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Characteristics |

The **moment magnitude scale** (**MMS**; denoted explicitly with **M _{w} ** or

- History
- Richter scale: the original measure of earthquake magnitude
- Single couple or double couple
- Dislocation theory
- Seismic moment
- Introduction of an energy-motivated magnitude Mw
- Moment magnitude scale
- Current use
- Definition
- Relations between seismic moment, potential energy released and radiated energy
- Comparative energy released by two earthquakes
- Subtypes of Mw
- See also
- Notes
- Sources
- External links

Moment magnitude (M_{w} ) is considered the authoritative magnitude scale for ranking earthquakes by size.^{ [3] } It is more directly related to the energy of an earthquake than other scales, and does not saturate—that is, it does not underestimate magnitudes as other scales do in certain conditions.^{ [4] } It has become the standard scale used by seismological authorities like the U.S. Geological Survey ^{ [5] } for reporting large earthquakes (typically M > 4), replacing the local magnitude (M_{L} ) and surface wave magnitude (M_{s} ) scales. Subtypes of the moment magnitude scale (M_{ww} , etc.) reflect different ways of estimating the seismic moment.

At the beginning of the twentieth century, very little was known about how earthquakes happen, how seismic waves are generated and propagate through the earth's crust, and what information they carry about the earthquake rupture process; the first magnitude scales were therefore empirical.^{ [6] } The initial step in determining earthquake magnitudes empirically came in 1931 when the Japanese seismologist Kiyoo Wadati showed that the maximum amplitude of an earthquake's seismic waves diminished with distance at a certain rate.^{ [7] } Charles F. Richter then worked out how to adjust for epicentral distance (and some other factors) so that the logarithm of the amplitude of the seismograph trace could be used as a measure of "magnitude" that was internally consistent and corresponded roughly with estimates of an earthquake's energy.^{ [8] } He established a reference point and the now familiar ten-fold (exponential) scaling of each degree of magnitude, and in 1935 published what he called the "magnitude scale", now called the local magnitude scale, labeled M_{L} .^{ [9] } (This scale is also known as the *Richter scale*, but news media sometimes use that term indiscriminately to refer to other similar scales.)

The local magnitude scale was developed on the basis of shallow (~15 km (9 mi) deep), moderate-sized earthquakes at a distance of approximately 100 to 600 km (62 to 373 mi), conditions where the surface waves are predominant. At greater depths, distances, or magnitudes the surface waves are greatly reduced, and the local magnitude scale underestimates the magnitude, a problem called *saturation*. Additional scales were developed^{ [10] } – a surface-wave magnitude scale (M_{s} ) by Beno Gutenberg in 1945^{ [11] }, a body-wave magnitude scale (mB ) by Gutenberg and Richter in 1956,^{ [12] } and a number of variants^{ [13] } – to overcome the deficiencies of the M_{L} scale, but all are subject to saturation. A particular problem was that the M_{s} scale (which in the 1970s was the preferred magnitude scale) saturates around M_{s} 8.0 and therefore underestimates the energy release of "great" earthquakes^{ [14] } such as the 1960 Chilean and 1964 Alaskan earthquakes. These had M_{s} magnitudes of 8.5 and 8.4 respectively but were notably more powerful than other M 8 earthquakes; their moment magnitudes were closer to 9.6 and 9.3.^{ [15] }

The study of earthquakes is challenging as the source events cannot be observed directly, and it took many years to develop the mathematics for understanding what the seismic waves from an earthquake can tell us about the source event. An early step was to determine how different systems of forces might generate seismic waves equivalent to those observed from earthquakes.^{ [16] }

The simplest force system is a single force acting on an object. If it has sufficient strength to overcome any resistance it will cause the object to move ("translate"). A pair of forces, acting on the same "line of action" but in opposite directions, will cancel; if they cancel (balance) exactly there will be no net translation, though the object will experience stress, either tension or compression. If the pair of forces are offset, acting along parallel but separate lines of action, the object experiences a rotational force, or torque. In mechanics (the branch of physics concerned with the interactions of forces) this model is called a * couple *, also *simple couple* or *single couple*. If a second couple of equal and opposite magnitude is applied their torques cancel; this is called a *double couple*.^{ [17] } A double couple can be viewed as "equivalent to a pressure and tension acting simultaneously at right angles".^{ [18] }

