Gravity of Earth

File:Gravity anomalies on Earth.jpg

Earth's gravity measured by NASA GRACE mission, showing deviations from the theoretical gravity of an idealized, smooth Earth, the so-called Earth ellipsoid. Red shows the areas where gravity is stronger than the smooth, standard value, and blue reveals areas where gravity is weaker.

The gravity of Earth, denoted by Template:Mvar, is the net acceleration that is imparted to objects due to the combined effect of gravitation (from mass distribution within Earth) and the centrifugal force (from the Earth's rotation). It is a vector quantity, whose direction coincides with a plumb bob and strength or magnitude is given by the norm $g=\Vert \mathbf{𝐠}\Vert$.

In SI units, this acceleration is expressed in metres per second squared (in symbols, m/s² or m·s⁻²) or equivalently in newtons per kilogram (N/kg or N·kg⁻¹). Near Earth's surface, the acceleration due to gravity, accurate to 2 significant figures, is . This means that, ignoring the effects of air resistance, the speed of an object falling freely will increase by about every second.

The precise strength of Earth's gravity varies with location. The agreed-upon value for standard gravity is by definition. This quantity is denoted variously as g_n, g_e (though this sometimes means the normal gravity at the equator, ), g₀, or simply Template:Mvar (which is also used for the variable local value).

The weight of an object on Earth's surface is the downwards force on that object, given by Newton's second law of motion, or F = m a (force = mass × acceleration). Gravitational acceleration contributes to the total gravity acceleration, but other factors, such as the rotation of Earth, also contribute, and, therefore, affect the weight of the object. Gravity does not normally include the gravitational pull of the Moon and Sun, which are accounted for in terms of tidal effects.

Variation in magnitude

A non-rotating perfect sphere of uniform mass density, or whose density varies solely with distance from the centre (spherical symmetry), would produce a gravitational field of uniform magnitude at all points on its surface. The Earth is rotating and is also not spherically symmetric; rather, it is slightly flatter at the poles while bulging at the Equator: an oblate spheroid. There are consequently slight deviations in the magnitude of gravity across its surface.

Gravity on the Earth's surface varies by around 0.7%, from 9.7639 m/s² on the Nevado Huascarán mountain in Peru to 9.8337 m/s² at the surface of the Arctic Ocean. In large cities, it ranges from 9.7806 m/s² in Kuala Lumpur, Mexico City, and Singapore to 9.825 m/s² in Oslo and Helsinki.

Conventional value

In 1901, the third General Conference on Weights and Measures defined a standard gravitational acceleration for the surface of the Earth: g_n = 9.80665 m/s². It was based on measurements at the Pavillon de Breteuil near Paris in 1888, with a theoretical correction applied in order to convert to a latitude of 45° at sea level. This definition is thus not a value of any particular place or carefully worked out average, but an agreement for a value to use if a better actual local value is not known or not important. It is also used to define the units kilogram force and pound force.

Latitude

File:Southern ocean gravity hg.png

The differences of Earth's gravity around the Antarctic continent.

The surface of the Earth is rotating, so it is not an inertial frame of reference. At latitudes nearer the Equator, the outward centrifugal force produced by Earth's rotation is larger than at polar latitudes. This counteracts the Earth's gravity to a small degree – up to a maximum of 0.3% at the Equator – and reduces the apparent downward acceleration of falling objects.

The second major reason for the difference in gravity at different latitudes is that the Earth's equatorial bulge (itself also caused by centrifugal force from rotation) causes objects at the Equator to be further from the planet's center than objects at the poles. The force due to gravitational attraction between two masses (a piece of the Earth and the object being weighed) varies inversely with the square of the distance between them. The distribution of mass is also different below someone on the equator and below someone at a pole. The net result is that an object at the Equator experiences a weaker gravitational pull than an object on one of the poles.

In combination, the equatorial bulge and the effects of the surface centrifugal force due to rotation mean that sea-level gravity increases from about 9.780 m/s² at the Equator to about 9.832 m/s² at the poles, so an object will weigh approximately 0.5% more at the poles than at the Equator.

