The Geodetic Reference System 1980 (GRS80) consists of a global reference ellipsoid and a normal gravity model.[1] [2] [3] The GRS80 gravity model has been followed by the newer more accurate Earth Gravitational Models, but the GRS80 reference ellipsoid is still the most accurate in use for coordinate reference systems, e.g. for the international ITRS, the European ETRS89 and (with a 0,1 mm rounding error) for WGS 84 used for the American Global Navigation Satellite System (GPS).
Geodesy is the scientific discipline that deals with the measurement and representation of the earth, its gravitational field and geodynamic phenomena (polar motion, earth tides, and crustal motion) in three-dimensional, time-varying space.
The geoid is essentially the figure of the Earth abstracted from its topographic features. It is an idealized equilibrium surface of sea water, the mean sea level surface in the absence of currents, air pressure variations etc. and continued under the continental masses. The geoid, unlike the ellipsoid, is irregular and too complicated to serve as the computational surface on which to solve geometrical problems like point positioning. The geometrical separation between it and the reference ellipsoid is called the geoidal undulation, or more usually the geoid-ellipsoid separation, N. It varies globally between .
A reference ellipsoid, customarily chosen to be the same size (volume) as the geoid, is described by its semi-major axis (equatorialradius) a and flattening f. The quantity f = (a−b)/a, where b is the semi-minor axis (polar radius), is a purely geometrical one. The mechanical ellipticity of the earth (dynamical flattening, symbol J2) is determined to high precision by observation of satellite orbit perturbations. Its relationship with the geometric flattening is indirect. The relationship depends on the internal density distribution.
The 1980 Geodetic Reference System (GRS 80) posited a semi-major axis and a flattening. This system was adopted at the XVII General Assembly of the International Union of Geodesy and Geophysics (IUGG) in Canberra, Australia, 1979.
The GRS 80 reference system was originally used by the World Geodetic System 1984 (WGS 84). The reference ellipsoid of WGS 84 now differs slightly due to later refinements.
The numerous other systems which have been used by diverse countries for their maps and charts are gradually dropping out of use as more and more countries move to global, geocentric reference systems using the GRS80 reference ellipsoid.
The reference ellipsoid is usually defined by its semi-major axis (equatorialradius)
a
b
(b/a)
f
a
GM
J2
\omega
f
a=6378137m
GM=3986005 x 108
| m3/s2 |
Dynamical form factor
J2=108263 x 10-8
Angular velocity of rotation
\omega=7292115 x 10-11
| s-1 |
f
Reciprocal of flattening =
1/f
Semi-minor axis = Polar Radius =
b
Aspect ratio =
b/a
Mean radius as defined by the International Union of Geodesy and Geophysics (IUGG):
R1=(2a+b)/3
Authalic mean radius =
R2
Radius of a sphere of the same volume =
R3=(a2b)1/3
Linear eccentricity =
c=\sqrt{a2-b2}
Eccentricity of elliptical section through poles =
e=
| \sqrt{a2-b2 | |
Polar radius of curvature =
a2/b
Equatorial radius of curvature for a meridian =
b2/a
Meridian quadrant = 10 001 965.7292 m;
2\pi/\omega
The formula giving the eccentricity of the GRS80 spheroid is:[1]
e2=
| a2-b2 | |
| a2 |
=3J2+
| 4{15} | |||
|
| e3 | |
| 2q0 |
,
where
2q0=\left(1+
| 3{e' | |
| 2}\right) |
\arctane'-
| 3{e'} | |
and
e'=
| e | |
| \sqrt{1-e2 |
\arctane'=\arcsine
e2=0.006694380022903415749574948586289306212443890\ldots
which gives
f=1/298.2572221008827112431628366\ldots.