Moment magnitude scale
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The moment magnitude scale (abbreviated as MMS; denoted as M_{W} or M) is used by seismologists to measure the size of earthquakes in terms of the energy released.^{[1]} The magnitude is based on the seismic moment of the earthquake, which is equal to the rigidity of the Earth multiplied by the average amount of slip on the fault and the size of the area that slipped.^{[2]} The scale was developed in the 1970s to succeed the 1930sera Richter magnitude scale (M_{L}). Even though the formulae are different, the new scale retains a similar continuum of magnitude values to that defined by the older one. The MMS is now the scale used to estimate magnitudes for all modern large earthquakes by the United States Geological Survey.^{[3]}
Popular press reports of earthquake magnitude usually fail to distinguish between magnitude scales, and are often reported as "Richter magnitudes" when the reported magnitude is a Moment magnitude (or a surfacewave or body wave magnitude). Because the scales are intended to report the same results within their applicable conditions, the confusion is minor.
Contents

Historical context 1
 The Richter scale: a former measure of earthquake magnitude 1.1
 The modified Richter scale 1.2
 Correcting weaknesses of the modified Richter scale 1.3
 Current research 1.4
 Definition 2
 Comparative energy released by two earthquakes 3
 Radiated seismic energy 4
 Nuclear explosions 5
 Comparison with Richter scale 6
 See also 7
 Notes 8
 References 9
 External links 10
Historical context
The Richter scale: a former measure of earthquake magnitude
In 1935, Charles Richter and Beno Gutenberg developed the local magnitude (M_\mathrm{L}) scale (popularly known as the Richter scale) with the goal of quantifying mediumsized earthquakes (between magnitude 3.0 and 7.0) in Southern California. This scale was based on the ground motion measured by a particular type of seismometer (a WoodAnderson seismograph) at a distance of 100 kilometres (62 mi) from the earthquake's epicenter.^{[3]} Because of this, there is an upper limit on the highest measurable magnitude, and all large earthquakes will tend to have a local magnitude of around 7.^{[4]} Further, the magnitude becomes unreliable for measurements taken at a distance of more than about 600 kilometres (370 mi) from the epicenter. Since this M_{L} scale was simple to use and corresponded well with the damage which was observed, it was extremely useful for engineering earthquakeresistant structures, and gained common acceptance.^{[5]}
The modified Richter scale
Although the Richter scale represented a major step forward, it was not as effective for characterizing some classes of quakes. As a result, Beno Gutenberg expanded Richter's work to consider earthquakes detected at distant locations. For such large distances the higher frequency vibrations are attenuated and seismic surface waves (Rayleigh and Love waves) are dominated by waves with a period of 20 seconds (which corresponds to a wavelength of about 60 km). Their magnitude was assigned a surface wave magnitude scale (M_{S}). Gutenberg also combined compressional Pwaves and the transverse Swaves (which he termed "body waves") to create a bodywave magnitude scale (M_{b}), measured for periods between 1 and 10 seconds. Ultimately Gutenberg and Richter collaborated to produce a combined scale which was able to estimate the energy released by an earthquake in terms of Gutenberg's surface wave magnitude scale (M_{S}).^{[5]}
Correcting weaknesses of the modified Richter scale
The Richter Scale, as modified, was successfully applied to characterize localities. This enabled local building codes to establish standards for buildings which were earthquake resistant. However a series of quakes were poorly handled by the modified Richter scale. This series of "great earthquakes", included faults that broke along a line of up to 1000 km. Examples include the 1952 Aleutian Fox Islands quake and the 1960 Chilean quake, both of which broke faults approaching 1000 km. The M_{S} scale was unable to characterize these "great earthquakes" accurately.^{[5]}
The difficulties with use of M_{S} in characterizing the quake resulted from the size of these earthquakes. Great quakes produced 20 s waves such that M_{S} was comparable to normal quakes, but also produced very long period waves (more than 200 s) which carried large amounts of energy. As a result, use of the modified Richter scale methodology to estimate earthquake energy was deficient at high energies.^{[5]}
In 1972, Keiiti Aki, a professor of Geophysics at the Massachusetts Institute of Technology, introduced elastic dislocation theory to improve understanding of the earthquake mechanism. This theory proposed that the energy release from a quake is proportional to the surface area that breaks free, the average distance that the fault is displaced, and the rigidity of the material adjacent to the fault. This is found to correlate well with the seismologic readings from longperiod seismographs. Hence the moment magnitude scale (M_{W}) represented a major step forward in characterizing earthquakes.^{[6]}
Current research
Recent research related to the moment magnitude scale focuses on:
 Timely earthquake magnitude estimates allow for early warnings of earthquakes and tsunami. Such earthquake early warning systems are operating in Japan, Mexico, Romania, Taiwan, and Turkey and are being tested in the United States, Europe, and Asia. Such systems rely on a variety of analytic methods to attain an early estimate of the moment magnitude of a quake.^{[7]}
 Efforts are underway to extend the moment magnitude scale accuracy for high frequencies, which are important in localizing small quakes. Earthquakes below magnitude 3 scale poorly because the earth attenuates high frequency waves near the surface, making it difficult to resolve quakes smaller than 100 meters. By use of seismographs in deep wells this attenuation can be overcome.^{[8]}
Definition
The symbol for the moment magnitude scale is M_\mathrm{w}, with the subscript \mathrm{w} meaning mechanical work accomplished. The moment magnitude ^{[9]}M_\mathrm{w} is a dimensionless number defined by Hiroo Kanamori as
 M_\mathrm{w} = {\frac{2}{3}}\log_{10}(M_0)  10.7,
where M_0 is the seismic moment in dyne⋅cm (10^{7} N⋅m).^{[1]} The constant values in the equation are chosen to achieve consistency with the magnitude values produced by earlier scales, the Local Magnitude and the Surface Wave magnitude, both referred to as the "Richter" scale by reporters.
