Earthquakes happen when there is a sudden movement of the rocks along a fault inside the Earth. As the rocks on either side of the fault move past each other, they send seismic waves through the Earth, radiating outwards like the ripples produced when a stone is dropped into a pond.
In this section:
How are earthquakes detected?
A seismogram is a record of the ground motions caused by seismic waves from an earthquake. A seismograph or seismometer is the measuring instrument that creates the seismogram. Almost all seismometers are based on the principle of inertia i.e. a suspended mass tends to remain still when the ground moves.
Seismometers allow us to detect and measure earthquakes by converting vibrations due to seismic waves into electrical signals, which we can then display as seismograms on a computer screen.
Seismologists study earthquakes and can use this data to determine where, and how big, a particular earthquake is.
There are two basic types of seismic wave that travel through the body of the Earth:
- P-waves: are longitudinal waves that consist of a series of compressions and dilations along the direction of travel. The P stands for Primary because they travel the fastest.
- S-waves: are transverse waves, whose motion is perpendicular to the direction of travel. The S stands for shear or secondary since they are slower than P-waves.
Where a free surface is present (like the Earth–air interface) these two types of motion can combine to form two other types of wave called surface waves that produce a type of shaking that causes buildings to fail and fall down. Rayleigh waves are generated by the interaction of P- and S- waves at the surface of the Earth, while Love waves are generated by interference of multiple shear waves. The ground motions from surface waves are often much larger than those motions from body waves.
|Type (and names)||Particle motion||Typical velocity||Other characteristics|
|Alternating compressions (‘pushes’) and dilations (‘pulls’) in the same direction as the wave is propagating||VP ~ 5 – 7 km/s in typical Earth’s crust :|
>~ 8 km/s in Earth’s mantle and core; 1.5 km/s in water; 0.3 km/s in air
|P motion travels fastest in materials, so the P-wave is the first-arriving energy on a seismogram. Generally smaller and higher frequency than the S and surface waves. P-waves in a liquid or gas are pressure waves, including sound waves.|
|Alternating transverse motions perpendicular to the direction of propagation.||VS ~ 3 – 4 km/s in typical Earth’s crust :|
>~ 4.5 km/s in Earth’s mantle; ~ 2.5-3.0 km/s in (solid) inner core
|S-waves do not travel through fluids, so do not exist in Earth’s liquid outer core or in air or water or molten rock (magma). S-waves travel slower than P-waves in a solid and, therefore, arrive after the P-wave.|
|Transverse horizontal motion, perpendicular to the direction of propagation and generally parallel to the Earth’s surface||VL ~ 2.0 – 4.5 km/s in the Earth depending on frequency of the propagating wave||Love waves exist because of the Earth’s surface. They are largest at the surface and decrease in amplitude with depth. Love waves are dispersive, that is, the wave velocity is dependent on frequency, with low frequencies normally propagating at higher velocity. Depth of penetration of the Love waves is also dependent on frequency, with lower frequencies penetrating to greater depth.|
|Motion is both in the direction of propagation and perpendicular (in a vertical plane)||VR ~ 2.0 – 4.5 km/s in the Earth depending on frequency of the propagating||Rayleigh waves are also dispersive and the amplitudes generally decrease with depth in the Earth. Appearance and particle motion are similar to water waves.|
How are earthquakes located?
Earthquakes generate different types of seismic waves and these travel at different speeds through the Earth. P-waves are fastest and are the first signal to arrive on a seismogram , followed by the slower S-wave, then the surface waves. The arrival times of the P- and S-waves at different seismometers are used to determine the location of the earthquake. Assuming that we know the relative speed of P- and S-waves, the time difference between the arrivals of the P- and S-waves determines the distance the earthquake is from the seismometer.
By looking at the seismograms from different recording stations, we can find out the epicentre of the earthquake. The signals arrive first at the closest station and last at the one furthest away. The time difference between the P- and S-waves tells us the distance the earthquake is from the seismograph. If we calculate the S minus P time to determine distance from the seismometer, at all three stations, we can work out where the epicentre of the earthquake is.
How are earthquakes measured?
Measurement of the severity of an earthquake can be expressed in several ways, but the two most common scales used by seismologists are intensity and magnitude.
- Earthquake intensity is a qualitative measure of the strength of shaking caused by an earthquake determined from the observed effects on people, objects and buildings. This usually decreases with distance from the epicentre.
- Magnitude is a measure of the amount of energy released during an earthquake and can be estimated from the amplitude of ground motions recorded by seismometers. It is independent of distance from the epicentre.
Intensity is a measure of the strength of shaking caused by an earthquake. For a given earthquake the intensity normally decreases with distance from the epicentre. There are a number of different intensity scales in use around the world based on the shaking people experience, and the effects it has on objects and buildings. It is also possible to estimate intensity from recordings of ground motions. In the UK, we use the European Macroseismic scale (EMS) to quantify the effect of earthquake shaking on people, objects and buildings. Estimates of intensity from different locations can be combined to make macroseismic maps that show how the strength of shaking varies.
Earthquake magnitude is a measure of the amount of energy released during an earthquake. A number of different magnitude scales have been developed, which are generally based on the amplitude of different parts of the observed record of ground motion.
