Geoscience Reference
In-Depth Information
particle transport processes in the D, E, and F1 ionospheric regions because of
the dominating photochemical, local heating, and heat exchange processes in these
ionospheric regions. Equations
4.11
and
4.12
are used to obtain the components of
the ion velocity vector, which are needed to calculate the thermospheric wind and
temperature, taking into account ion drag and Joule heating.
4.2.2
Ionospheric F2-Region and Protonosphere Block
In this block, parameters of the ionospheric F2-region and the protonosphere
(plasmasphere and inner magnetosphere cold plasma) are calculated, namely, the
atomic oxygen and hydrogen ion number densities
n
(O
C
)and
n
(H
C
)aswellas
ion and electron temperatures
T
i
and
T
e
and ion velocities
V
(O
C
)and
V
(H
C
)for
the height range from 175 km to the radial distance of 15
R
E
. We consider that all
charged components of the upper atmosphere are fully magnetized above 175 km
because
in
˝
i
at these heights (where ˝
i
is ion gyrofrequency) so that the
geomagnetic field has a very strong influence on the behavior of the ion and electron
gases. For this reason, we use the magnetic dipole coordinate system in this block
and perform the integration of modeling equations along dipole geomagnetic field
lines simultaneously, taking into account electromagnetic plasma drift perpendicular
to geomagnetic field lines. The following continuity, momentum, and heat balance
equations are solved in this block:
par
n
i
V
i
D
Q
i
L
i
n
i
r
par
per
per
Dn
i
=Dt
Cr
V
(4.14)
2m
i
n
i
.
˝ V
i
/
par
par
par
.n
i
kT
i
/
.n
i
=n
e
/
r
par
.n
e
kT
e
/
D
m
i
n
g
r
ij
ij
n
i
j
X
n
par
X
j
in
in
n
i
V
par
i
par
i
par
V
V
V
(4.15)
per
i
per
e
D E B
=B
2
V
D V
(4.16)
D
X
i
per
i
=n
e
per
e
V
n
i
V
(4.17)
.3n
i
k=2/
DT
i
=Dt
C V
par
T
i
C
.n
i
kT
i
/
rV
par
i
par
i
par
.
i
r
par
T
i
/
r
r
D
P
iQ
C
P
iT
C
P
j
iT
C
P
iT
(4.18)
.3n
e
k=2/
DT
e
=Dt
C V
par
T
e
C
.n
e
kT
e
/
rV
par
e
par
e
par
.
e
r
par
T
e
/
r
r
D
P
eQ
C
P
eQ
C
P
eT
C
P
eT
C
P
eT
(4.19)
