Earth radius (denoted as R🜨 or RE) is the distance from the center of Earth to a point on or near its surface. Approximating the figure of Earth by an Earth spheroid (an oblate ellipsoid), the radius ranges from a maximum (equatorial radius, denoted a) of about to a minimum (polar radius, denoted b) of nearly .
The globally averaged value is with a 0.3% variability (±10 km) for the following reasons. The International Union of Geodesy and Geophysics (IUGG) provides three reference values: the mean radius (R) of three radii measured at two equator points and a pole; the authalic radius, which is the radius of a sphere with the same surface area (R); and the volumetric radius, which is the radius of a sphere having the same volume as the ellipsoid (R). All three values are about .
Other ways to define and measure the Earth's radius involve either the spheroid's radius of curvature or the actual topography. A few definitions yield values outside the range between the polar radius and equatorial radius because they account for localized effects.
A nominal Earth radius (denoted ) is sometimes used as a unit of measurement in astronomy and geophysics, a conversion factor used when expressing planetary properties as multiples or fractions of a constant terrestrial radius; if the choice between equatorial or polar radii is not explicit, the equatorial radius is to be assumed, as recommended by the International Astronomical Union (IAU).
Introduction
Earth's rotation, internal density variations, and external tidal forces cause its shape to deviate systematically from a perfect sphere.For details see figure of the Earth, geoid, and Earth tide. Local topography increases the variance, resulting in a surface of profound complexity. Our descriptions of Earth's surface must be simpler than reality in order to be tractable. Hence, we create models to approximate characteristics of Earth's surface, generally relying on the simplest model that suits the need.
Each of the models in common use involve some notion of the geometric radius. Strictly speaking, spheres are the only solids to have radii, but broader uses of the term radius are common in many fields, including those dealing with models of Earth. The following is a partial list of models of Earth's surface, ordered from exact to more approximate: The actual surface of Earth The geoid, defined by mean sea level at each point on the real surfaceThere is no single center to the geoid; it varies according to local geodetic conditions. Where there is land, the geoid is generally below ground; it represents where the sea level would be if water could reach it from the ocean via an imaginary canal. A spheroid, also called an ellipsoid of revolution, geocentric to model the entire Earth, or else geodetic for regional workIn a geocentric ellipsoid, the center of the ellipsoid coincides with some computed center of Earth, and best models the earth as a whole. Geodetic ellipsoids are better suited to regional idiosyncrasies of the geoid. A partial surface of an ellipsoid gets fitted to the region, in which case the center and orientation of the ellipsoid generally do not coincide with the earth's center of mass or axis of rotation. A sphere
In the case of the geoid and ellipsoids, the fixed distance from any point on the model to the specified center is called "a radius of the Earth" or "the radius of the Earth at that point".The value of the radius is completely dependent upon the latitude in the case of an ellipsoid model, and nearly so on the geoid. It is also common to refer to any mean radius of a spherical model as "the radius of the earth". When considering the Earth's real surface, on the other hand, it is uncommon to refer to a "radius", since there is generally no practical need. Rather, elevation above or below sea level is useful.
Regardless of the model, any of these geocentric radii falls between the polar minimum of about 6357 km and the equatorial maximum of about 6378 km (3950 to 3963 mi). Hence, the Earth deviates from a perfect sphere by only a third of a percent, which supports the spherical model in most contexts and justifies the term "radius of the Earth". While specific values differ, the concepts in this article generalize to any major planet.
Physics of Earth's deformation
Rotation of a planet causes it to approximate an oblate ellipsoid/spheroid with a bulge at the equator and flattening at the North and South Poles, so that the equatorial radius is larger than the polar radius by approximately . The oblateness constant is given by
where is the angular frequency, is the gravitational constant, and is the mass of the planet. For the Earth , which is close to the measured inverse flattening . Additionally, the bulge at the equator shows slow variations. The bulge had been decreasing, but since 1998 the bulge has increased, possibly due to redistribution of ocean mass via currents.Satellites Reveal A Mystery Of Large Change In Earth's Gravity Field , Aug. 1, 2002, Goddard Space Flight Center.
The variation in density and crustal thickness causes gravity to vary across the surface and in time, so that the mean sea level differs from the ellipsoid. This difference is the geoid height, positive above or outside the ellipsoid, negative below or inside. The geoid height variation is under on Earth. The geoid height can change abruptly due to earthquakes (such as the Sumatra-Andaman earthquake) or reduction in ice masses (such as Greenland)., December 20, 2005, Goddard Space Flight Center.
Not all deformations originate within the Earth. Gravitational attraction from the Moon or Sun can cause the Earth's surface at a given point to vary by tenths of a meter over a nearly 12-hour period (see Earth tide).
Radius and local conditions
Given local and transient influences on surface height, the values defined below are based on a "general purpose" model, refined as globally precisely as possible within of reference ellipsoid height, and to within of mean sea level (neglecting geoid height).
