Richter Scale

This was later revised and renamed the local magnitude scale, denoted as ML or M_L .

Because of various shortcomings of the original M_L  scale, most seismological authorities now use other similar scales such as the moment magnitude scale (M_w ) to report earthquake magnitudes, but much of the news media still erroneously 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 (typically in the middle of the scale). Due to the variance in earthquakes, it is essential to understand the Richter scale uses common logarithms simply to make the measurements manageable (i.e., a magnitude 3 quake factors 10³ while a magnitude 5 quake factors 10⁵ and has seismometer readings 100 times larger).

 

The Richter magnitude of an earthquake is determined from the logarithm of the amplitude of waves recorded by seismographs. Adjustments are included to compensate for the variation in the distance between the various seismographs and the epicenter of the earthquake. The original formula is:

$${\displaystyle M_{\mathrm {L} }=\log _{10}A-\log _{10}A_{\mathrm {0} }(\delta )=\log _{10}[A/A_{\mathrm {0} }(\delta )],\ }$$
 

where A is the maximum excursion of the Wood-Anderson seismograph, the empirical function A₀ depends only on the epicentral distance of the station, ${\displaystyle \delta }$ . In practice, readings from all observing stations are averaged after adjustment with station-specific corrections to obtain the M_L  value.

Because of the logarithmic basis of the scale, each whole number increase in magnitude represents a tenfold increase in measured amplitude. In terms of energy, each whole number increase corresponds to an increase of about 31.6 times the amount of energy released, and each increase of 0.2 corresponds to approximately a doubling of the energy released.

Events with magnitudes greater than 4.5 are strong enough to be recorded by a seismograph anywhere in the world, so long as its sensors are not located in the earthquake's shadow.

The following describes the typical effects of earthquakes of various magnitudes near the epicenter. The values are typical and may not be exact in a future event because intensity and ground effects depend not only on the magnitude but also on (1) the distance to the epicenter, (2) the depth of the earthquake's focus beneath the epicenter, (3) the location of the epicenter, and (4) geological conditions.

(Based on U.S. Geological Survey documents.)

The intensity and death toll depend on several factors (earthquake depth, epicenter location, and population density, to name a few) and can vary widely.

Millions of minor earthquakes occur every year worldwide, equating to hundreds every hour every day. On the other hand, earthquakes of magnitude ≥8.0 occur about once a year, on average. The largest recorded earthquake was the Great Chilean earthquake of May 22, 1960, which had a magnitude of 9.5 on the moment magnitude scale.

Seismologist Susan Hough has suggested that a magnitude 10 quake may represent a very approximate upper limit for what the Earth's tectonic zones are capable of, which would be the result of the largest known continuous belt of faults rupturing together (along the Pacific coast of the Americas). A research at the Tohoku University in Japan found that a magnitude 10 earthquake was theoretically possible if a combined 3,000 kilometres (1,900 mi) of faults from the Japan Trench to the Kuril–Kamchatka Trench ruptured together and moved by 60 metres (200 ft) (or if a similar large-scale rupture occurred elsewhere). Such an earthquake would cause ground motions for up to an hour, with tsunamis hitting shores while the ground is still shaking, and if this kind of earthquake occurred, it would probably be a 1-in-10,000-year event.

 

Prior to the development of the magnitude scale, the only measure of an earthquake's strength or "size" was a subjective assessment of the intensity of shaking observed near the epicenter of the earthquake, categorized by various seismic intensity scales such as the Rossi-Forel scale. ("Size" is used in the sense of the quantity of energy released, not the size of the area affected by shaking, though higher-energy earthquakes do tend to affect a wider area, depending on the local geology.) In 1883, John Milne surmised that the shaking of large earthquakes might generate waves detectable around the globe, and in 1899 E. Von Rehbur Paschvitz observed in Germany seismic waves attributable to an earthquake in Tokyo. In the 1920s, Harry O. Wood and John A. Anderson developed the Wood–Anderson seismograph, one of the first practical instruments for recording seismic waves. Wood then built, under the auspices of the California Institute of Technology and the Carnegie Institute, a network of seismographs stretching across Southern California. He also recruited the young and unknown Charles Richter to measure the seismograms and locate the earthquakes generating the seismic waves.

