Earthquake Magnitude & Intensity

Earthquake magnitude is a quantitative, mathematical calculation to measure the energy released at the source of an earthquake. On the other hand, earthquake intensity is the qualitative measurement of the strength of shaking produced by an earthquake.

Content:
Earthquake (Seismic) Magnitude Scales
Richter Scale (ML)
Body Wave Magnitude Scale (mb)
Moment Magnitude Scale (M­W)
Duration Magnitude Scale (Md OR Mt)
Earthquake (Seismic) Intensity Scales
Modified Mercalli Intensity Scale
Earthquake Magnitude/Intensity Comparison
Which is the “correct” magnitude and location?
What is a minor or light earthquake?

Earthquake (Seismic) Magnitude Scales

Typical seismogram. The compressive P-waves (following the red lines) – essentially sound passing through rock – are the fastest seismic waves, and arrive first, typically in about 10 seconds for an earthquake around 50 km away. The sideways-shaking S-waves (following the green lines) arrive some seconds later, traveling a little over half the speed of the P-waves; the delay is a direct indication of the distance to the quake. S-waves may take an hour to reach a point 1000s of km away. Both of these are body-waves, that pass directly through the earth’s crust. Following the S-waves are various kinds of surface-waves – Love waves and Rayleigh waves – that travel only at the earth’s surface. Surface waves are smaller for deep earthquakes, which have less interaction with the surface. For shallow earthquakes – less than roughly 60 km deep – the surface waves are stronger, and may last several minutes; these carry most of the energy of the quake and cause the most severe damage. (Credit: 1906 San Francisco earthquake’s seismogram recorded in Gottingen, Germany, USGS)

Magnitude scales describe, numerically, the size of the earthquake using mathematical equations and characteristics from the seismic waves recorded on seismographs.

Determination of an earthquake’s magnitude generally involves identifying specific types of seismic waves on a seismogram and then measuring one or more characteristics of a wave, such as its timing, orientation, amplitude, frequency, or duration. Additional adjustments are usually made for distance, kind of crust, and the characteristics of the seismograph that recorded the seismogram.

The various magnitude scales represent different ways of deriving magnitude from information as is available. All magnitude scales retain the logarithmic scale as devised by Charles Richter, and are adjusted so the mid-range approximately correlates with the original “Richter” scale.

There are several magnitude scales that are used across the world. Comprehensive and technical information can be found on the USGS’ website. In the Eastern Caribbean, there are some that are frequently used.

Richter Magnitude Scale (ml, ML, ML)

The Richter Magnitude, or local magnitude scale, was the first scale for measuring earthquakes. It was developed in 1935 by Charles F. Richter.

Richter established two features now common to all magnitude scales.

How is the ML Scale Calculated?

The original Richter scale was developed to relate the amplitude of a seismic wave and the distance of the S and P waves on the seismogram. It is based on the maximum amplitude of a seismogram recorded on a Wood-Anderson torsion seismograph. Although these instruments are no longer widely in use, ML values are calculated using modern instrumentation with appropriate adjustments.

The most important, and widely known fact about this scale is that it is logarithmic. Each unit represents a ten-fold increase in the amplitude of the seismic waves and each unit of magnitude represents a nearly 32-fold increase in the energy (strength) of an earthquake.

Limitations

All “Local” (ML) magnitudes are based on the maximum amplitude of the ground shaking, without distinguishing the different seismic waves. They underestimate the strength of:

  • distant earthquakes (over ~600 km) because of attenuation of the S-waves,
  • deep earthquakes because the surface waves are smaller, and
  • strong earthquakes (over M ~7) because they do not take into account the duration of shaking.

Because of these shortcomings, other magnitude scales were developed.

In Trinidad and Tobago, this scale is rarely used. In the few occurrences it is utilized by international seismological organizations, such as the USGS, it is because no other types of magnitude using available scales were able to be calculated.

