Earth radius (denoted by the symbol R⊕ or by ) 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, the radius ranges from a maximum of nearly 6,378 km (3,963 mi) (equatorial radius, denoted a) to a minimum of nearly 6,357 km (3,950 mi) (polar radius, denoted b).
|Unit system||astronomy, geophysics|
|Symbol||R⊕ or ,|
|1 R⊕ in ...||... is equal to ...|
|SI base unit||6.3781×106 m|
|Metric system||6,357 to 6,378 km|
|English units||3,950 to 3,963 mi|
A globally-average value is usually considered to be 6,371 kilometres (3,959 mi) 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 (R1) 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 (R2); and the volumetric radius, which is the radius of a sphere having the same volume as the ellipsoid (R3). All three values are about 6,371 kilometres (3,959 mi).
Other ways to define and measure the Earth radius involve the radius of curvature. A few definitions yield values outside the range between polar radius and equatorial radius because they include local or geoidal topography or because they depend on abstract geometrical considerations.
Earth's rotation, internal density variations, and external tidal forces cause its shape to deviate systematically from a perfect sphere. 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 surface
- A spheroid, also called an ellipsoid of revolution, geocentric to model the entire Earth, or else geodetic for regional work
- 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". 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 radius falls between the polar minimum of about 6,357 km and the equatorial maximum of about 6,378 km (3,950 to 3,963 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 a is larger than the polar radius b by approximately aq. The oblateness constant q is given by
where ω is the angular frequency, G is the gravitational constant, and M is the mass of the planet. For the Earth 1/q ≈ 289, which is close to the measured inverse flattening 1/f ≈ 298.257. 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.
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 110 m (360 ft) 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).
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 5 m (16 ft) of reference ellipsoid height, and to within 100 m (330 ft) 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.[clarification needed]
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 a, or semi-major axis, is the distance from its center to the equator and equals 6,378.1370 km (3,963.1906 mi). The equatorial radius is often used to compare Earth with other planets.
- The Earth's polar radius b, or semi-minor axis, is the distance from its center to the North and South Poles, and equals 6,356.7523 km (3,949.9028 mi).
The geocentric radius is the distance from the Earth's center to a point on the spheroid surface at geodetic latitude φ:
where a and b are, respectively, the equatorial radius and the polar radius.
The extrema geocentric radii on the ellipsoid coincide with the equatorial and polar radii. They are vertices of the ellipse and also coincide with minimum and maximum radius of curvature.
Radii of curvature
Principal radii of curvature
In particular, the Earth's meridional radius of curvature (in the (north–south) meridian direction) at φ is:
The Earth's meridional radius of curvature at the equator equals the meridian's semi-latus rectum:
- b2/a = 6,335.439 km
The Earth's prime-vertical radius of curvature at the equator equals the equatorial radius, N = a.
The Earth's polar radius of curvature (either meridional or prime-vertical) is:
- a2/b = 6,399.594 km
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 the principal radii of curvature are
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 .
Combined radii of curvature
It is possible to combine the principal radii of curvature above in a non-directional manner.
The Earth's Gaussian radius of curvature at latitude φ is:
Where K is the Gaussian curvature, .
The Earth's mean radius of curvature at latitude φ is::97
The Earth can be modeled as a sphere in many ways. This section describes the common ways. The various radii derived here use the notation and dimensions noted above for the Earth as derived from the WGS-84 ellipsoid; namely,
- Equatorial radius: a = (6378.1370 km)
- Polar radius: b = (6356.7523 km)
A sphere being a gross approximation of the spheroid, which itself is an approximation of the geoid, units are given here in kilometers rather than the millimeter resolution appropriate for geodesy.
In astronomy, the International Astronomical Union denotes the nominal equatorial Earth radius as , which is defined to be 6,378.1 km (3,963.2 mi).:3 The nominal polar Earth radius is defined as = 6,356.8 km (3,949.9 mi). These values correspond to the zero Earth tide convention. Equatorial radius is conventionally used as the nominal value unless the polar radius is explicitly required.:4 The nominal radius serves as a unit of length for astronomy. (The notation is defined such that it can be easily generalized for other planets; e.g., for the nominal polar Jupiter radius.)
In geophysics, the International Union of Geodesy and Geophysics (IUGG) defines the Earth's mean radius (denoted R1) to be
Earth's authalic radius (meaning "equal area") is the radius of a hypothetical perfect sphere that has the same surface area as the reference ellipsoid. The IUGG denotes the authalic radius as R2. A closed-form solution exists for a spheroid:
where e2 = a2 − b2/a2 and A is the surface area of the spheroid.