Altitude

The gravity of a body is inversely proportional to the distance form that body. This graph displays this relation as the distance changes from the surface (Script error: No such module "val".) to Script error: No such module "val"..

Earth's gravity vs. distance from it, from the surface to

File:Earth vs Mars gravity at elevation.webp

Earth vs Mars vs Moon gravity at elevation

Gravity decreases with altitude as one rises above the Earth's surface because greater altitude means greater distance from the Earth's centre. All other things being equal, an increase in altitude from sea level to causes a weight decrease of about 0.29%. An additional factor affecting apparent weight is the decrease in air density at altitude, which lessens an object's buoyancy. This would increase a person's apparent weight at an altitude of 9,000 metres by about 0.08%.

It is a common misconception that astronauts in orbit are weightless because they have flown high enough to escape the Earth's gravity. In fact, at an altitude of , equivalent to a typical orbit of the ISS, gravity is still nearly 90% as strong as at the Earth's surface. Weightlessness actually occurs because orbiting objects are in free-fall.

The effect of ground elevation depends on the density of the ground (see Local geology). A person flying at Template:Cvt above sea level over mountains will feel more gravity than someone at the same elevation but over the sea. However, a person standing on the Earth's surface feels less gravity when the elevation is higher.

The following formula approximates the Earth's gravity variation with altitude:

Calculator

Re	6,371.00877 km
g0	9.80665 m/s2
Template:Calculator label	Template:Calculator km
gh	Template:Calculator m/s2

$g_h=g_0{\left(\frac{R_{\mathrm{e}}}{R_{\mathrm{e}}+h}\right)}^2$

where

• g_h is the gravitational acceleration at height Template:Mvar above sea level.
• R_e is the Earth's mean radius.
• g₀ is the standard gravitational acceleration.

The formula treats the Earth as a perfect sphere with a radially symmetric distribution of mass; a more accurate mathematical treatment is discussed below.

Depth

File:Earth-G-force.png

Gravity at different internal layers of Earth (1 = continental crust, 2 = oceanic crust, 3 = upper mantle, 4 = lower mantle, 5+6 = core, A = crust-mantle boundary)

File:RadialDensityPREM.jpg

Earth's radial density distribution according to the Preliminary Reference Earth Model (PREM).

File:EarthGravityPREM.svg

Earth's gravity according to the Preliminary Reference Earth Model (PREM). Two models for a spherically symmetric Earth are included for comparison. The dark green straight line is for a constant density equal to the Earth's average density. The light green curved line is for a density that decreases linearly from center to surface. The density at the center is the same as in the PREM, but the surface density is chosen so that the mass of the sphere equals the mass of the real Earth.

An approximate value for gravity at a distance Template:Mvar from the center of the Earth can be obtained by assuming that the Earth's density is spherically symmetric. The force of gravity at a radius Template:Mvar depends only on the mass inside the sphere of that radius. All the contributions from outside cancel out as a consequence of the inverse-square law of gravitation. Another consequence is that the gravity is the same as if all the mass were concentrated at the center. Thus, the gravitational acceleration at this radius is

$g(r)=-\frac{GM(r)}{r^2}.$

where Template:Mvar is the gravitational constant and M(r) is the total mass enclosed within radius Template:Mvar. This result is known as the Shell theorem; it took Isaac Newton 20 years to prove this result, delaying his work on gravity.Template:Rp

If the Earth had a constant density Template:Mvar, the mass would be M(r) = (4/3)πρr³ and the dependence of gravity on depth would be

$g(r)=\frac{4\pi }{3}G\rho r.$

The gravity g′ at depth Template:Mvar is given by g′ = g(1 − d/R) where Template:Mvar is acceleration due to gravity on the surface of the Earth, Template:Mvar is depth and Template:Mvar is the radius of the Earth. If the density decreased linearly with increasing radius from a density ρ₀ at the center to ρ₁ at the surface, then ρ(r) = ρ₀ − (ρ₀ − ρ₁) r / R, and the dependence would be

$g(r)=\frac{4\pi }{3}G{\rho }_{0}r-\pi G({\rho }_0-{\rho }_1)\frac{r^2}{R}.$

The actual depth dependence of density and gravity, inferred from seismic travel times (see Adams–Williamson equation), is shown in the graphs below.

Local topography and geology

Local differences in topography (such as the presence of mountains), geology (such as the density of rocks in the vicinity), and deeper tectonic structure cause local and regional differences in the Earth's gravitational field, known as gravity anomalies. Some of these anomalies can be very extensive, resulting in bulges in sea level, and throwing pendulum clocks out of synchronisation.

The study of these anomalies forms the basis of gravitational geophysics. The fluctuations are measured with highly sensitive gravimeters, the effect of topography and other known factors is subtracted, and from the resulting data conclusions are drawn. Such techniques are now used by prospectors to find oil and mineral deposits. Denser rocks (often containing mineral ores) cause higher than normal local gravitational fields on the Earth's surface. Less dense sedimentary rocks cause the opposite.

File:Spreading ridges volcanoes map-en.svg

A map of recent volcanic activity and ridge spreading. The areas where NASA GRACE measured gravity to be stronger than the theoretical gravity have a strong correlation with the positions of the volcanic activity and ridge spreading.

There is a strong correlation between the gravity derivation map of earth from NASA GRACE with positions of recent volcanic activity, ridge spreading and volcanos: these regions have a stronger gravitation than theoretical predictions.

Other factors

In air or water, objects experience a supporting buoyancy force which reduces the apparent strength of gravity (as measured by an object's weight). The magnitude of the effect depends on the air density (and hence air pressure) or the water density respectively; see Apparent weight for details.

The gravitational effects of the Moon and the Sun (also the cause of the tides) have a very small effect on the apparent strength of Earth's gravity, depending on their relative positions; typical variations are 2 μm/s² (0.2 mGal) over the course of a day.

Direction

File:Plumb bob.jpg

A plumb bob determines the local vertical direction

Gravity acceleration is a vector quantity, with direction in addition to magnitude. In a spherically symmetric Earth, gravity would point directly towards the sphere's centre. As the Earth's figure is slightly flatter, there are consequently significant deviations in the direction of gravity: essentially the difference between geodetic latitude and geocentric latitude. Smaller deviations, called vertical deflection, are caused by local mass anomalies, such as mountains.

Comparative values worldwide

Tools exist for calculating the strength of gravity at various cities around the world. The effect of latitude can be clearly seen with gravity in high-latitude cities: Anchorage (9.826 m/s²), Helsinki (9.825 m/s²), being about 0.5% greater than that in cities near the equator: Kuala Lumpur (9.776 m/s²). The effect of altitude can be seen in Mexico City (9.776 m/s²; altitude ), and by comparing Denver (9.798 m/s²; ) with Washington, D.C. (9.801 m/s²; ), both of which are near 39° N. Measured values can be obtained from Physical and Mathematical Tables by T.M. Yarwood and F. Castle, Macmillan, revised edition 1970.

Mathematical models

If the terrain is at sea level, we can estimate, for the Geodetic Reference System 1980, $g\{\varphi \}$, the acceleration at latitude $\varphi$:

$\begin{array}{rl}g\{\varphi \}& =9.780327\mathrm{m}\cdot {\mathrm{s}}^{-2}(1+0.0053024{\sin }^2\varphi -0.0000058{\sin }^{2}2\varphi ),\\ & =9.780327\mathrm{m}\cdot {\mathrm{s}}^{-2}(1+0.0052792{\sin }^2\varphi +0.0000232{\sin }^4\varphi ),\\ & =9.780327\mathrm{m}\cdot {\mathrm{s}}^{-2}(1.0053024-0.0053256{\cos }^2\varphi +0.0000232{\cos }^4\varphi ),\\ & =9.780327\mathrm{m}\cdot {\mathrm{s}}^{-2}(1.0026454-0.0026512\cos 2\varphi +0.0000058{\cos }^{}2\varphi )\end{array}$

This is the International Gravity Formula 1967, the 1967 Geodetic Reference System Formula, Helmert's equation or Clairaut's formula.

An alternative formula for g as a function of latitude is the WGS (World Geodetic System) 84 Ellipsoidal Gravity Formula:

$g\{\varphi \}={\mathbb{𝔾}}_e\left[\frac{1+k{\sin }^2\varphi }{\sqrt{1-e^2{\sin }^2\varphi }}\right],$

where

• $a,b$ are the equatorial and polar semi-axes, respectively;
• $e^2=1-(b/a{)}^2$ is the spheroid's eccentricity, squared;
• ${\mathbb{𝔾}}_e,{\mathbb{𝔾}}_p$ is the defined gravity at the equator and poles, respectively;
• $k=\frac{b{\mathbb{𝔾}}_p-a{\mathbb{𝔾}}_e}{a{\mathbb{𝔾}}_e}$ (formula constant);

then, where ${\mathbb{𝔾}}_p=9.8321849378\mathrm{m}\cdot {\mathrm{s}}^{-2}$,

$g\{\varphi \}=9.7803253359\mathrm{m}\cdot {\mathrm{s}}^{-2}\left[\frac{1+0.001931852652{\sin }^2\varphi }{\sqrt{1-0.0066943799901{\sin }^2\varphi }}\right]$

where the semi-axes of the earth are:

$a=6378137.0\mathrm{m}$

$b=6356752.314245\mathrm{m}$

The difference between the WGS-84 formula and Helmert's equation is less than 0.68 μm·s⁻².

Further reductions are applied to obtain gravity anomalies (see: Gravity anomaly#Computation).

Estimating g from the law of universal gravitation

From the law of universal gravitation, the force on a body acted upon by Earth's gravitational force is given by

$F=G\frac{m_1{m}_2}{r^2}=\left(G\frac{M_{\oplus }}{r^2}\right)m$

where r is the distance between the centre of the Earth and the body (see below), and here we take $M_{\oplus }$ to be the mass of the Earth and m to be the mass of the body.

Additionally, Newton's second law, F = ma, where m is mass and a is acceleration, here tells us that

$F=mg$

Comparing the two formulas it is seen that:

$g=G\frac{M_{\oplus }}{r^2}$

So, to find the acceleration due to gravity at sea level, substitute the values of the gravitational constant, G, the Earth's mass (in kilograms), m₁, and the Earth's radius (in metres), r, to obtain the value of g:

$g=G\frac{M_{\oplus }}{r^2}=6.674\times 10^{-11}{\mathrm{m}}^{\mathrm{3}}\mathrm{\cdot }{\mathrm{k}\mathrm{g}}^{\mathrm{-}\mathrm{1}}\mathrm{\cdot }{\mathrm{s}}^{\mathrm{-}\mathrm{2}}\times \frac{6\times 10^{24}\mathrm{k}\mathrm{g}}{(6.4\times 10^6\mathrm{m}{)}^2}\approx 9.77637\mathrm{m}\mathrm{\cdot }{\mathrm{s}}^{\mathrm{-}\mathrm{2}}$

This formula only works because of the mathematical fact that the gravity of a uniform spherical body, as measured on or above its surface, is the same as if all its mass were concentrated at a point at its centre. This is what allows us to use the Earth's radius for r.

The value obtained agrees approximately with the measured value of g. The difference may be attributed to several factors, mentioned above under "Variation in magnitude":

• The Earth is not homogeneous
• The Earth is not a perfect sphere, and an average value must be used for its radius
• This calculated value of g only includes true gravity. It does not include the reduction of constraint force that we perceive as a reduction of gravity due to the rotation of Earth, and some of gravity being counteracted by centrifugal force.

There are significant uncertainties in the values of r and m₁ as used in this calculation, and the value of G is also rather difficult to measure precisely.

If G, g and r are known then a reverse calculation will give an estimate of the mass of the Earth. This method was used by Henry Cavendish.

Measurement

The measurement of Earth's gravity is called gravimetry.

See also

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External links

• Altitude gravity calculator
• GRACE – Gravity Recovery and Climate Experiment Template:Webarchive
• GGMplus high resolution data (2013)
• Geoid 2011 model Potsdam Gravity Potato