This type of scale is used for earthquakes of magnitudes 2.0 to 6.5, at distances of 0 to 600 kilometers away from seismometers.

Body Wave Magnitude Scale (mb)

Body-waves consist of P-waves that are the first to arrive (see above seismogram), or S-waves, or reflections of either. Body-waves travel through rock directly. (Havskov & Ottemöller 2009)

While there are several iterations of body magnitude scales, most times in the Trinidad and Tobago region, if this scale is used, the mb iteration is reported.

How is the mb Scale Calculated?

The mb or mb scale uses only P-waves measured in the first few seconds on a specific model of a short-period seismograph. The short period improves the detection of smaller events.

The measurement of mb has changed several times. The modern practice by the USGS is to measure the short-period mb scale at less than three seconds, while the broadband mBBB scale is measured at periods of up to 30 seconds.

Limitations

The mb scale is typically used for earthquakes of magnitude 4.0 to 6.5, at distances of 15 to 100 degrees away from the seismometer.

It is reported for most M4.0-4.5 to 6.5 earthquakes that are observed teleseismically (recorded far distances from the earthquake source). Typically, with a light (M4.0-4.9) or moderate (M5.0-5.9) earthquake occurs near Trinidad and Tobago, this type of magnitude is published by the USGS.

Mb tends to saturate at about M 6.5 or larger.

Moment Magnitude (MW or Mw)

The Moment Magnitude (MW or Mw) is a measure of an earthquake’s magnitude based on its seismic moment (the energy released). Its numerical value is similar to the magnitudes on the original Richter Scale.

How is the MW Scale Calculated?

The MW scale is based on an earthquake’s seismic moment. This is a measure of how much work an earthquake does in sliding one area of rock past another area of rock.

In the simplest case, the moment can be calculated knowing only the amount of slip, the area of the surface ruptured or slipped, and a factor for the resistance or friction encountered.

These factors can be estimated for an existing fault to determine the magnitude of past earthquakes, or what might be anticipated for the future.

Our neighbouring seismological organization, FUNVISIS, typically publishes the MW magnitude as their earthquake solutions.

An earthquake’s seismic moment can be estimated in various ways, which are the bases of the MwbMwrMwcMwwMwpMi, and Mwpd scales, all subtypes of the generic Mw scale.

In the Trinidad and Tobago region, these values are typically calculated and published by international seismological centers such as the USGS or GFZ.

Generally, for larger events, the USGS (NEIC) publishes the MwbMwc and most commonly the Mww magnitudes. FUNVISIS publishes the Mwr for larger events.

The differences amongst these MW magnitude types are fairly complex geophysical and mathematical calculations but are generally seen as the most accurate in determining the magnitude of larger earthquakes, generally above M6.0.

Mww is generally calculated by USGS for all M5.0 or larger earthquakes worldwide, but generally robust for all M5.5 worldwide. It provides consistent results to M~4.5 within a regional network of high-quality broadband stations. It is the authoritative USGS magnitude if computed. The August 21st 2018 earthquake magnitude by the USGS was Mww 7.3, versus the UWI SRC’s magnitude of M6.9 (more on this below).

Mw and Mwr are usually calculated by FUNVISIS, with Mwr for larger events, within their area of responsibility. Generally, source complexity and dimensions at larger magnitudes (~M7.0 or greater) limit Mwr applicability.
Mw magnitude is usually calculated there is there a large number of high-quality broadband stations, where Mw values can be calculated for events as small as M4.0. In FUNVISIS’ case, it is calculated for all magnitudes of earthquakes.

Limitations

Since the seismic moment is required for the calculation of a moment magnitude, this type of magnitude scale is generally used for quakes with magnitudes larger than M4.0 by the USGS. FUNVISIS, on the other hand, calculates the moment magnitude for all events.

Duration Magnitude Scale (Md, md OR Mt )

The duration magnitude is the magnitude that is published by the University of the West Indies Seismic Research Centre (Page 6) for all seismic events within their area of responsibility for the Eastern Caribbean.