The single couple and double couple models are important in seismology because each can be used to derive how the seismic waves generated by an earthquake event should appear in the "far field" (that is, at distance). Once that relation is understood it can be inverted to use the earthquake's observed seismic waves to determine its other characteristics, including fault geometry and seismic moment.^{ [19] }

In 1923 Hiroshi Nakano showed that certain aspects of seismic waves could be explained in terms of a double couple model.^{ [20] } This led to a three-decade long controversy over the best way to model the seismic source: as a single couple, or a double couple?^{ [21] } While Japanese seismologists favored the double couple, most seismologists favored the single couple.^{ [22] } Although the single couple model had some short-comings, it seemed more intuitive, and there was a belief – mistaken, as it turned out – that the elastic rebound theory for explaining why earthquakes happen required a single couple model.^{ [23] } In principle these models could be distinguished by differences in the radiation patterns of their S-waves, but the quality of the observational data was inadequate for that.^{ [24] }

The debate ended when Maruyama (1963), Haskell (1964), and Burridge & Knopoff (1964) showed that if earthquake ruptures are modeled as dislocations the pattern of seismic radiation can always be matched with an equivalent pattern derived from a double couple, but not from a single couple.^{ [25] } This was confirmed as better and more plentiful data coming from the World-Wide Standard Seismograph Network (WWSSN) permitted closer analysis of seismic waves. Notably, in 1966 Keiiti Aki showed that the seismic moment of the 1964 Niigata earthquake as calculated from the seismic waves on the basis of a double couple was in reasonable agreement with the seismic moment calculated from the observed physical dislocation.^{ [26] }

A double couple model suffices to explain an earthquake's far-field pattern of seismic radiation, but tells us very little about the nature of an earthquake's source mechanism or its physical features.^{ [27] } While slippage along a fault was theorized as the cause of earthquakes (other theories included movement of magma, or sudden changes of volume due to phase changes^{ [28] }), observing this at depth was not possible, and understanding what could be learned about the source mechanism from the seismic waves requires an understanding of the source mechanism.^{ [29] }

Modeling the physical process by which an earthquake generates seismic waves required much theoretical development of dislocation theory, first formulated by the Italian Vito Volterra in 1907, with further developments by E. H. Love in 1927.^{ [30] } More generally applied to problems of stress in materials,^{ [31] } an extension by F. Nabarro in 1951 was recognized by the Russian geophysicist A. V. Vvedenskaya as applicable to earthquake faulting.^{ [32] } In a series of papers starting in 1956 she and other colleagues used dislocation theory to determine part of an earthquake's focal mechanism, and to show that a dislocation – a rupture accompanied by slipping — was indeed equivalent to a double couple,^{ [33] }

In a pair of papers in 1958, J. A. Steketee worked out how to relate dislocation theory to geophysical features.^{ [34] } Numerous other researchers worked out other details,^{ [35] } culminating in a general solution in 1964 by Burridge and Knopoff, which established the relationship between double couples and the theory of elastic rebound, and provided the basis for relating an earthquake's physical features to seismic moment.^{ [36] }

* Seismic moment * – symbol M_{0} – is a measure of the work accomplished by the faulting of an earthquake.^{ [37] } Its magnitude is that of the forces that form the earthquake's equivalent double couple. (More precisely, it is the scalar magnitude of the second-order moment tensor that describes the force components of the double-couple^{ [38] }.) Seismic moment is measured in units of Newton meters (N·m) or Joules, or (in the older CGS system) dyne-centimeters (dyn-cm).^{ [39] }

The first calculation of an earthquake's seismic moment from its seismic waves was by Keiiti Aki for the 1964 Niigata earthquake.^{ [40] } He did this two ways. First, he used data from distant stations of the WWSSN to analyze long-period (200 second) seismic waves (wavelength of about 1,000 kilometers) to determine the magnitude of the earthquake's equivalent double couple.^{ [41] } Second, he drew upon the work of Burridge and Knopoff on dislocation to determine the amount of slip, the energy released, and the stress drop (essentially how much of the potential energy was released).^{ [42] } In particular, he derived a now famous equation that relates an earthquake's seismic moment to its physical parameters:

*M*_{0}=*μūS*

with μ being the rigidity (or resistance) of moving a fault with a surface areas of S over an average dislocation (distance) of ū. (Modern formulations replace ūS with the equivalent D̄A, known as the "geometric moment" or "potency".^{ [43] }.) By this equation the *moment* determined from the double couple of the seismic waves can be related to the moment calculated from knowledge of the surface area of fault slippage and the amount of slip. In the case of the Niigata earthquake the dislocation estimated from the seismic moment reasonably approximated the observed dislocation.^{ [44] }

Seismic moment is a measure of the work (more precisely, the torque) that results in inelastic (permanent) displacement or distortion of the earth's crust.^{ [45] } It is related to the total energy released by an earthquake. However, the power or potential destructiveness of an earthquake depends (among other factors) on how much of the total energy is converted into seismic waves.^{ [46] } This is typically 10% or less of the total energy, the rest being expended in fracturing rock or overcoming friction (generating heat).^{ [47] }

Nonetheless, seismic moment is regarded as the fundamental measure of earthquake size,^{ [48] } representing more directly than other parameters the physical size of an earthquake.^{ [49] } As early as 1975 it was considered "one of the most reliably determined instrumental earthquake source parameters".^{ [50] }

Most earthquake magnitude scales suffered from the fact that they only provided a comparison of the amplitude of waves produced at a standard distance and frequency band; it was difficult to relate these magnitudes to a physical property of the earthquake. Gutenberg and Richter suggested that radiated energy E_{s} could be estimated as

(in Joules). Unfortunately, the duration of many very large earthquakes was longer than 20 seconds, the period of the surface waves used in the measurement of M_{s} . This meant that giant earthquakes such as the 1960 Chilean earthquake (M 9.5) were only assigned an M_{s} 8.2. Caltech seismologist Hiroo Kanamori ^{ [51] } recognized this deficiency and took the simple but important step of defining a magnitude based on estimates of radiated energy, M_{w} , where the "w" stood for work (energy):

Kanamori recognized that measurement of radiated energy is technically difficult since it involves the integration of wave energy over the entire frequency band. To simplify this calculation, he noted that the lowest frequency parts of the spectrum can often be used to estimate the rest of the spectrum. The lowest frequency asymptote of a seismic spectrum is characterized by the seismic moment, M_{0} . Using an approximate relation between radiated energy and seismic moment (which assumes stress drop is complete and ignores fracture energy),

(where **E** is in Joules and M_{0} is in Nm), Kanamori approximated M_{w} by

The formula above made it much easier to estimate the energy-based magnitude M_{w} , but it changed the fundamental nature of the scale into a moment magnitude scale. Caltech seismologist Thomas C. Hanks noted that Kanamori's M_{w} scale was very similar to a relationship between M_{L} and M_{0} that was reported by Thatcher & Hanks (1973)

Hanks & Kanamori (1979) combined their work to define a new magnitude scale based on estimates of seismic moment

where is defined in newton meters (N·m).

Moment magnitude is now the most common measure of earthquake size for medium to large earthquake magnitudes,^{ [52] }^{[ scientific citation needed ]} but in practice, seismic moment, the seismological parameter it is based on, is not measured routinely 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,^{[ citation needed ]} which includes the great majority of quakes.

Current practice in official^{[ who? ]} earthquake reports is to adopt moment magnitude as the preferred magnitude, i.e., M_{w} is the official magnitude reported whenever it can be computed. Because seismic moment (M_{0} , the quantity needed to compute M_{w} ) is not measured if the earthquake is too small, the reported magnitude for earthquakes smaller than M 4 is often Richter's M_{L} .

Popular press reports most often deal with significant earthquakes larger than M ~ 4. For these events, the official^{[ who? ]} magnitude is the moment magnitude M_{w} , not Richter's local magnitude M_{L} .