Another spherical model is defined by the Earth's volumetric radius, which is the radius of a sphere of volume equal to the ellipsoid. The IUGG denotes the volumetric radius as R3.
Another global radius is the Earth's rectifying radius, giving a sphere with circumference equal to the perimeter of the ellipse described by any polar cross section of the ellipsoid. This requires an elliptic integral to find, given the polar and equatorial radii:
For integration limits of [0,π/2], the integrals for rectifying radius and mean radius evaluate to the same result, which, for Earth, amounts to 6,367.4491 km (3,956.5494 mi).
The meridional mean is well approximated by the semicubic mean of the two axes,
which differs from the exact result by less than 1 μm (4×10−5 in); the mean of the two axes,
about 6,367.445 km (3,956.547 mi), can also be used.
Global mean radius of curvature
The global mean radius of curvature, averaged in all azimuths and at all points on the surface, is given by the area-weighted global mean Gaussian curvature:
For the WGS 84 ellipsoid, the mean curvature equals 6,370.994 km (3,958.752 mi).
The mathematical expressions above apply over the surface of the ellipsoid. The cases below considers Earth's topography, above or below a reference ellipsoid. As such, they are topographical geocentric distances, Rt, which depends not only on latitude.
- Maximum Rt: the summit of Chimborazo is 6,384.4 km (3,967.1 mi) from the Earth's center.
- Minimum Rt: the floor of the Arctic Ocean is approximately 6,352.8 km (3,947.4 mi) from the Earth's center.
Topographical global mean
The topographical mean geocentric distance averages elevations everywhere, resulting in a value 230 m larger than the IUGG mean radius, the authalic radius, or the volumetric radius. This topographical average is 6,371.230 km (3,958.899 mi) with uncertainty of 10 m (33 ft).
Derived quantities: diameter, circumference, arc-length, area, volume
Earth's diameter is simply twice Earth's radius; for example, equatorial diameter (2a) and polar diameter (2b). For the WGS84 ellipsoid, that's respectively:
- 2a=12,756.2740 km (7,926.3812 mi),
- 2b=12,713.5046 km (7,899.8055 mi).
Earth's circumference equals the perimeter length. The equatorial circumference is simply the circle perimeter: Ce=2πa, in terms of the equatorial radius, a. The polar circumference equals Cp=4mp, four times the quarter meridian mp=aE(e), where the polar radius b enters via the eccentricity, e=(1-b2/a2)0.5; see Ellipse#Circumference for details.
Earth's volume, or that of the reference ellipsoid, is V = 4/3πa2b. Using the parameters from WGS84 ellipsoid of revolution, a = 6,378.137 km and b = 6,356.7523142km, V = 1.08321×1012 km3 (2.5988×1011 cu mi).
This table summarizes the accepted values of the Earth's radius.
|Agency||Description||Value (in meters)||Ref|
|IAU||nominal "zero tide" equatorial||6378100|
|IAU||nominal "zero tide" polar||6356800|
|IUGG||semiminor axis (b)||6356752.3141|
|IUGG||polar radius of curvature (c)||6399593.6259|
|IUGG||mean radius (R1)||6371008.7714|
|IUGG||radius of sphere of same surface (R2)||6371007.1810|
|IUGG||radius of sphere of same volume (R3)||6371000.7900|
|IERS||WGS-84 ellipsoid, semi-major axis (a)||6378137.0|
|IERS||WGS-84 ellipsoid, semi-minor axis (b)||6356752.3142|
|IERS||WGS-84 first eccentricity squared (e2)||0.00669437999014|
|IERS||WGS-84 ellipsoid, polar radius of curvature (c)||6399593.6258|
|IERS||WGS-84 ellipsoid, Mean radius of semi-axes (R1)||6371008.7714|
|IERS||WGS-84 ellipsoid, Radius of Sphere of Equal Area (R2)||6371007.1809|
|IERS||WGS-84 ellipsoid, Radius of Sphere of Equal Volume (R3)||6371000.7900|
|GRS 80 semi-major axis (a)||6378137.0|
|GRS 80 semi-minor axis (b)||≈6356752.314140|
|Spherical Earth Approx. of Radius (RE)||6366707.0195|
|meridional radius of curvature at the equator||6335439|
|Maximum (the summit of Chimborazo)||6384400|
|Minimum (the floor of the Arctic Ocean)||6352800|
|Average distance from center to surface||6371230±10|
The first published reference to the Earth's size appeared around 350 BC, when Aristotle reported in his book On the Heavens that mathematicians had guessed the circumference of the Earth to be 400,000 stadia. Scholars have interpreted Aristotle's figure to be anywhere from highly accurate to almost double the true value. The first known scientific measurement and calculation of the circumference of the Earth was performed by Eratosthenes in about 240 BC. Estimates of the accuracy of Eratosthenes's measurement range from 0.5% to 17%. For both Aristotle and Eratosthenes, uncertainty in the accuracy of their estimates is due to modern uncertainty over which stadion length they meant.
