Earth radius is the distance from a selected center of Earth to a point on its surface, which is often chosen to be sea level, or more commonly, the surface of an idealized ellipsoid representing the shape of Earth. Because Earth is not a perfect sphere, the determination of Earth's radius can have several values, depending on how it is measured; from its equatorial radius of about 6,378 kilometres (3,963 miles) to its polar radius of about 6,357 kilometres (3,950 miles).
13th century illustration of Earth in De sphaera mundi.
|Unit system||astronomy, geophysics|
|Symbol||R⊕ or ,|
|1 R⊕ in ...||... is equal to ...|
|SI base unit||×106 m6.3781|
|Metric system||6,357 to 6,378 km|
|English units||3,950 to 3,963 mi|
The International Union of Geodesy and Geophysics (IUGG) gives three global average radii, the arithmetic mean of the radii of the ellipsoid (R1), the radius of a sphere with the same surface area as the ellipsoid or authalic radius (R2), and the radius of a sphere with the same volume as the ellipsoid (R3). All three IUGG average radii are about 6,371 kilometres (3,959 mi). A fourth global average radius not mentioned by the IUGG is the rectifying radius, the radius of a sphere with a circumference equal to the perimeter of the polar cross section of the ellipsoid, about 6,367 kilometres (3,956 mi). The radius of curvature at any point on the surface of the ellipsoid depends on its coordinates and its azimuth, north-south (meridional), east-west (prime vertical), or somewhere in between.
Earth's rotation, internal density variations, and external tidal forces cause its shape to deviate systematically from a perfect sphere.[a] 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[b]
- A spheroid, also called an ellipsoid of revolution, geocentric to model the entire Earth, or else geodetic for regional work[c]
- 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".[d] 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 many 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 deformationEdit
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.[e] For the Earth 1/ ≈ 289, which is close to the measured inverse flattening 1/ ≈ 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. The gravity of the Moon and Sun cause the Earth's surface at a given point to undulate by tenths of meters over a nearly 12-hour period (see Earth tide).
Radius and local conditionsEdit
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.
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 radii in this section are for an idealized surface. Even the idealized radii have an uncertainty of ±2 m. The discrepancy between the ellipsoid radius and the radius to a physical location may 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 symbol given for the named radius is used in the formulae found in this article.
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 distance from the Earth's center to a point on the spheroid surface at geodetic latitude φ is:
where a and b are, respectively, the equatorial radius and the polar radius.
- Maximum: The summit of Chimborazo is 6,384.4 km (3,967.1 mi) from the Earth's center.
- Minimum: The floor of the Arctic Ocean is approximately 6,352.8 km (3,947.4 mi) from the Earth's center.
Radii of curvatureEdit
In particular, the Earth's radius of curvature in the (north–south) meridian at φ is:
This is the radius that Eratosthenes measured.
If one point had appeared due east of the other, one finds the approximate curvature in the east–west direction.[f]
This radius is also called the transverse radius of curvature. At the equator, N = R.
The Earth's meridional radius of curvature at the equator equals the meridian's semi-latus rectum:
- b2/ = 6,335.439 km
The Earth's polar radius of curvature is:
- a2/ = 6,399.594 km
It is possible to combine the principal radii of curvature above in a non-directional manner.
Global average radiiEdit
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,
- a = Equatorial radius (378.1370 km) 6
- b = Polar radius (356.7523 km) 6
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.
For Earth, the mean radius is 6,371.0088 km (3,958.7613 mi).
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 tide radii. Equatorial radius is conventionally used as the nominal value unless the polar radius is explicitly required.:4
A closed-form solution exists for a spheroid:
where e2 = a2 − b2/ and A is the surface area of the spheroid.
For the Earth, the authalic radius is 6,371.0072 km (3,958.7603 mi).
For Earth, the volumetric radius equals 6,371.0008 km (3,958.7564 mi).
Another mean radius is the 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:
The rectifying radius is equivalent to the meridional mean, which is defined as the average value of M:
For integration limits of [0,π/], 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.
Average distance from center to surfaceEdit
Most global mean radii are based on the reference ellipsoid, which approximates the geoid. The geoid has no direct relationship with surface topography, however. An alternative calculation averages elevations everywhere, resulting in a mean radius larger than the 230 mIUGG mean radius, the authalic radius, or the volumetric radius. This average is 6,371.230 km (3,958.899 mi) with uncertainty of 10 m (33 ft).
The best local spherical approximation to the ellipsoid in the vicinity of a given point is the osculating sphere. Its radius equals the Gaussian radius of curvature as above, and its radial direction coincides with the ellipsoid normal direction. The center of the osculating sphere is offset from the center of the ellipsoid, but is at the center of curvature for the given point on the ellipsoid surface. This concept aids the interpretation of terrestrial and planetary radio occultation refraction measurements and in some navigation and surveillance applications.
This table summarizes the accepted values of the Earth's radius.
|Agency||Description||Value (in meters)||Ref|
|IAU||nominal "zero tide" equatorial||378100 6|||
|IAU||nominal "zero tide" polar||356800 6|||
|IUGG||equatorial radius||378137 6|||
|IUGG||semiminor axis (b)||356752.3141 6|||
|IUGG||polar radius of curvature (c)||399593.6259 6|||
|IUGG||mean radius (R1)||371008.7714 6|||
|IUGG||radius of sphere of same surface (R2)||371007.1810 6|||
|IUGG||radius of sphere of same volume (R3)||371000.7900 6|||
|IERS||WGS-84 ellipsoid, semi-major axis (a)||378137.0 6|||
|IERS||WGS-84 ellipsoid, semi-minor axis (b)||356752.3142 6|||
|IERS||WGS-84 ellipsoid, polar radius of curvature (c)||399593.6258 6|||
|IERS||WGS-84 ellipsoid, Mean radius of semi-axes (R1)||371008.7714 6|||
|IERS||WGS-84 ellipsoid, Radius of Sphere of Equal Area (R2)||371007.1809 6|||
|IERS||WGS-84 ellipsoid, Radius of Sphere of Equal Volume (R3)||371000.7900 6|||
|GRS 80 semi-major axis (a)||378137.0 6|
|GRS 80 semi-minor axis (b)||356752.314140 ≈6|
|meridional radius of curvature at the equator||335439 6|
|Maximum (the summit of Chimborazo)||384400 6|||
|Minimum (the floor of the Arctic Ocean)||352800 6|||
|Average distance from center to surface||371230±10 6|||
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. Archived April 28, 2010, at the Wayback Machine.
- 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. Retrieved 2016-08-10.
- "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.
- "Geodesy". google.com.br.
- Moritz, H. (March 2000). "Geodetic Reference System 1980". Journal of Geodesy. 74 (1): 128–133. Bibcode:2000JGeod..74..128.. doi:10.1007/s001900050278.
- 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.
- Frédéric Chambat; Bernard Valette (2001). "Mean radius, mass, and inertia for reference Earth models" (PDF). Physics of the Earth and Planetary Interiors. 124. pp. 234–253. Retrieved 18 November 2017.
- Williams, Paul; Last, David (November 3–7, 2003). On Loran-C Time-Difference to Co-ordinate Converters (PDF). International Loran Association (ILA) - 32nd Annual Convention and Technical Symposium. Boulder, Colorado. CiteSeerX 10.1.1.594.6212.
- Razin, Sheldon (Fall 1967). "Explicit (Noniterative) Loran Solution". Navigation, Journal of the Institute of Navigation. 14 (3): 265–269.
- 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.