The symbol for the moment magnitude scale is M_{w} , with the subscript "w" meaning mechanical work accomplished. The moment magnitude M_{w} is a dimensionless value defined by Hiroo Kanamori ^{ [53] } as

where M_{0} is the seismic moment in dyne⋅cm (10^{−7} N⋅m).^{ [54] } The constant values in the equation are chosen to achieve consistency with the magnitude values produced by earlier scales, such as the local magnitude and the surface wave magnitude. Thus, a magnitude zero microearthquake has a seismic moment of approximately 1.2×10^{9} N⋅m, while the Great Chilean earthquake of 1960, with an estimated moment magnitude of 9.4–9.6, had a seismic moment between 1.4×10^{23} N⋅m and 2.8×10^{23} N⋅m.

Seismic moment is not a direct measure of energy changes during an earthquake. The relations between seismic moment and the energies involved in an earthquake depend on parameters that have large uncertainties and that may vary between earthquakes. Potential energy is stored in the crust in the form of elastic energy due to built-up stress and gravitational energy.^{ [55] } During an earthquake, a portion of this stored energy is transformed into

- energy dissipated in frictional weakening and inelastic deformation in rocks by processes such as the creation of cracks
- heat
- radiated seismic energy

The potential energy drop caused by an earthquake is related approximately to its seismic moment by

where is the average of the *absolute* shear stresses on the fault before and after the earthquake (e.g., equation 3 of Venkataraman & Kanamori 2004) and is the average of the shear moduli of the rocks that constitute the fault. Currently, there is no technology to measure absolute stresses at all depths of interest, nor method to estimate it accurately, and is thus poorly known. It could vary highly from one earthquake to another. Two earthquakes with identical but different would have released different .

The radiated energy caused by an earthquake is approximately related to seismic moment by

where is radiated efficiency and is the static stress drop, i.e., the difference between shear stresses on the fault before and after the earthquake (e.g., from equation 1 of Venkataraman & Kanamori 2004). These two quantities are far from being constants. For instance, depends on rupture speed; it is close to 1 for regular earthquakes but much smaller for slower earthquakes such as tsunami earthquakes and slow earthquakes. Two earthquakes with identical but different or would have radiated different .

Because and are fundamentally independent properties of an earthquake source, and since can now be computed more directly and robustly than in the 1970s, introducing a separate magnitude associated to radiated energy was warranted. Choy and Boatwright defined in 1995 the *energy magnitude*^{ [56] }

where is in J (N·m).

Assuming the values of σ̄/μ are the same for all earthquakes, one can consider M_{w} as a measure of the potential energy change Δ*W* caused by earthquakes. Similarly, if one assumes is the same for all earthquakes, one can consider M_{w} as a measure of the energy *E*_{s} radiated by earthquakes.

Under these assumptions, the following formula, obtained by solving for M_{0} the equation defining M_{w} , allows one to assess the ratio of energy release (potential or radiated) between two earthquakes of different moment magnitudes, and :

As with the Richter scale, an increase of one step on the logarithmic scale of moment magnitude 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.

Various ways of determining moment magnitude have been developed, and several subtypes of the M_{w} scale can be used to indicate the basis used.^{ [57] }

**Mwb**– Based on*moment tensor inversion*of long-period (~10 – 100 s) body-waves.**Mwr**– From a*moment tensor inversion*of complete waveforms at regional distances (~ 1,000 miles). Sometimes called RMT.**Mwc**– Derived from a*centroid moment tensor inversion*of intermediate- and long-period body- and surface-waves.**Mww**– Derived from a*centroid moment tensor inversion*of the W-phase.**Mwp**(**Mi**) – Developed by Seiji Tsuboi^{ [58] }for quick estimation of the tsunami potential of large near-coastal earthquakes from measurements of the P-waves, and later extended to teleseismic earthquakes in general.^{ [59] }**Mwpd**– A duration-amplitude procedure which takes into account the duration of the rupture, providing a fuller picture of the energy released by longer lasting ("slow") ruptures than seen with M_{w}.^{ [60] }