Across the world, the duration magnitude is denoted by Md or md. At the UWI SRC, it is denoted by Mt. This should not be confused with the Tsunami magnitude of Mt.

How is the Duration Magnitude Scale Calculated?

Md designates various scales that estimate magnitude from the duration or length of some part of the seismic wave-train. 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. This is referred to as “earthquake duration”.

Duration magnitude is especially useful for measuring local or regional earthquakes, both powerful earthquakes that might drive the seismometer off-scale (a problem with the analog instruments formerly used) and preventing measurement of the maximum wave amplitude, and weak earthquakes, whose maximum amplitude is not accurately measured.

Even for distant earthquakes, measuring the duration of the shaking (as well as the amplitude) provides a better measure of the earthquake’s total energy. 

Earthquake (Seismic) Intensity Scales

Intensity measures the strength of shaking produced by the earthquake at a certain location. It is determined by effects on people, human structures, and the natural environment. Intensity is typically represented by Roman numerals, to emphasize the point of it being an integer value historically. However, in the age of technology, most seismologists use Arabic numerals. (Musson et al., 2012)

The use of intensity scales is historically important because no instrumentation is necessary, and useful measurements of an earthquake can be made by an unequipped observer. This is how we can estimate a magnitude for historical earthquakes in the Caribbean, and beyond before seismometers were present.

The first scale to be used internationally was the ten-degree Rossi-Forel Scale of 1883. The scale of Sieberg became the foundation of all modern twelve-degree scales.

Across the modern world, there are three intensity scales that are predominantly used to characterize earthquake shaking and earthquake damage:

Modified Mercalli Intensity Scale

The Modified Mercalli intensity scale (MM or MMI), 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.

This scale is generally used by most countries and seismological agencies across the world, including Trinidad and Tobago.

Most versions of the MMI that are typically found on the internet are abridged versions or some arrangement and/or amalgamation of different published definitions of the MMI. A comprehensive (i.e. another amalgamation) MMI is presented below, taking into account the works of Stover & Coffman (1993), Wood & Neumann (1931) and edits from Musson.

Generally, the lower degrees of the Modified Mercalli Intensity scale generally deal with the manner in which the earthquake is felt by people. The higher numbers of the scale are based on observed structural damage and are assigned by structural engineers.

A comprehensive MMI taking into account the works of Stover & Coffman (1993), Wood & Neumann (1931) and edits from Musson. (Click for higher resolution image)

The UWI Seismic Research Centre also has an abridged version, which can be found on their website.

In Trinidad and Tobago, we generally experience events that cause shaking resulting in MMI values less than IV. The strong M6.9 earthquake on 21st August 2018, the average MMI value was IV, with the maximum values of VIII.

Peak ground acceleration (PGA) is the effective Peak Ground Acceleration during the earthquake. That is the maximum horizontal ground acceleration excluding high-frequency spikes. PGA of the M6.9 quake in stations across Port of Spain ranged from 0.16g to 0.27g. More information can be found on the preliminary report compiled by the UWI Seismic Research Center.

Earthquake Magnitude/Intensity Comparison

Hence, the above magnitudes may sometimes generate stronger or weaker shaking than expected. In turn, there may be higher or lower MMI values reported depending on the characteristics of the earthquake.

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.

Which is the “correct” magnitude and location?

Across the globe, different seismic monitoring agencies use different methods, or several methods, for processing earthquake parameters. Each method has its limitations and will likely produce different results within the ranges of the uncertainty of that data. This is generally accepted within the scientific community.

Additionally, to meet the public’s need for information, seismological agencies have now begun publishing and updating information as an earthquake occurs. The data is usually automatically processed with limited data by computers and published either directly online for the public (USGS, EMSC, etc.), or sent to stakeholders, then to the public (U.W.I. SRC).

Because limited amounts of data are used for these preliminary outputs, it is common to see minor changes in latitude, longitude, depths, and magnitude.

