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Seismology (//; from Greek σεισμός "earthquake" and -λογία "study of") 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 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.
- 1 Highlights of the history of seismology
- 2 Types of seismic wave
- 3 Earthquakes
- 4 Controlled seismic sources
- 5 Detection of seismic waves
- 6 Mapping the earth's interior
- 7 Seismology and society
- 8 Tools
- 9 Notable seismologists
- 10 See also
- 11 Notes
- 12 References
- 13 External links
Highlights of the history of seismology
Some milestones in the development of seismology are:
In 1664 Athanasius Kircher argued that earthquakes were caused by the movement of fire within a system of channels inside the Earth.
The Lisbon earthquake of 1755, coinciding with the general flowering of science in Europe, set in motion intensified scientific attempts to understand the behaviour and causation of earthquakes. The earliest responses include work by John Bevis (1757) and John Michell (1761). Michell determined that earthquakes originate within the Earth and were waves of movement caused by "shifting masses of rock miles below the surface".
From 1857 Robert Mallet laid the foundation of instrumental seismology and he carried out seismological experiments using explosives.
In 1910, after studying the 1906 San Francisco earthquake, Harry Fielding Reid put forward the "elastic rebound theory" which remains the foundation for modern tectonic studies. The development of this theory depended on the considerable progress of earlier independent streams of work on the behaviour of elastic materials and in mathematics.
In 1926 Harold Jeffreys was the first to claim, based on his study of earthquake waves, that below the crust, the core of the Earth is liquid.
In 1937 Inge Lehmann determined that within the earth's liquid outer core there is a solid inner core.
By the 1960s earth science had developed to the point where a comprehensive theory of the causation of seismic events had come together in the now well-established theory of plate tectonics.
Types of seismic wave
Seismic waves are elastic waves that propagate in solid or fluid materials. They can be divided into body waves that travel through the interior of the materials; surface waves that travel along surfaces or interfaces between materials; and normal modes, a form of standing wave.
There are two types of body wave, P-waves and S-waves (both body waves). Pressure waves or Primary waves (P-waves), are longitudinal waves that involve compression and rarefaction (expansion) in the direction that the wave is traveling. P-waves are the fastest waves in solids and are therefore the first waves to appear on a seismogram. S-waves, also called shear or secondary waves, are transverse waves that involve motion perpendicular to the direction of propagation. S-waves appear later than P-waves on a seismogram. Fluids cannot support this perpendicular motion, or shear, so S-waves only travel in solids. P-waves travel in both solids and fluids.
The two main kinds of surface wave are the Rayleigh wave,which has some compressional motion, and the Love wave, which does not. Such waves can be theoretically explained in terms of interacting P- and/or S-waves. Surface waves travel more slowly than P-waves and S-waves, but because they are guided by the surface of the Earth (and their energy is thus trapped near the Earth's surface) they can be much larger in amplitude than body waves, and can be the largest signals seen in earthquake seismograms. They are particularly strongly excited when their source is close to the surface of the Earth, as in a shallow earthquake or explosion.
The above waves are traveling waves. Large earthquakes can also make the Earth "ring" like a bell. This ringing is a mixture of normal modes with discrete frequencies and periods of an hour or shorter. Motion caused by a large earthquake can be observed for up to a month after the event. The first observations of normal modes were made in the 1960s as the advent of higher fidelity instruments coincided with two of the largest earthquakes of the 20th century - the 1960 Great Chilean Earthquake and the 1964 Great Alaskan Earthquake. Since then, the normal modes of the Earth have given us some of the strongest constraints on the deep structure of the Earth. See also free oscillations of the Earth.
One of the first attempts at the scientific study of earthquakes followed the 1755 Lisbon earthquake. Other especially notable earthquakes that spurred major developments in the science of seismology include the 1857 Basilicata earthquake, 1906 San Francisco earthquake, the 1964 Alaska earthquake, the 2004 Sumatra-Andaman earthquake, and the 2011 Great East Japan earthquake. An extensive list of famous earthquakes can be found on the List of earthquakes page.