Since earthquake intensity can be related to what people feel or experience during the shaking from an earthquake it is possible to use people as ‘intensity sensors’ and collect earthquake felt reports for significant earthquakes. For example:
Scientists can make use of these felt report surveys to compare the size of recent earthquakes to ones which occurred before modern scientific measurements (from about 1970 in the UK), but for which contemporary written reports are available. In this way earthquake records in the UK can be extrapolated back to the 14th century.
|1||Not felt||Not felt, even under the most favourable circumstances.|
|2||Scarcely felt||Vibration is felt only by individual people at rest in houses, especially on upper floors of buildings.|
|3||Weak||The vibration is weak and is felt indoors by a few people. People at rest feel a swaying or light trembling.|
|4||Largely observed||The earthquake is felt indoors by many people, outdoors by very few. A few people are awakened. The level of vibration is not frightening. Windows, doors and dishes rattle. Hanging objects swing.|
|5||Strong||The earthquake is felt indoors by most, outdoors by few. Many sleeping people awake. A few run outdoors. Buildings tremble throughout. Hanging objects swing considerably. China and glasses clatter together. The vibration is strong. Top heavy objects topple over. Doors and windows swing open or shut.|
|6||Slightly damaging||Felt by most indoors and by many outdoors. Many people in buildings are frightened and run outdoors. Small objects fall. Slight damage to many ordinary buildings e.g.; fine cracks in plaster and small pieces of plaster fall.|
|7||Damaging||Most people are frightened and run outdoors. Furniture is shifted and objects fall from shelves in large numbers. Many ordinary buildings suffer moderate damage: small cracks in walls; partial collapse of chimneys.|
|8||Heavily damaging||Furniture may be overturned. Many ordinary buildings suffer damage: chimneys fall; large cracks appear in walls and a few buildings may partially collapse.|
|9||Destructive||Monuments and columns fall or are twisted. Many ordinary buildings partially collapse and a few collapse completely.|
|10||Very destructive||Many ordinary buildings collapse.|
|11||Devastating||Most ordinary buildings collapse.|
|12||Completely devastating||Practically all structures above and below ground are heavily damaged or destroyed.|
Abstracted from – Grünthal, G., (ed.), (1998). “European Macroseismic Scale 1998”, Cahiers du Centre Européen de Géodynamique et de Séismologie Volume 15, Luxembourg.
Earthquake magnitude is a measure of the amount of energy released during an earthquake. A number of different magnitude scales have been developed based on the amplitude of different parts of the observed record of ground motion with specific corrections for distance. Earthquake magnitude scales are logarithmic, i.e. a 1 unit increase in magnitude corresponds to a 10 fold increase in amplitude.
The first magnitude scale was developed by Charles Richter in 1935 using observations of earthquakes in Southern California and although the scale is only strictly applicable there, it has been used all around the world. Press reporters love the Richter scale and will report any earthquake magnitude as a ‘magnitude on the Richter scale’. However, for any large earthquake that has made the news, it is very unlikely that a Richter (or Local magnitude) is an appropriate scale.
Due to the complexities of the calculations the reported magnitude of events can change as more data gets analysed. For the devastating 24 December 2004 event in Sumatra the original magnitude of Mw 9.0 was recalculated several months later to Mw 9.3 as more data was analysed.
We can’t directly measure the size of an earthquake, because of all the complex and inaccessible geology that lies hidden beneath the surface of the Earth.
Seismologists have to use various methods to try and measure earthquakes by the effects they produce at the surface.
Nowadays, the most standard and reliable measure of earthquake size is moment magnitude (Mw), which is based on seismic moment. Moment is related to the area of the earthquake fault rupture and the amount of slip on the rupture, as well as the strength of the rocks themselves. Richter’s original magnitude scale underestimates the size of large events, however, the constants used in the definition of moment magnitude (Mw) were chosen so that the magnitude numbers for Richter and moment magnitudes match for smaller events.
Seismic moment (Mo) = μ* rupture area * slip length
where μ is the shear modulus of the crust (approx 3×1010 N/m)
Moment magnitude (Mw) = 2/3log(Mo) – 6.06
Originally earthquake magnitudes were based on the amplitude of ground motion displacement as measured by a standard seismograph. The best known of these is the Richter Magnitude which was defined for local earthquakes in southern California.
ML = logA + 2.56logD – 1.67
Where A is the measured ground motion (in micrometres) and D is the distance from the event (in km). This is still used for measuring the magnitude of shallow events at distances less than 600 km (today called the Local Magnitude). For events larger than magnitude 8 this scale saturates and gives magnitude estimates that are too small.
For earthquakes measured at distances greater than 600 km magnitude can be estimated from the formula.
Mb = log(A/T) + σ(D,h)
Where A is the maximum amplitude (in micrometres)of the P-waves measured at period T (generally about one second) and σ is a calibration term (in the range 6–8) that depends on distance from the event D and depth of the event h (tables of σ are used).
For shallow earthquakes (i.e. ones that generate surface waves) magnitudes can be estimated using the formula.
MS = log(A/T) + 1.66logΔ + 3.3
Where A is the maximum amplitude (in micrometres) of the Rayleigh waves, T is the period (usually about 20 seconds) and Δ is the distance (in degrees).
Earthquake energy as a function of magnitude. Both the magnitude and the seismic moment are related to the amount of energy that is radiated by an earthquake.
|Magnitude||Energy in joules||Notes|
|-3.0||2||1 kg dropped 20 cm|
|-1.0||2000||100 kg person jumps down 2 m|
|0.0||6.3 x 104|
|1.0||2.0 x 106|
|2.0||6.3 x 107||Only felt nearby|
|3.0||2.0 x 109||Energy from 50 litres of petrol|
|4.0||6.3 x 1010||Often felt up to 10’s of miles away|
|5.0||2.0 x 1012||Energy from 50 000 litres of petrol|
|6.0||6.3 x 1013||3.3 Hiroshima-size A bombs|
|7.0||2.0 x 1015|
|8.0||6.3 x 1016||1–2 earthquakes this size each year|
|9.0||2.0 x 1018||Total annual energy use of UK|