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Not to be confused with Gravitational anomaly.

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A **gravity anomaly** is the difference between the observed acceleration of a planet's gravity and a value predicted from a model. A location with a positive anomaly exhibits more gravity than predicted, while a negative anomaly exhibits a lower value than predicted. The anomaly is the body or effect that causes the deviation from the "ideal" gravity model. Many data corrections must be made to the measured gravity value in order to extract the response of the local anomaly, or local geology, which is typically the goal of applied geophysics.

Lateral variations in gravity anomalies are related to anomalous density distributions within the Earth. Gravity measures help us to understand the internal structure of the planet. Synthetic calculations show that the gravity anomaly signature of a thickened crust (for example, in orogenic belts produced by continental collision) is negative and larger in absolute value, relative to a case where thickening affects the entire lithosphere.

The Bouguer anomalies usually are negative in the mountains because of isostasy: the rock density of their roots is lower, compared with the surrounding earth's mantle. Typical anomalies in the Central Alps are −150 milligals (−1.5 mm/s²). Rather local anomalies are used in applied geophysics: if they are positive, this may indicate metallic ores. At scales between entire mountain ranges and ore bodies, Bouguer anomalies may indicate rock types. For example, the northeast-southwest trending high across central New Jersey (see figure) represents a graben of Triassic age largely filled with dense basalts. Salt domes are typically expressed in gravity maps as lows, because salt has a low density compared to the rocks the dome intrudes. Anomalies can help to distinguish sedimentary basins whose fill differs in density from that of the surrounding region - see Gravity Anomalies of Britain and Ireland for example.

In geodesy and geophysics, the usual theoretical model is the gravity on the surface of a reference ellipsoid such as WGS84.

To understand the nature of the gravity anomaly due to the subsurface, a number of corrections must be made to the measured gravity value:

- The
*theoretical gravity*(smoothed normal gravity) should be removed in order to leave only local effects. - The elevation of the point where each gravity measurement was taken must be reduced to a reference datum to compare the whole profile. This is called the
*Free-air Correction*, and when combined with the removal of theoretical gravity leaves the free-air anomaly . - the normal gradient of gravity (rate of change of gravity by change of elevation), as in free air, usually 0.3086 milligals per meter, or the
*Bouguer gradient*of 0.1967 mGal/m (19.67 µm/(s²·m) which considers the mean rock density (2.67 g/cm³) beneath the point; this value is found by subtracting the gravity due to the Bouguer plate, which is 0.1119 mGal/m (11.19 µm/(s²·m)) for this density. Simply, we have to correct for the effects of any material between the point where gravimetry was done and the geoid. To do this we model the material in between as being made up of an infinite number of slabs of thickness*t*. These slabs have no lateral variation in density, but each slab may have a different density than the one above or below it. This is called the*Bouguer correction*. - and (in special cases) a digital terrain model (DTM). A terrain correction, computed from a model structure, accounts for the effects of rapid lateral change in density, e.g. edge of plateau, cliffs, steep mountains, etc.

For these reductions, different methods are used:

- The gravity changes as we move away from the surface of the Earth. For this reason, we must compensate with the free air anomaly.
**free-air anomaly**(or Faye^{[disambiguation needed]}'s anomaly): application of the*normal gradient*0.3086 mGal/m, but no terrain model. This anomaly means a downward shift of the point, together with the whole shape of the terrain. This simple method is ideal for many geodetic applications. - simple Bouguer anomaly: downward reduction just by the Bouguer gradient (0.1967). This anomaly handles the point as if it is located on a flat plain.
**refined**(or**complete**) Bouguer anomaly (usual abbreviation Δ*g*_{B}): the DTM is considered as accurate as possible, using a standard density of 2.67 g/cm³ (granite, limestone). Bouguer anomalies are ideal for geophysics because they show the effects of different rock densities in the subsurface.- The difference between the two - the differential gravitational effect of the unevenness of the terrain - is called the terrain effect. It is always negative (up to 100 milligals).
- The difference between
*Faye anomaly*and Δ*g*_{B}is called*Bouguer reduction*(attraction of the terrain).

**special methods**like that of Poincare-Prey, using an interior gravity gradient of about 0.009 milligal per meter (90 nm/(s²·m)). These methods are valid for the gravity within boreholes or for special geoid computations.

Large-scale gravity anomalies can be detected from space. The Gravity Recovery and Climate Experiment (GRACE) consists of two satellites that can detect gravitational changes across the Earth.

Any region of space with higher than expected mass density will produce a gravity anomaly. Observations of gravity anomalies on galactic and intergalactic scales lead to the assumption of dark matter.