large coher-
ence (Varentsov et al., 2003a, b), while Vanyan and his workmates reconstruct a
plane-wave normal field by averaging geomagnetic disturbances over a long period
of time (Vanyan et al., 2002b).
Going toward the strong source effect, the sophisticated situations may arise that
need examination, theoretical comprehension and special technological solutions.
The recent promising results obtained by Schmucker and by Semenov et al. in com-
bining the gradient and tipper soundings (Schmucker, 2003, 2004; Semenov et al.,
in press) may be very helpful in this area.
×
