Fair-weather atmospheric electricity
Fair-weather atmospheric electricity
Basic facts about atmospheric electricity
Atmospheric electricity involves phenomena which are connected with the separation of
electric charges in the sub-ionospheric atmosphere (below about 100 km height).
In the ionosphere and magnetosphere there are strong electric currents originating
directly from the solar-terrestrial interaction; in the lower atmosphere,
a much weaker electric current flows in the so-called global circuit, which is maintained
by the thunderstorm activity. Charge separation takes place in three ways:
The mobility of electrically charged particles depends strongly on their size and
on the density of the medium. The mobility of small ions in the lower atmosphere
corresponds to a (terminal) speed of about 1 cm/s in an electric field
of 100 V/m. Dust particles are slower by a few orders of magnitude, so that the
electric conductivity of air is practically that due to the small ions. In the stratosphere
and mesosphere (10 - 90 km) air becomes thinner and cosmic radiation intensifies so that
the conductivity increases exponentially with height: while the electric conductivity of
air near the ground is of the order of 20 fS/m (femtosiemens/metre), in the ionosphere it
is already as high as that of the ground. (In the ionosphere, the electric conductivity
becomes also anisotropic: the geomagnetic field has an increasing influence on the
- In a thundercloud, small ice crystals collide with rime-growing graupels;
the crystals gain positive charge, the graupels negative
(the microscopic mechanism is not yet well known).
- Convection in the thundercloud carries the ice crystals to the cloud top,
the heavier graupels staying in the mid-cloud: a macroscopic dipole structure forms.
- by radiation ionization
- Cosmic and radioactive radiation ionize air, and equal numbers of
molecular-size positive and negative small ions are formed; air becomes (weakly)
- Small ions are also attached to airborne dust (aerosol), which thus
regularizes the number of small ions.
- by collision ionization
- Lightning and other discharges in the thundercloud ionize air
temporarily into electrically conducting channels.
The thundercloud charge centres, accumulating tens of coulombs of electricity, are
discharged mainly by lightning: cloud flashes (most abundant) cause mutual
neutralization of the centres; the lower centre is also discharged to the ground
- by negative ground flashes -
and charges up the earth (the positive centre is discharged similarly, but by a
smaller amount). An excess charge will be left in the upper positive centre, and it
leaks by conduction to the surrounding air, about one ampere per thunderstrom cell.
Because of the exponentially increasing conductivity, most of this leak current
is guided to the ionosphere, where it is distributed over the globe and
charges the upper atmosphere to a potential of about 250-300 kV with respect to the ground.
This "ionospheric potential" maintains the so-called fair-weather current, whose density is about
2 pA/m2 (picoamperes per square metre). According to Ohm's law, the fair-weather
current density and the electric conductivity are associated with a downward electric
field, about 100 V/m near the ground. The number of simultaneously active
thunder cells ("thunderstorms") over the globe is about 1000-2000,
so the whole circuit carries a current of about 1000 amperes.
Why does not the (fair-weather) atmospheric electric field cause a shock of 200 V
to a standing human? Because the human is grounded in practice; the poorly conducting
air cannot charge up a grounded object. Below a thundercloud, where the
ground-level electric field
may be tens of kV/m, the situation is different - but then the threat comes from
a lightning strike.
The ion balance near the ground can most simply be described by the equation
q = an2 + bnN
where q is ionization, n is the density of small ions (both polarities separately,
assumed equal), N is the density of aerosol, and a and b are recombination coefficients,
which describe the neutralization of ions with each other or with aerosol particles.
a and b are both about 1.6x10-12 m3s-1.
Ionization in southern Finland is about 6.6x106 m-3s-1,
one fifth or sixth coming from radioactivity. The small-ion densities are both
about 5x108 m-3 and the aerosol density is more than
tenfold, almost 1010 m-3.
It should be noted that the notion "dirt increases electric conductivity" is valid
for surfaces, for example insulators, but the matter is contrary for air: dirty
(dusty) air has poorer conductivity. However, if the "dirt" is a radioactive pollutant,
the higher ionization increases the electric conductivity. Such an episode
happened in May 1986, when an iodine cloud from the Chernobyl emission arrived at
southern Finland: the electric conductivity grew tenfold, but returned to a lower
level in a few days, because the half-life of radioactive iodine is 8 days.
Fair-weather atmospheric electricity has been measured in Finland in the 1970's and 1980's. The results are presented in Tapio J. Tuomi: Ten year summary 1977-1986 of atmospheric electricity measured at Helsinki-Vantaa Airport, Finland, Geophysica 25(1-2), 1-20 (1989). Other publications on the subject are Tapio J. Tuomi: Atmospheric electrode effect: approximate theory and wintertime observations. PAGEOPH 119, 31-45 (1980), and Tapio J. Tuomi: The atmospheric electrode effect over snow, J. Atm. Terr. Phys. 44(9), 737-745 (1982).