In 1931, Kiyoo Wadati showed how he had measured, for several strong earthquakes in Japan, the amplitude of the shaking observed at various distances from the epicenter. He then plotted the logarithm of the amplitude against the distance and found a series of curves that showed a rough correlation with the estimated magnitudes of the earthquakes. Richter resolved some difficulties with this method and then, using data collected by his colleague Beno Gutenberg, he produced similar curves, confirming that they could be used to compare the relative magnitudes of different earthquakes.

Additional developments were required to produce a practical method of assigning an absolute measure of magnitude . First, to span the wide range of possible values, Richter adopted Gutenberg's suggestion of a logarithmic scale, where each step represents a tenfold increase of magnitude, similar to the magnitude scale used by astronomers for star brightness. Second, he wanted a magnitude of zero to be around the limit of human perceptibility. Third, he specified the Wood–Anderson seismograph as the standard instrument for producing seismograms. Magnitude was then defined as "the logarithm of the maximum trace amplitude, expressed in microns", measured at a distance of 100 km (62 mi). The scale was calibrated by defining a magnitude 0 shock as one that produces (at a distance of 100 km (62 mi)) a maximum amplitude of 1 micron (1 µm, or 0.001 millimeters) on a seismogram recorded by a Wood-Anderson torsion seismometer. Finally, Richter calculated a table of distance corrections, in that for distances less than 200 kilometers the attenuation is strongly affected by the structure and properties of the regional geology.

When Richter presented the resulting scale in 1935, he called it (at the suggestion of Harry Wood) simply a "magnitude" scale. "Richter magnitude" appears to have originated when Perry Byerly told the press that the scale was Richter's and "should be referred to as such." In 1956, Gutenberg and Richter, while still referring to "magnitude scale", labelled it "local magnitude", with the symbol M_L , to distinguish it from two other scales they had developed, the surface wave magnitude (M_S) and body wave magnitude (M_B) scales.

 

The Richter scale was defined in 1935 for particular circumstances and instruments; the particular circumstances refer to it being defined for Southern California and "implicitly incorporates the attenuative properties of Southern California crust and mantle." The particular instrument used would become saturated by strong earthquakes and unable to record high values. The scale was replaced in the 1970s by the moment magnitude scale (MMS, symbol M_w ); for earthquakes adequately measured by the Richter scale, numerical values are approximately the same. Although values measured for earthquakes now are M_w , they are frequently reported by the press as Richter values, even for earthquakes of magnitude over 8, when the Richter scale becomes meaningless.

The Richter and MMS scales measure the energy released by an earthquake; another scale, the Mercalli intensity scale, classifies earthquakes by their effects, from detectable by instruments but not noticeable, to catastrophic. The energy and effects are not necessarily strongly correlated; a shallow earthquake in a populated area with soil of certain types can be far more intense in impact than a much more energetic deep earthquake in an isolated area.

Several scales have been historically described as the "Richter scale",^{[citation needed]}, especially the local magnitude M_L  and the surface wave M_s  scale. In addition, the body wave magnitude, mb , and the moment magnitude, M_w , abbreviated MMS, have been widely used for decades. A couple of new techniques to measure magnitude are in the development stage by seismologists.

All magnitude scales have been designed to give numerically similar results. This goal has been achieved well for M_L , M_s , and M_w . The mb  scale gives somewhat different values than the other scales. The reason for so many different ways to measure the same thing is that at different distances, for different hypocentral depths, and for different earthquake sizes, the amplitudes of different types of elastic waves must be measured.

M_L  is the scale used for the majority of earthquakes reported (tens of thousands) by local and regional seismological observatories. For large earthquakes worldwide, the moment magnitude scale (MMS) is most common, although M_s  is also reported frequently.

The seismic moment, M₀ , is proportional to the area of the rupture times the average slip that took place in the earthquake, thus it measures the physical size of the event. M_w  is derived from it empirically as a quantity without units, just a number designed to conform to the M_s  scale. A spectral analysis is required to obtain M₀ . In contrast, the other magnitudes are derived from a simple measurement of the amplitude of a precisely defined wave.

All scales, except M_w , saturate for large earthquakes, meaning they are based on the amplitudes of waves that have a wavelength shorter than the rupture length of the earthquakes. These short waves (high-frequency waves) are too short a yardstick to measure the extent of the event. The resulting effective upper limit of measurement for M_L  is about 7 and about 8.5 for M_s .

New techniques to avoid the saturation problem and to measure magnitudes rapidly for very large earthquakes are being developed. One of these is based on the long-period P-wave; The other is based on a recently discovered channel wave.

The energy release of an earthquake, which closely correlates to its destructive power, scales with the 3⁄2 power of the shaking amplitude (see Moment magnitude scale for an explanation). Thus, a difference in magnitude of 1.0 is equivalent to a factor of 31.6 (${\displaystyle =({10^{1.0}})^{(3/2)}}$ ) in the energy released; a difference in magnitude of 2.0 is equivalent to a factor of 1000 (${\displaystyle =({10^{2.0}})^{(3/2)}}$ ) in the energy released. The elastic energy radiated is best derived from an integration of the radiated spectrum, but an estimate can be based on mb  because most energy is carried by the high-frequency waves.

These formulae for Richter magnitude ${\displaystyle \ M_{\mathsf {L}}\ }$  are alternatives to using Richter correlation tables based on Richter standard seismic event ${\displaystyle {\big (}\ M_{\mathsf {L}}=0\ ,}$  ${\displaystyle \ A=0.001\ {\mathsf {mm}}\ ,}$  ${\displaystyle \ D=100\ {\mathsf {km}}\ {\big )}~.}$  In the formulas below, ${\displaystyle \ \Delta \ }$  is the epicentral distance in kilometers, and ${\displaystyle \ \Delta ^{\circ }\ }$  is the same distance represented as sea level great circle degrees.

The Lillie empirical formula is:

${\displaystyle \ M_{\mathsf {L}}=\log _{10}A-2.48+2.76\ \log _{10}\Delta \ }$ 
where ${\displaystyle \ A\ }$  is the amplitude (maximum ground displacement) of the P-wave, in micrometers (µm), measured at 0.8 Hz.

Lahr's empirical formula proposal is:

${\displaystyle \ M_{\mathsf {L}}=\log _{10}A+1.6\ \log _{10}D-0.15\ ,}$ 
where
${\displaystyle \ A\ }$  is seismograph signal amplitude in mm and
${\displaystyle \ D\ }$  is in km, for distances under 200 km .

and

${\displaystyle \ M_{\mathsf {L}}=\log _{10}A+3.0\ \log _{10}D-3.38\ ;}$ 
where ${\displaystyle \ D\ }$  is in km, for distances between 200 km and 600 km .

The Bisztricsany empirical formula (1958) for epicentre distances between 4° and 160° is:

${\displaystyle \ M_{\mathsf {L}}=2.92+2.25\ \log _{10}\left(\tau \right)-0.001\ \Delta ^{\circ }\ ,}$ 
where
${\displaystyle \ \tau \ }$  is the duration of the surface wave in seconds, and
${\displaystyle \ \Delta ^{\circ }\ }$  is in degrees.
${\displaystyle \ M_{\mathsf {L}}\ }$  is mainly between 5 and 8.

The Tsumura empirical formula is:

${\displaystyle \ M_{\mathsf {L}}=-2.53+2.85\log _{10}\left(F-P\right)+0.0014\ \Delta ^{\circ }\ ,}$ 
where
${\displaystyle \ F-P\ }$  is the total duration of oscillation in seconds.
${\displaystyle \ M_{\mathsf {L}}\ }$  mainly takes on values between 3 and 5.

The Tsuboi (University of Tokyo) empirical formula is:

${\displaystyle \ M_{\mathsf {L}}=\log _{10}A+1.73\ \log _{10}\Delta -0.83\ ,}$ 
where ${\displaystyle \ A\ }$  is the amplitude in µm.