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introduced a method for determining elastic-rebound strain increments of earthquakes on a particular fault. He determined that the square root of an earthquake's energy is proportional to both the elastic rebound strain increment and the rebound displacement, and developed a way to determine whether
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at the interface of the two plates, because the asthenosphere is weak and cannot support the stresses necessary for faulting. In this region, internal deformation of the still-cool down-going slab is the source of the earthquakes. Up to depths of 300 km, dehydration reactions and the formation
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portion of the down-going lithosphere, is still debated; the global ubiquity of double
Benioff zones indicates that it must be a process that commonly occurs in subduction zones. Some of the suggested instability mechanisms include dehydration embrittlement caused by the breakdown of antigorite or
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In some cases, subduction zones show two parallel surfaces of seismicity separated by tens of kilometres at intermediate depths (50–200 km). A primary example of this is located along Japan's largest island of Honshu, where the Wadati–Benioff zone is characterized by two well-defined lines of
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is hotter and more buoyant, resulting in shallow-dipping
Benioff zones, whereas older lithosphere is denser and colder, causing steeper dips. The Benioff zone spans from near-surface to depths of up to 670 km. The upper bound is just beneath the weak sediments in the toe of the wedge of the
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chlorite in a hydrated peridotite upper mantle, and un-bending of the slab. Observations from seismic studies indicate that the lithospheric mantle at the intermediate depths where double
Benioff zones occur is dry, which favours the proposed slab-unbending mechanism.
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The uppermost seismicity surface is in the crust of the down-going slab and attributed to the dehydration reactions within this oceanic crust resulting in the formation of eclogite. The mechanism behind the lower zone of seismicity, located in the
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and the South
American subduction zone, and determined that in both locations, earthquake foci fall along planes dipping ~45° from the trenches. These planes of seismicity were later termed Benioff zones, or Wadati–Benioff zones for
175:, in the interior of the slab that has not yet heated up to match the temperature of the surrounding mantle into which it is being subducted. At depths below the thickness of the lithosphere, earthquakes are no longer generated by
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earthquake foci, with a distance between each line of 30–40 kilometers. A study of the global prevalence of double
Benioff zones has found that they are common in subduction zones worldwide.
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The angle of dip of the subducting slab, and therefore the
Benioff seismic zone, is dominantly controlled by the negative buoyancy of the slab and forces from the flowing of the
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are the main causes of seismicity. Below 300 km, beginning at approximately the 700 °C isotherm, a mineralogical phase change from
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subduction zone, and the lower bound is where the brittle-ductile transition occurs. Most earthquakes occur within the 1000 °C
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or slip on faults within the downgoing plate, as a result of bending and extension as the plate is pulled into the mantle. The
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along the zone allow seismologists to map the three-dimensional surface of a subducting slab of oceanic crust and mantle.
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Brudzinski, M.R.; Thurber, C.H.; Hacker, B.R.; Engdahl, E.R. (2007). "Global prevalence of double
Benioff zones".
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occurs, and is thought to be the dominant earthquake mechanism of these very deep-seated earthquakes.
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a series of earthquakes was generated along a single fault structure. His research focused on the
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506:"Earthquakes and plastic deformation of anhydrous slab mantle in double Wadati-Benioff zones"
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How to Build a
Habitable Planet: The Story of Earth from the Big Bang to Humankind
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above active subduction zones. They can be produced by slip along the subduction
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Benioff, Hugo (1949). "Seismic evidence for the fault origin of oceanic deeps".
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Green, H. W. (1994). "Solving the paradox of deep earthquakes".
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Planar zone of seismicity corresponding with the down-going slab
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229:"Benioff zone (seismic belt) – Britannica Online Encyclopedia"
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Earthquakes: 2006 Centennial Update – The 1906 Big One
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zone. Differential motion along the zone produces numerous
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10.1130/0016-7606(1949)60[1837:seftfo]2.0.co;2
250:"Developing the theory [This Dynamic Earth, USGS]"
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422:"Rheological controls of Wadati–Benioff zone seismicity"
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Langmuir, Charles H.; Broecker, Wally (2012-07-22).
297:Benioff Zone | World of Earth Science Summary
504:Reynard, B.; Nakajima, J.; Kawakatsu, H. (2010).
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116:Wadati–Benioff zone earthquakes develop beneath
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405:Keary, P.; Klepeis, K.A.; Vines, F.J. (2012).
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274:. Princeton University Press. p. 298.
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409:. Wiley-Blackwell. pp. 225–264.
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484:10.1038/scientificamerican0994-64
420:Brodholt, J.; Stein, S. (1988).
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147:Kermadec-Tonga subduction zone
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45:Seismicity cross-section,
557:W. H. Freeman and Company
356:Suzuki, Yasumoto (2001).
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51:15 November 2006, 8.3 M
130:deep-focus earthquakes
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196:Double Benioff zones
118:volcanic island arcs
75:Benioff seismic zone
596:2007Sci...316.1472B
590:(5830): 1472–1474.
525:2010GeoRL..3724309R
476:1994SciAm.271c..64G
441:1988GeoRL..15.1081B
335:1949GSAB...60.1837B
122:continental margins
67:Benioff–Wadati zone
63:Wadati–Benioff zone
555:(Fifth ed.),
227:Related Articles.
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91:earthquakes
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256:2010-03-02
235:2010-03-02
214:References
166:. Younger
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600:CiteSeerX
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158:Structure
140:In 1949,
136:Discovery
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