- ↑ These are normally not bolded. In the technical literature a single bolded "
**M**" – with or without italicization – is used for several related concepts.^{[ example needed ]} - ↑ Bormann, Wendt & Di Giacomo 2013 , pp. 14, 177.
- ↑ Bormann, Wendt & Di Giacomo 2013 , p. 86.
- ↑ Bormann, Wendt & Di Giacomo 2013 , p. 18.
- ↑ The "USGS Earthquake Magnitude Policy" for reporting earthquake magnitudes to the public as formulated by the
*USGS Earthquake Magnitude Working Group*was implemented January 18, 2002, and posted at https://earthquake.usgs.gov/aboutus/docs/020204mag_policy.php. That page was removed following a web redesign; a copy is archived at the Internet Archive. - ↑ Miyake 2017 , p. 112.
- ↑ Suzuki 2001 , p. 121. See also Figure 2-22 in Richter 1958 (copy in Bormann, Wendt & Di Giacomo 2013 , p. 60), which replicates Wadati's curves.
- ↑ Gutenberg & Richter 1956a.
- ↑ Richter 1935.
- ↑ See Bormann & Saul 2009 for an overview.
- ↑ Gutenberg 1945a.
- ↑ Gutenberg 1945b, Gutenberg & Richter 1956b.
- ↑ See Seismic magnitude scales.
- ↑ Kanamori 1977 , p. 2981.
- ↑ ISC-EHB Event 879136 [ IRIS ]; ISC-EHB Event 869809 [ IRIS ].
- ↑ Miyake 2017 , pp. 112-113; Stauder 1962 , p. 39.
- ↑ Miyake 2017 , p. 115.
- ↑ Ben-Menahem 1995 , p. 1210; Maruyama 1963 , p. 484.
- ↑ Shearer 2009 , p. 245.
- ↑ Ben-Menahem 1995 , p. 1210.
- ↑ Miyake 2017 , p. 115.
- ↑ Miyake 2017 , p. 115. See Byerly 1960 for a contemporary account of why many seismologists favored a single couple model.
- ↑ Miyake 2017 , pp. 116, 117.
- ↑ Pujol 2003b , p. 164.
- ↑ Pujol 2003b , p. 165; Miyake 2017 , pp. 117–118.
- ↑ Aki 1966b , p. 84; Pujol 2003b , p. 167.
- ↑ Julian, Miller & Foulger 1998 , §2.2.1.
- ↑ Miyake 2017 , p. 114, 117; Maruyama 1963 , p. 483.
- ↑ Miyake 2017 , p. 112.
- ↑ Miyake 2017 , p. 117.
- ↑ Steketee 1958b , pp. 1168-1169.
- ↑ Stauder 1962 , p. 42; Aki & Richards 2002 , p. 48.
- ↑ Honda 1962 , pp. 32, 65, and see bibliography; Ben-Menahem 1995 , p. 1212; Udías 1991 , p. 90; Maruyama 1963 , p. 467.
- ↑ Miyake 2017 , p. 467; Steketee 1958a , 1958b.
- ↑ Udías 1991 provides a partial overview.
- ↑ Pujol 2003b , pp. 165, 167; Miyake 2017 , p. 118.
- ↑ Bormann, Wendt & Di Giacomo 2013 , p. 14.
- ↑ Aki 1966b , p. 73; Kassaras & Kapetanidis 2018 , p. 410.
- ↑ Beroza & Kanamori 2015 , p. 5.
- ↑ Dziewonski, Chou & Woodhouse 1981 , p. 2826; Aki 1966b.
- ↑ Aki 1966a , pp. 24, 36.
- ↑ Aki 1966a , p. 24.
- ↑ Bormann, Wendt & Di Giacomo 2013 , p. 12, equation 3.1.
- ↑ Aki 1966b , p. 84.
- ↑ Bormann, Wendt & Di Giacomo 2013 , p. 14; Bormann & Di Giacomo 2011 , p. 412.
- ↑ Bormann, Wendt & Di Giacomo 2013 , pp. 39–40.
- ↑ Bormann, Wendt & Di Giacomo 2013 , p. 7.
- ↑ Deichmann 2006 , p. 1268.
- ↑ Abe 1982 , p. 322.
- ↑ Kanamori & Anderson 1975 , p. 1076.
- ↑ Kanamori 1977.
- ↑ Boyle 2008.
- ↑ Kanamori 1977.
- ↑ Hanks & Kanamori 1979.
- ↑ Kostrov 1974; Dahlen 1977.
- ↑ Choy & Boatwright 1995
- ↑ USGS Technical Terms used on Event Pages.
- ↑ Tsuboi et al. 1995.
- ↑ Bormann, Wendt & Di Giacomo 2013 , §3.2.8.2, p. 135.
- ↑ Bormann, Wendt & Di Giacomo 2013 , §3.2.8.3, pp. 137–128.