Additionally, the radius can be estimated from the curvature of the Earth at a point. Like a torus, the curvature at a point will be greatest (tightest) in one direction (north–south on Earth) and smallest (flattest) perpendicularly (east–west). The corresponding radius of curvature depends on the location and direction of measurement from that point. A consequence is that a distance to the true horizon at the equator is slightly shorter in the north–south direction than in the east–west direction.
In summary, local variations in terrain prevent defining a single "precise" radius. One can only adopt an idealized model. Since the estimate by Eratosthenes, many models have been created. Historically, these models were based on regional topography, giving the best reference ellipsoid for the area under survey. As satellite remote sensing and especially the Global Positioning System gained importance, true global models were developed which, while not as accurate for regional work, best approximate the Earth as a whole.
Extrema: equatorial and polar radii The following radii are derived from the World Geodetic System 1984 (WGS-84) reference ellipsoid. It is an idealized surface, and the Earth measurements used to calculate it have an uncertainty of ±2 m in both the equatorial and polar dimensions. Additional discrepancies caused by topographical variation at specific locations can be significant. When identifying the position of an observable location, the use of more precise values for WGS-84 radii may not yield a corresponding improvement in accuracy.
The value for the equatorial radius is defined to the nearest 0.1 m in WGS-84. The value for the polar radius in this section has been rounded to the nearest 0.1 m, which is expected to be adequate for most uses. Refer to the WGS-84 ellipsoid if a more precise value for its polar radius is needed. The Earth's equatorial radius , or semi-major axis, is the distance from its center to the equator and equals . The equatorial radius is often used to compare Earth with other planets. The Earth's polar radius , or semi-minor axis is the distance from its center to the North and South Poles, and equals .
Location-dependent radii
Geocentric radius
The geocentric radius is the distance from the Earth's center to a point on the spheroid surface at geodetic latitude , given by the formula
where and are, respectively, the equatorial radius and the polar radius.
The maximum and minimum geocentric radii on the ellipsoid coincide, respectively, with the equatorial and polar radii, at the vertices of the ellipse. However, the maximum and minimum radii of curvature coincide with the poles and Equator, in opposite regions than the geocentric radii, due to Earth's oblateness.
Radii of curvature
Principal radii of curvature
There are two principal radii of curvature: along the meridional and prime-vertical normal sections.
The principal curvatures are the roots of Equation (125) in:
where in the first fundamental form for a surface (Equation (112) in):
E, F, and G are elements of the metric tensor:
, ,
in the second fundamental form for a surface (Equation (123) in):
e, f, and g are elements of the shape tensor:
is the unit normal to the surface at , and because and are tangents to the surface,
is normal to the surface at .
With for an oblate spheroid, the curvatures are
and
and the principal radii of curvature are
and
The first and second radii of curvature correspond, respectively, to the Earth's meridional and prime-vertical radii of curvature.
Geometrically, the second fundamental form gives the distance from to the plane tangent at .
Meridional In particular, the Earth's meridional radius of curvature (in the north–south direction) at is
where is the eccentricity of the earth. This is the radius that Eratosthenes measured in his arc measurement.
Prime vertical
If one point had appeared due east of the other, one finds the approximate curvature in the east–west direction.East–west directions can be misleading. Point B, which appears due east from A, will be closer to the equator than A. Thus the curvature found this way is smaller than the curvature of a circle of constant latitude, except at the equator. West can be exchanged for east in this discussion. This Earth's prime-vertical radius of curvature, also called the Earth's transverse radius of curvature, is defined perpendicular (orthogonal) to at geodetic latitude is defined as the radius of curvature in the plane that is normal to both the surface of the ellipsoid at, and the meridian passing through, the specific point of interest. and is
N can also be interpreted geometrically as the normal distance from the ellipsoid surface to the polar axis. The radius of a parallel of latitude is given by .
Combined radii of curvature
Azimuthal
Earth's azimuthal radius of curvature of an Earth normal section at an azimuth (measured clockwise from north) and at latitude , is derived from Euler's curvature formula as follows:
or
where is the azimuthal curvature of the ellipsoid.
Non-directional (Gaussian and mean)
It is possible to combine the principal radii of curvature above in a non-directional manner.
Earth's Gaussian radius of curvature at latitude is
or
where K is the Gaussian curvature, The Gaussian radius of curvature is defined in terms of the product of the principal radii of curvature and it integrates the azimuthal radius of curvature over the full circle. It corresponds to the radius of the osculating sphere that best fits the ellipsoid locally.
Earth's radius of mean curvature at latitude is
or
The mean curvature equals the arithmetic mean of the two principal curvatures and integrates the azimuthal curvature over the full circle.
Equatorial radii of curvature Earth's meridional radius of curvature at the equator equals the meridian's semi-latus rectum: