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Earthquakes
Types Mainshock Foreshock Aftershock Blind thrust Doublet Interplate Intraplate Megathrust Remotely triggered Slow Submarine Supershear Tsunami Earthquake swarm
Causes Fault movement Volcanism Induced seismicity
Characteristics Epicenter Epicentral distance Hypocenter Shadow zone Seismic waves P wave S wave
Measurement Seismometer Seismic magnitude scales Seismic intensity scales
Prediction Coordinating Committee for Earthquake Prediction Forecasting
Other topics Shear wave splitting Adams–Williamson equation Flinn–Engdahl regions Earthquake engineering Seismite Seismology
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The concept of Earthquake Duration Magnitude – originally proposed by E. Bisztricsany^[1] in 1958 using surface waves only - is based on the realization that on a recorded earthquake seismogram, the total length of the seismic wavetrain – sometimes referred to as the CODA – reflects its size. Thus larger earthquakes give longer seismograms [as well as stronger seismic waves] than small ones. The seismic wave interval measured on the time axis of an earthquake record - starting with the first seismic wave onset until the wavetrain amplitude diminishes to at least 10% of its maximum recorded value - is referred to as "earthquake duration". It is this concept that Bisztricsany first used to develop his Earthquake Duration Magnitude Scale employing surface wave durations.

In 1965, Solovev^[2] proposed the use of total duration instead of the duration of surface waves. In 1972, Lee et al.^[3] used coda duration for the first time to estimate Richter magnitude of local Californian earthquakes. Based on their study, they suggested that it is appropriate to estimate the magnitude of local earthquakes using signal duration. More recently, the development in instrumentation led to the use of signal duration to estimate the coda magnitude (M_d ) for earthquakes recorded on short-period vertical seismographs. Numerous studies determined the relation between coda duration and magnitude for different regions of the World. According to a recent study by Mandal et al. (2004),^[4] previous studies showed that duration magnitude estimation is quite stable for local earthquakes ranging from magnitude M_d  0.0 to 5.0.

In two most recent investigations using statistically stable samples for Italian earthquakes (approximately 100,000 events over the period 1981–2002 in the Richter local [M_L ] magnitude range of 3.5–5.8)^[5] and for Indian earthquakes exemplified by an aftershock sequence of 121 events with M_s (surface wave magnitude) > 4.0 in 2001 in the Bhuj area of northwestern India,^[4] the latest empirically derived equations for M_d  determinations are published:

${\displaystyle M_{d}=2.49*log_{10}(T)-2.31+(Station\ correction\ factor)}$ (Castello et al., 2007)^[5]

${\displaystyle M_{d}=0.08*log_{10}(T)^{2}+1.7*log_{10}(T)-0.87}$ (Mandal et al., 2004)^[4]

Where M_d  is coda duration magnitude, and T is the coda duration in seconds.

Although conversions between empirically derived "sensitive" seismic parameters such as earthquake magnitude scales is mathematically cautioned as well as physically limited, some seismologists such as Brumbaugh^[6] have nevertheless attempted to produce a relationship linking M_L  to M_d  for a rather small sample of 17 events in Arizona:

${\displaystyle M_{L}=0.936*M_{d}-0.16\pm 0.22}$