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An **earthquake** is the shaking of the surface of the Earth resulting from a sudden release of energy in the Earth's lithosphere that creates seismic waves. Earthquakes can range in size from those that are so weak that they cannot be felt to those violent enough to propel objects into the air, and wreak destruction across entire cities. The seismicity, or **seismic activity**, of an area is the frequency, type, and size of earthquakes experienced over a period of time. The word *tremor* is also used for non-earthquake seismic rumbling.

The **Modified Mercalli intensity scale**, descended from Giuseppe Mercalli's **Mercalli intensity scale** of 1902, is a seismic intensity scale used for measuring the *intensity of shaking* produced by an earthquake. It measures the *effects* of an earthquake *at a given location*, distinguished from the earthquake's inherent *force* or *strength* as measured by seismic magnitude scales. While shaking is driven by the seismic energy released by an earthquake, earthquakes differ in how much of their energy is radiated as seismic waves. Deeper earthquakes also have less interaction with the surface, and their energy is spread out across a larger area. Shaking intensity is localized, generally diminishing with distance from the earthquake's epicenter, but can be amplified in sedimentary basins and certain kinds of unconsolidated soils.

**Seismology** is the scientific study of earthquakes and the propagation of elastic waves through the Earth or through other planet-like bodies. The field also includes studies of earthquake environmental effects such as tsunamis as well as diverse seismic sources such as volcanic, tectonic, oceanic, atmospheric, and artificial processes such as explosions. A related field that uses geology to infer information regarding past earthquakes is paleoseismology. A recording of earth motion as a function of time is called a seismogram. A seismologist is a scientist who does research in seismology.

**Beno Gutenberg** was a German-American seismologist who made several important contributions to the science. He was a colleague and mentor of Charles Francis Richter at the California Institute of Technology and Richter's collaborator in developing the Richter magnitude scale for measuring an earthquake's magnitude.

**Seismic moment** is a quantity used by seismologists to measure the size of an earthquake. The scalar seismic moment is defined by the equation , where

**Hiroo Kanamori** is a Japanese seismologist who has made fundamental contributions to understanding the physics of earthquakes and the tectonic processes that cause them.

**Peak ground acceleration** (**PGA**) is equal to the maximum ground acceleration that occurred during earthquake shaking at a location. PGA is equal to the amplitude of the largest absolute acceleration recorded on an accelerogram at a site during a particular earthquake. Earthquake shaking generally occurs in all three directions. Therefore, PGA is often split into the horizontal and vertical components. Horizontal PGAs are generally larger than those in the vertical direction but this is not always true, especially close to large earthquakes. PGA is an important parameter for earthquake engineering, The **design basis earthquake ground motion** (**DBEGM**) is often defined in terms of PGA.

**Seismicity** is a measure encompassing earthquake occurrences, mechanisms, and magnitude at a given geographical location. As such, it summarizes a region's seismic activity. The term was coined by Beno Gutenberg and Charles Francis Richter in 1941. Seismicity is studied by geophysicists.

**Seismic magnitude scales** are used to describe the overall strength or "size" of an earthquake. These are distinguished from seismic intensity scales that categorize the intensity or severity of ground shaking (quaking) caused by an earthquake at a given location. Magnitudes are usually determined from measurements of an earthquake's seismic waves as recorded on a seismogram. Magnitude scales vary on what aspect of the seismic waves are measured and how they are measured. Different magnitude scales are necessary because of differences in earthquakes, the information available, and the purposes for which the magnitudes are used.

