Online Encyclopedia
Geoid
A geoid is a close representation, physical model, of the figure of the Earth. According to C.F. Gauss, it is the "mathematical figure of the Earth", in fact, of her gravity field. It is that equipotential surface (surface of fixed potential value) which coincides on average with mean sea level.
The geoid surface is more irregular than the ellipsoid of revolution often used to approximate the shape of the physical Earth, but considerably more smooth than the Earth's physical surface. While the latter has excursions of +8,000 m (Mount Everest) and −11,000 ;m (Mariana Trench), the geoid varies by only approx. ±100 m about the reference ellipsoid of revolution.
Because the force of gravity is everywhere perpendicular to the geoid (being an equipotential surface), sea water if left to itself would assume a surface equal to it. Similarly if sea water would be allowed to freely penetrate the continental masses, e.g., through tunnels. In reality it is not, of course; still, geodesists are able to derive the heights of continental points above this imaginary, but physically defined, surface by a technique called spirit levelling.
When travelling by ship, one does not notice the undulations of the geoid; the local vertical is always perpendicular to it, and the local horizon tangential to it. A GPS receiver on board may show the height variations relative to the (mathematically defined) reference ellipsoid, the centre of which coincides with the Earth's centre of mass, the centre of orbital motion of the GPS satellites.
Spherical harmonics representation
Spherical harmonics are often used to approximate the shape of the geoid. The current best such set of spherical harmonic coefficients is EGM96 (Earth Gravity Model 1996), determined in an international collaborative project led by NIMA. It contains a full set of coefficients to degree and order 360, describing details in the global geoid as small as 55 km.
The mathematical description of this model is
![V=\frac{GM}{r}\left(1+{\sum_{n=2}^{360}}\left(\frac{a}{r}\right){\sum_{m=0}^n} \overline{P}_{nm}(\sin\varphi)\left[\overline{C}_{nm}\cos m\lambda+\overline{S}_{nm}\sin m\lambda\right]\right),](a/../upload/math/474c299381b5d4337afab3fc13b09a55.png)
where 
and λ are geocentric latitude and longitude respectively, 
are the fully normalized Legendre functions of degree n and order m, and 
and 
are the coefficients of the model. One easily counts that there are approx. 
different coefficients. The above formula produces the Earth's gravitational potential V at location 
, the co-ordinate r being the geocentric radius, i.e, distance from the Earth's centre.