Furthermore, because of the difference in magnitude types, you will likely see even more variation amongst seismic reports from different organizations (UWI SRC, FUNVISIS, USGS, BSCF (France), etc.).

However, nearly all international seismic monitoring agencies do not receive seismic data from FUNVISIS or UWI SRC. This means that in most cases, with reporting stations mainly north of T&T, the epicenter of quakes nearly always have a northward bias when it comes to latitude and longitude of a quake. It is also important to note that there is no exact location of a quake, as these seismic events occur due to a slip across a fault.

No matter how dense the seismic network is, there is always uncertainty which by the density of stations is reduced but never eliminated. When a solution is produced, the longitude and latitude are generated. All processing algorithms also provide the small and big axis of the eclipse with that location in the center, hence the location of an earthquake is not one point on the earth, but an area defined by those axes.

In Trinidad, Tobago & The Eastern Caribbean

In the case of Trinidad and Tobago, automated posts from the U.W.I. Seismic Research Centre are posted onto their social media platforms within minutes of the event. These events are always then reviewed by a seismologist or seismic analyst at the SRC. In most instances, the reviewed solution is then posted to their website.

There is usually a 10 km margin of error in latitude and longitude, but often tens of km in depth, between preliminary results and reviewed results (which is standard for monitoring agencies), magnitude tends to change as more data come to hand, even with manual processing.

Ultimately, there is no correct method to calculate magnitude as each method has its strengths and weaknesses. It is important to note that for Trinidad, Tobago and the remainder of the English-speaking Eastern Caribbean, the University of the West Indies Seismic Research Center is the authoritative agency for seismic hazards in the English-speaking Eastern Caribbean. It operates the widest and densest network of seismic stations in the region. Thus, it is likely to consistently yield the most accurate results for the islands under its area of responsibility, which includes Trinidad & Tobago.

What does a minor or light earthquake mean?

The Richter magnitude scale is a measure of the strength of earthquakes, which can also be used to qualitatively describe the strength of a quake based on the quantitative number.

MagnitudeDescriptionModified Mercalli Intensity (MMI)Average Earthquake ImpactsAverage Estimated Global Frequency
1.0 - 1.9MicroIMicroearthquakes, not felt, or felt rarely. Recorded by seismographs.Continual/several million per year
2.0 - 2.9MinorI to IIFelt slightly by some people. No damage to buildings.Over one million per year
3.0 - 3.9III to IVFelt slightly by some people. No damage to buildings.Over 100,000 per year
4.0 - 4.9LightIV to VINoticeable shaking of indoor objects and rattling noises. Felt by most people in the affected area. Slightly felt outside. Generally causes zero to minimal damage. Moderate to significant damage very unlikely. Some objects may fall off shelves or be knocked over.10,000 to 15,000 per year
5.0 - 5.9ModerateVI to VIICan cause damage of varying severity to poorly constructed buildings. Zero to slight damage to all other buildings. Felt by everyone.1,000 to 1,500 per year
6.0 - 6.9StrongVIII to XDamage to a moderate number of well-built structures in populated areas. Earthquake-resistant structures survive with slight to moderate damage. Poorly designed structures receive moderate to severe damage. Felt in wider areas; up to hundreds of miles/kilometers from the epicenter. Strong to violent shaking in epicentral area.100 to 150 per year
7.0 - 7.9MajorX or greaterCauses damage to most buildings, some to partially or completely collapse or receive severe damage. Well-designed structures are likely to receive damage. Felt across great distances with major damage mostly limited to 250 km from epicenter.10 to 20 per year
8.0 - 8.9GreatMajor damage to buildings, structures likely to be destroyed. Will cause moderate to heavy damage to sturdy or earthquake-resistant buildings. Damaging in large areas. Felt in extremely large regions.One per year
9.0 - 9.9At or near total destruction – severe damage or collapse to all buildings. Heavy damage and shaking extends to distant locations. Permanent changes in ground topography.One per 10 to 50 years
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