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Free-air gravity anomaly

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Circular free-air gravity anomaly over the Chicxulub Crater

In geophysics, the free-air gravity anomaly, often simply called the free-air anomaly, is the measured gravity anomaly after a free-air correction is applied to account for the elevation at which a measurement is made. It does so by adjusting these measurements of gravity to what would have been measured at a reference level, which is commonly taken as mean sea level or the geoid.

Applications

Studies of the subsurface structure and composition of the Earth's crust and mantle employ surveys using gravimeters to measure the departure of observed gravity from a theoretical gravity value to identify anomalies due to geologic features below the measurement locations. The computation of anomalies from observed measurements involves the application of corrections that define the resulting anomaly. The free-air anomaly can be used to test for isostatic equilibrium over broad regions.

Survey methods

The free-air correction adjusts measurements of gravity to what would have been measured at mean sea level, that is, on the geoid. The gravitational attraction of Earth below the measurement point and above mean sea level is ignored and it is imagined that the observed gravity is measured in air, hence the name. The theoretical gravity value at a location is computed by representing the Earth as an ellipsoid that approximates the more complex shape of the geoid. Gravity is computed on the ellipsoid surface using the International Gravity Formula.

For studies of subsurface structure, the free-air anomaly is further adjusted by a correction for the mass below the measurement point and above the reference of mean sea level or a local datum elevation. This defines the Bouguer anomaly.

Calculation

The free-air gravity anomaly g F {\displaystyle g_{F}} is given by the equation:

g F = ( g o b s + δ g F ) − g λ {\displaystyle g_{F}=(g_{obs}+\delta g_{F})-g_{\lambda }}

Here, g o b s {\displaystyle g_{obs}} is observed gravity, δ g F {\displaystyle \delta g_{F}} is the free-air correction, and g λ {\displaystyle g_{\lambda }} is theoretical gravity.

It can be helpful to think of the free-air anomaly as comparing observed gravity to theoretical gravity adjusted up to the measurement point instead of observed gravity adjusted down to the geoid. This avoids any confusion of assuming that the measurement is made in free air. Either way, however, the Earth mass between the observation point and the geoid is neglected. The equation for this approach is simply rearranging terms in the first equation of this section so that reference gravity is adjusted and not the observed gravity:

g F = g o b s − ( g λ − δ g F ) {\displaystyle g_{F}=g_{obs}-(g_{\lambda }-\delta g_{F})}

Correction

Gravitational acceleration decreases as an inverse square law with the distance at which the measurement is made from the mass. The free air correction is calculated from Newton's Law, as a rate of change of gravity with distance:

g = G M R 2 d g d R = − 2 G M R 3 = − 2 g R {\displaystyle {\begin{aligned}g&={\frac {GM}{R^{2}}}\\{\frac {dg}{dR}}&=-{\frac {2GM}{R^{3}}}=-{\frac {2g}{R}}\end{aligned}}}

At 45° latitude, 2 g / R = 0.3086 {\displaystyle 2g/R=0.3086} mGal/m.

The free-air correction is the amount that must be added to a measurement at height h {\displaystyle h} to correct it to the reference level:

δ g F = 2 g R × h {\displaystyle \delta g_{F}={\frac {2g}{R}}\times h}

Here we have assumed that measurements are made relatively close to the surface so that R does not vary significantly. The value of the free-air correction is positive when measured above the geoid, and negative when measured below. There is the assumption that no mass exists between the observation point and the reference level. The Bouguer and terrain corrections are used to account for this.

Significance

Over the ocean where gravity is measured from ships near sea level, there is no or little free-air correction. In marine gravity surveys, it was observed that the free-air anomaly is positive but very small over the Mid-Ocean Ridges in spite of the fact that these features rise several kilometers above the surrounding seafloor. The small anomaly is explained by the lower density crust and mantle below the ridges resulting from seafloor spreading.  This lower density is an apparent offset to the extra height of the ridge indicating that Mid-Ocean Ridges are in isostatic equilibrium.

See also

References

  1. ^ Fowler, C.M.R. (2005). The Solid Earth: An Introduction to Global Geophysics (2 ed.). Cambridge, UK: Cambridge University Press. pp. 205–206. ISBN 978-0-521-89307-7.
  2. Water Resources Division, U. S. Geological Survey (1997). "Introduction to Potential Fields: Gravity" (PDF). U.S. Geological Survey Fact Sheets. Fact Sheet. FS–239–95: 19. Bibcode:1997usgs.rept...19W. doi:10.3133/fs23995. Retrieved 30 May 2019.
  3. ^ Telford, W.M.; Geldart, L.P.; Sheriff, R.E. (1990). Applied Geophysics (2nd ed.). Cambridge: Cambridge University Press. pp. 11–12. ISBN 978-0-521-32693-3.
  4. Ervin, C. Patrick (December 1977). "Theory of the Bouguer Anomaly". Geophysics. 42 (7): 1468. Bibcode:1977Geop...42.1468E. doi:10.1190/1.1440807. ISSN 0016-8033.
  5. Lillie, R.J. (1998). Whole Earth Geophysics: An Introductory Textbook for Geologists and Geophysicists. Prentice Hall. ISBN 978-0-13-490517-4.
  6. Cochran, James R.; Talwani, Manik (1977-09-01). "Free-air gravity anomalies in the world's oceans and their relationship to residual elevation". Geophysical Journal International. 50 (3): 495–552. Bibcode:1977GeoJ...50..495C. doi:10.1111/j.1365-246X.1977.tb01334.x. ISSN 0956-540X.
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