The **2007 Kuril Islands earthquake** occurred east of the Kuril Islands on 13 January at 1:23 p.m. (JST). The shock had a moment magnitude of 8.1 and a maximum Mercalli intensity of VI (*Strong*). A non-destructive tsunami was generated, with maximum wave amplitudes of 0.32 meters. The earthquake is considered a doublet of the 8.3 magnitude 2006 Kuril Islands earthquake which occurred the previous November approximately 95 km to the southeast.

The **International Seismological Centre** (ISC) is a non-governmental, nonprofit organisation charged with the final collection, definitive analysis and publication of global seismicity. The ISC was formed in 1964 as an international organisation independent of national governments that would carry on the work of the International Seismological Summary in collecting and analyzing seismic data from around the world, and particularly to handle increased flow of data from the World-Wide Standard Seismograph Network (WWSSN), also established that year. The ISC considers its prime task to be the collection and re-analysis of all available earthquake seismic date in order to produce definitive data on earthquakes. The ISC's catalog is considered "the most complete and authoritative final depositary of global earthquake parameter data."

The **surface wave magnitude** scale is one of the magnitude scales used in seismology to describe the size of an earthquake. It is based on measurements in Rayleigh surface waves that travel primarily along the uppermost layers of the Earth. It is currently used in People's Republic of China as a national standard(**GB 17740-1999**) for categorising earthquakes.

A **supershear earthquake** is an earthquake in which the propagation of the rupture along the fault surface occurs at speeds in excess of the seismic shear wave (S-wave) velocity. This causes an effect analogous to a sonic boom.

The **Richter scale** – also **Richter magnitude****Richter magnitude scale**, or **Richter's magnitude scale** – for measuring the strength of earthquakes refers to the original "magnitude scale" developed by Charles F. Richter and presented in his landmark 1935 paper. This was later revised and renamed the **local magnitude scale**, denoted as ML or M_{L} . Because of various shortcomings of the M_{L} scale most seismological authorities now use other scales, such as the moment magnitude scale (M_{w} ), to report earthquake magnitudes, but much of the news media still refers to these as "Richter" magnitudes. All magnitude scales retain the logarithmic character of the original and are scaled to have roughly comparable numeric values.

A **tsunami earthquake** triggers a tsunami of a magnitude that is very much larger than the magnitude of the earthquake as measured by shorter-period seismic waves. The term was introduced by Hiroo Kanamori in 1972. Such events are a result of relatively slow rupture velocities. They are particularly dangerous as a large tsunami may arrive at a coastline with little or no warning. A tsunami is a sea wave of local or distant origin that results from large-scale seafloor displacements associated with large earthquakes, major submarine slides, or exploding volcanic islands.

The **1942 Guatemala earthquake** occurred at 17:37 local time on August 6 and had ratings of 7.7 on the moment magnitude scale and 7.9 on the surface wave magnitude scale. The epicenter was located off the southern coast of Guatemala, and it was one of the strongest earthquakes ever recorded there.

An **earthquake rupture** is the extent of slip that occurs during an earthquake in the Earth's crust. Earthquakes occur for many reasons that include: landslides, movement of magma in a volcano, the formation of a new fault, or, most commonly of all, a slip on an existing fault.

**Energy class** – also called **energy class K** or **K-class **, and denoted by **K** – is a measure of the force or magnitude of local and regional earthquakes used in countries of the former Soviet Union, and Cuba and Mongolia. K is nominally the logarithm of seismic energy radiated by an earthquake, as expressed in the formula K = log E_{S}. Values of K in the range of 12 to 15 correspond approximately to the range of 4.5 to 6 in other magnitude scales; a magnitude M_{w} 6.0 quake will register between 13 and 14.5 on various K-class scales. The energy class system was developed by seismologists of the Soviet *Tadzhikskaya Complex* [Interdisciplinary] *Seismological Expedition* established in the remote Garm (Tajikistan) region of Central Asia in 1954 after several devastating earthquakes in that area.

**Seismic intensity scales** categorize the intensity or severity of ground shaking (quaking) at a given location, such as resulting from an earthquake. They are distinguished from seismic magnitude scales, which measure the magnitude or overall strength of an earthquake, which may, or perhaps not, cause perceptible shaking.

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