- For details see figure of the Earth, geoid, and Earth tide.
- There is no single center to the geoid; it varies according to local geodetic conditions.
- In 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.
- The value of the radius is completely dependent upon the latitude in the case of an ellipsoid model, and nearly so on the geoid.
- This follows from the International Astronomical Union definition rule (2): a planet assumes a shape due to hydrostatic equilibrium where gravity and centrifugal forces are nearly balanced.
- 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.
- N 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.
- Mamajek, E. E; Prsa, A; Torres, G; et al. (2015). "IAU 2015 Resolution B3 on Recommended Nominal Conversion Constants for Selected Solar and Planetary Properties". arXiv:1510.07674 [astro-ph.SR].
- Moritz, H. (1980). Geodetic Reference System 1980, by resolution of the XVII General Assembly of the IUGG in Canberra.
- IAU 2006 General Assembly: Result of the IAU Resolution votes Archived 2006-11-07 at the Wayback Machine
- Satellites Reveal A Mystery Of Large Change In Earth's Gravity Field , Aug. 1, 2002, Goddard Space Flight Center.
- NASA's Grace Finds Greenland Melting Faster, 'Sees' Sumatra Quake, December 20, 2005, Goddard Space Flight Center.
- "WGS84RPT.tif:Corel PHOTO-PAINT" (PDF). Retrieved 2018-10-17.
- "Info" (PDF). earth-info.nga.mil.
- "Equatorial Radius of the Earth". Numerical Standards for Fundamental Astronomy: Astronomical Constants : Current Best Estimates (CBEs). IAU Division I Working Group. 2012. Archived from the original on 2016-08-26. Retrieved 2016-08-10.
- Bowring, B. R. (October 1987). "Notes on the curvature in the prime vertical section". Survey Review. 29 (226): 195–196. doi:10.1179/sre.19188.8.131.52.
- Lass, Harry (1950). Vector and Tensor Analysis. McGraw Hill Book Company, Inc. pp. 71–77.
- Torge, Wolfgang (2001). Geodesy. ISBN 9783110170726.
- Moritz, H. (March 2000). "Geodetic Reference System 1980". Journal of Geodesy. 74 (1): 128–133. Bibcode:2000JGeod..74..128.. doi:10.1007/s001900050278. S2CID 195290884.
- Snyder, J.P. (1987). Map Projections – A Working Manual (US Geological Survey Professional Paper 1395) p. 16–17. Washington D.C: United States Government Printing Office.
- "Discover-TheWorld.com – Guam – POINTS OF INTEREST – Don't Miss – Mariana Trench". Guam.discover-theworld.com. 1960-01-23. Archived from the original on 2012-09-10. Retrieved 2013-09-16.
- Frédéric Chambat; Bernard Valette (2001). "Mean radius, mass, and inertia for reference Earth models" (PDF). Physics of the Earth and Planetary Interiors. 124 (3–4): 234–253. Bibcode:2001PEPI..124..237C. doi:10.1016/S0031-9201(01)00200-X. Retrieved 18 November 2017.
- Williams, David R. (2004-09-01), Earth Fact Sheet, NASA, retrieved 2007-03-17
- Phillips, Warren (2004). Mechanics of Flight. John Wiley & Sons, Inc. p. 923. ISBN 0471334588.
- Aristotle. On the Heavens. Book II 298 B. Retrieved 5 November 2017.
- Drummond, William (1817). "On the Science of the Egyptians and Chaldeans, Part I". The Classical Journal. 16: 159.
- "Figure of the Earth". Encyclopædia Britannica. 1911.
- "Eratosthenes, the Greek Scientist". Encyclopædia Britannica. 2016.