Comparative energy released by two earthquakes
As with the Richter scale, an increase of one step on this logarithmic scale corresponds to a 10^{1.5} ≈ 32 times increase in the amount of energy released, and an increase of two steps corresponds to a 10^{3} = 1000 times increase in energy. Thus, an earthquake of M_{W} of 7.0 contains 1000 times as much energy as one of 5.0 and about 32 times that of 6.0.
The following formula, obtained by solving the previous equation for M_0, allows one to assess the proportional difference f_{\Delta E} in energy release between earthquakes of two different moment magnitudes, say m_1 and m_2:
 f_{\Delta E} = 10^{\frac{3}{2}(m_1  m_2)}.
For example, an earthquake with a moment magnitude of 7.0 is approximately 5.62 times greater than a quake with moment magnitude 6.5.
Radiated seismic energy
Potential energy is stored in the crust in the form of builtup stress. During an earthquake, this stored energy is transformed and results in
 cracks and deformation in rocks
 heat
 radiated seismic energy E_s.
The seismic moment M_0 is a measure of the total amount of energy that is transformed during an earthquake. Only a small fraction of the seismic moment M_0 is converted into radiated seismic energy E_\mathrm{s}, which is what seismographs register. Using the estimate
 E_\mathrm{s} = M_0\cdot10^{4.8}=M_0\cdot1.6\times10^{5},
Choy and Boatwright defined in 1995 the energy magnitude ^{[10]}
 M_\mathrm{e} = \textstyle{\frac{2}{3}}\log_{10}E_\mathrm{s}2.9
where E_\mathrm{s} is in N.m.
Nuclear explosions
The energy released by nuclear weapons is traditionally expressed in terms of the energy stored in a kiloton or megaton of the conventional explosive trinitrotoluene (TNT).
A rule of thumb equivalence from seismology used in the study of nuclear proliferation asserts that a one kiloton nuclear explosion creates a seismic signal with a magnitude of approximately 4.0.^{[11]} This in turn leads to the equation^{[12]}
 M_n = \textstyle\frac{2}{3}\displaystyle\log_{10} \frac{m_{\mathrm{TNT}}}{\mbox{Mt}} + 6,
where m_{\mathrm{TNT}} is the mass of the explosive TNT that is quoted for comparison (relative to megatons Mt).
Such comparison figures are not very meaningful. As with earthquakes, during an underground explosion of a nuclear weapon, only a small fraction of the total amount of energy released ends up being radiated as seismic waves. Therefore, a seismic efficiency needs to be chosen for the bomb that is being quoted in this comparison. Using the conventional specific energy of TNT (4.184 MJ/kg), the above formula implies that about 0.5% of the bomb's energy is converted into radiated seismic energy E_s.^{[13]} For real underground nuclear tests, the actual seismic efficiency achieved varies significantly and depends on the site and design parameters of the test.