Controlled seismic sources
Seismic waves produced by explosions or vibrating controlled sources are one of the primary methods of underground exploration in geophysics (in addition to many different electromagnetic methods such as induced polarization and magnetotellurics). Controlled-source seismology has been used to map salt domes, faults, anticlines and other geologic traps in petroleum-bearing rocks, geological faults, rock types, and long-buried giant meteor craters. For example, the Chicxulub Crater, which was caused by an impact that has been implicated in the extinction of the dinosaurs, was localized to Central America by analyzing ejecta in the Cretaceous–Paleogene boundary, and then physically proven to exist using seismic maps from oil exploration.
Detection of seismic waves
Seismometers are sensors that sense and record the motion of the Earth arising from elastic waves. Seismometers may be deployed at Earth's surface, in shallow vaults, in boreholes, or underwater. A complete instrument package that records seismic signals is called a seismograph. Networks of seismographs continuously record ground motions around the world to facilitate the monitoring and analysis of global earthquakes and other seismic sources. Rapid location of earthquakes makes tsunami warnings possible because seismic waves travel considerably faster than tsunami waves. Seismometers also record signals from non-earthquake sources ranging from explosions (nuclear and chemical), to local noise from wind or anthropogenic activities, to incessant signals generated at the ocean floor and coasts induced by ocean waves (the global microseism), to cryospheric events associated with large icebergs and glaciers. Above-ocean meteor strikes with energies as high as 4.2 × 1013 J (equivalent to that released by an explosion of ten kilotons of TNT) have been recorded by seismographs, as have a number of industrial accidents and terrorist bombs and events (a field of study referred to as forensic seismology). A major long-term motivation for the global seismographic monitoring has been for the detection and study of nuclear testing.
Mapping the earth's interior
Because seismic waves commonly propagate efficiently and interact with internal structure, they provide high-resolution noninvasive methods for studying Earth's interior. One of the earliest important discoveries (suggested by Richard Dixon Oldham in 1906 and definitively shown by Harold Jeffreys in 1926) was that the outer core of the earth is liquid. Since S-waves do not pass through liquids, the liquid core causes a "shadow" on the side of the planet opposite of the earthquake where no direct S-waves are observed. In addition, P-waves travel much slower through the outer core than the mantle.
Processing readings from many seismometers using seismic tomography, seismologists have mapped the mantle of the earth to a resolution of several hundred kilometers. This has enabled scientists to identify convection cells and other large-scale features such as Ultra Low Velocity Zones near the core–mantle boundary.
Seismology and society
Forecasting a probable timing, location, magnitude and other important features of a forthcoming seismic event is called earthquake prediction. Various attempts have been made by seismologists and others to create effective systems for precise earthquake predictions, including the VAN method. Most seismologists do not believe that a system to provide timely warnings for individual earthquakes has yet been developed, and many believe that such a system would be unlikely to give significant warning of impending seismic events. However, more general forecasts routinely predict seismic hazard. Such forecasts estimate the probability of an earthquake of a particular size affecting a particular location within a particular time-span, and they are routinely used in earthquake engineering.
Public controversy over earthquake prediction erupted after Italian authorities indicted six seismologists and one government official for manslaughter in connection with a magnitude 6.3 earthquake in L'Aquila, Italy on April 5, 2009. The indictment has been widely perceived[by whom?] as an indictment for failing to predict the earthquake and has drawn condemnation from the American Association for the Advancement of Science and the American Geophysical Union. The indictment claims that, at a special meeting in L'Aquila the week before the earthquake occurred, scientists and officials were more interested in pacifying the population than providing adequate information about earthquake risk and preparedness.
Seismological instruments can generate large amounts of data. Systems for processing such data include:
- Aki, Keiiti
- Don L. Anderson
- Bolt, Bruce
- Claerbout, Jon
- Dziewonski, Adam Marian
- Ewing, Maurice
- Galitzine, Boris Borisovich
- Gamburtsev, Grigory A.
- Gutenberg, Beno
- Hough, Susan
- Jeffreys, Harold
- Jones, Lucy
- Kanamori, Hiroo
- Keilis-Borok, Vladimir
- Knopoff, Leon
- Lehmann, Inge
- Mallet, Robert
- Mercalli, Giuseppe
- Milne, John
- Mohorovičić, Andrija
- Oldham, Richard Dixon
- Fusakichi Omori
- Sebastião de Melo, Marquis of Pombal
- Press, Frank
- Richards, Paul G.
- Richter, Charles Francis
- Sekiya, Seikei
- Sieh, Kerry
- Paul G. Silver
- Tucker, Brian
- Vidale, John
- Wen, Lianxing
- Winthrop, John
- Zhang Heng
- Ambient Vibrations
- Engineering geology
- Forensic seismology
- Free Geophysics Software
- The IRIS Consortium
- Isoseismal map
- Linear seismic inversion
- Seismic interferometry
- Seismic loading
- Seismic migration
- Seismic performance analysis
- Ben-Menahem, Ari (August 1995). "A Concise History of Mainstream Seismology: Origins, Legacy, and Perspectives" (PDF). Bulletin of the Seismological Society of America Vol. 85, No. 4. pp. 1202–1225. Retrieved 21 January 2013.
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- Akkar, Sinan; Polat, Gülkan; van Eck, Torild, eds. (2010). Earthquake Data in Engineering Seismology: Predictive Models, Data Management and Networks. Geotechnical, Geological and Earthquake Engineering 14. Springer. p. 194. ISBN 978-94-007-0151-9. Retrieved 2011-10-19.
- Allaby, Ailsa; Allaby, Michael, eds. (2003). Oxford Dictionary of Earth Sciences (Second ed.). Oxford University Press.
- Gubbins, David (1990). Seismology and Plate Tectonics. Cambridge University Press. ISBN 0-521-37141-4.
- Hall, Stephen S. (2011). "Scientists on trial: At fault?". Nature 477 (7364): 264–269. Bibcode:2011Natur.477..264H. doi:10.1038/477264a.
- Kanamori, Hiroo (2003). Earthquake prediction: An overview. International Handbook of Earthquake and Engineering Seismology 81B. International Association of Seismology & Physics of the Earth's Interior. pp. 1205–1216.
- Lay, Thorne, ed. (2009). Seismological Grand Challenges in Understanding Earth's Dynamic Systems. Report to the National Science Foundation, IRIS consortium.
- Schulte, Peter; Laia Alegret, Ignacio Arenillas, José A. Arz, Penny J. Barton, Paul R. Bown, Timothy J. Bralower, Gail L. Christeson, Philippe Claeys, Charles S. Cockell, Gareth S. Collins, Alexander Deutsch, Tamara J. Goldin, Kazuhisa Goto, José M. Grajales-Nishimura, Richard A. F. Grieve, Sean P. S. Gulick, Kirk R. Johnson, Wolfgang Kiessling, Christian Koeberl, David A. Kring, Kenneth G. MacLeod, Takafumi Matsui, Jay Melosh, Alessandro Montanari, Joanna V. Morgan, Clive R. Neal, Douglas J. Nichols, Richard D. Norris, Elisabetta Pierazzo, Greg Ravizza, Mario Rebolledo-Vieyra, Wolf Uwe Reimold, Eric Robin, Tobias Salge, Robert P. Speijer, Arthur R. Sweet, Jaime Urrutia-Fucugauchi, Vivi Vajda, Michael T. Whalen, Pi S. Willumsen (5 March 2010). "The Chicxulub Asteroid Impact and Mass Extinction at the Cretaceous-Paleogene Boundary". Science (AAAS) 327 (5970): 1214–1218. Bibcode:2010Sci...327.1214S. doi:10.1126/science.1177265. ISSN 1095-9203. PMID 20203042. Retrieved 5 March 2010.
- Shearer, Peter M. (2009). Introduction to Seismology (Second ed.). Cambridge University Press. ISBN 978-0-521-70842-5.
- Stein, Seth; Wysession, Michael (2002). An Introduction to Seismology, Earthquakes and Earth Structure. Wiley-Blackwell. ISBN 978-0-86542-078-6.
- Wen, Lianxing; Helmberger, Donald V. (1998). "Ultra-Low Velocity Zones Near the Core-Mantle Boundary from Broadband PKP Precursors". Science 279 (5357): 1701–1703. Bibcode:1998Sci...279.1701W. doi:10.1126/science.279.5357.1701.
|Wikimedia Commons has media related to Seismology.|
- European-Mediterranean Seismological Center, real-time earthquake information website.
- Seismological Society of America.
- Incorporated Research Institutions for Seismology.
- USGS Earthquake Hazards Program.