Comparison with Richter scale
The moment magnitude (M_\mathrm{w}) scale was introduced in 1979 by Caltech seismologists Thomas C. Hanks and Hiroo Kanamori to address the shortcomings of the Richter scale (detailed above) while maintaining consistency. Thus, for mediumsized earthquakes, the moment magnitude values should be similar to Richter values. That is, a magnitude 5.0 earthquake will be about a 5.0 on both scales. This scale was based on the physical properties of the earthquake, specifically the seismic moment (M_0). Unlike other scales, the moment magnitude scale does not saturate at the upper end; there is no upper limit to the possible measurable magnitudes. However, this has the sideeffect that the scales diverge for smaller earthquakes.^{[1]}
The concept of seismic moment was introduced in 1966,^{[14]} but it took 13 years before the M_\mathrm{w} scale was designed. The reason for the delay was that the necessary spectra of seismic signals had to be derived by hand at first, which required personal attention to every event. Faster computers than those available in the 1960s were necessary and seismologists had to develop methods to process earthquake signals automatically. In the mid1970s Dziewonski^{[15]} started the Harvard Global Centroid Moment Tensor Catalog.^{[16]} After this advance, it was possible to introduce M_\mathrm{w} and estimate it for large numbers of earthquakes.
Moment magnitude is now the most common measure for medium to large earthquake magnitudes,^{[17]} but breaks down for smaller quakes. For example, the United States Geological Survey does not use this scale for earthquakes with a magnitude of less than 3.5, which is the great majority of quakes.
Magnitude scales differ from earthquake intensity, which is the perceptible shaking, and local damage experienced during a quake. The shaking intensity at a given spot depends on many factors, such as soil types, soil sublayers, depth, type of displacement, and range from the epicenter (not counting the complications of building engineering and architectural factors). Rather, magnitude scales are used to estimate with one number the size of the quake.
The following table compares magnitudes towards the upper end of the Richter Scale for major Californian earthquakes.^{[1]}^{[18]}
Date  Seismic moment M_0\times10^{25} (dynecm)  Richter scale M_\mathrm{L}  Moment magnitude M_\mathrm{w} 

19330311  2  6.3  6.2 
19400519  30  6.4  7.0 
19410701  0.9  5.9  6.0 
19421021  9  6.5  6.6 
19460315  1  6.3  6.0 
19470410  7  6.2  6.5 
19481204  1  6.5  6.0 
19520721  200  7.2  7.5 
19540319  4  6.2  6.4 
See also
Notes
 ^ ^{a} ^{b} ^{c} ^{d}
 ^ "Glossary of Terms on Earthquake Maps".
 ^ ^{a} ^{b} "USGS Earthquake Magnitude Policy (implemented on January 18, 2002)".
 ^ "On Earthquake Magnetudes".
 ^ ^{a} ^{b} ^{c} ^{d} Hiroo Kanamori, 1978, Quantification of Earthquakes, Nature 271, 411414 doi:10.1038/271411a0
 ^ K. Aki; Earthquake Mechanism; Tectonophysics; Elsevier B.V.; Vol 13, pages 423446
 ^ Caprio, M., M. Lancieri, G. B. Cua, A. Zollo, and S. Wiemer (2011), An evolutionary approach to realtime moment magnitude estimation via inversion of displacement spectra, Geophys. Res. Lett., 38, L02301, doi:10.1029/2010GL045403.
 ^ Abercrombie, R. E.; Earthquake source scaling relationships from 1 to 5 using seismograms recorded at a 2.5 km depth; Journal of Geophysical Research, Vol. 100, No. B12, p. 24, 01524, 036, 1995
 ^ Hiroo Kanamori, 1977, The energy release in great earthquakes. Journal of geophysical research, 82(20), 29812987.
 ^ Choy, George L.; Boatwright, John L. (1995), "Global patterns of radiated seismic energy and apparent stress", Journal of Geophysical Research 100 (B9): 18205–28,
 ^ "Nuclear Testing and Nonproliferation", "Chapter 5: Assessing Monitoring Requirements"
 ^ "Nevada Seismological Lab".
 ^ Q: How much energy is released in an earthquake?
 ^
 ^ Dziewonski, A. M.; Gilbert, F. (1976). "The effect of small aspherical perturbations on travel times and a reexamination of the corrections for ellipticity". Geophys. J. R. Astr. Soc. 44 (1): 7–17.
 ^ "Global Centroid Moment Tensor Catalog". Globalcmt.org. Retrieved 20111130.
 ^ Boyle, Alan (May 12, 2008). "Quakes by the numbers".
 ^ "Upper end magnitudes comparison" Fxsolver
References
 Utsu, T (2002). Lee, W.H.K.; Kanamori, H.; Jennings, P.C.; Kisslinger, C., eds. "Relationships between magnitude scales". International Handbook of Earthquake and Engineering Seismology. International Geophysics (Academic Press, a division of Elsevier) A (81): 733–46.
External links
 USGS: Measuring earthquakes
 Earthquake Energy Calculator with seismic energy approximated in everyday equivalent measures.
