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The asthenosphere shown at a subduction boundary

The asthenosphere (Ancient Greek: ἀσθενός [asthenos] meaning "without strength" and σφαίρα [sphaira] meaning "sphere") is the highly viscous, mechanically weak,[1] and ductile region of the upper mantle of Earth. It lies below the lithosphere, between approximately 80 and 200 km (50 and 120 miles) below the surface. The lithosphere–asthenosphere boundary is usually referred to as the LAB.[2][3] The asthenosphere is almost solid, although some of its regions are molten (e.g., below mid-ocean ridges). The lower boundary of the asthenosphere within the mantle is not well defined. The thickness of the asthenosphere depends mainly on temperature. However, the rheology of the asthenosphere also depends on the rate of deformation,[4][5][full citation needed] which suggests that the asthenosphere could be also formed as a result of a high rate of deformation. In some regions, the asthenosphere could extend as deep as 700 km (430 mi). It is considered the source of mid-ocean ridge basalt (MORB).[6]


The asthenosphere is a part of the upper mantle just below the lithosphere that is involved in plate tectonic movement and isostatic adjustments. The lithosphere-asthenosphere boundary is conventionally taken at the 1300 °C isotherm. Below this temperature (closer to the surface) the mantle behaves rigidly; above this temperature (deeper below the surface) it acts in a ductile fashion.[7]

Seismic waves pass relatively slowly through the asthenosphere[8] compared to the overlying lithospheric mantle, thus it has been called the low-velocity zone (LVZ), although the two are not the same.[9][10] This was the observation that originally alerted seismologists to its presence and gave some information about its physical properties, as the speed of seismic waves decreases with decreasing rigidity. This decrease in seismic wave velocity from the lithosphere to the asthenosphere could be caused by the presence of a very small percentage of melt in the asthenosphere. The lower boundary of the LVZ lies at a depth of 180–220 km,[11] whereas the base of the asthenosphere lies at a depth of about 700 km.[12]

In the oceanic mantle, the transition from the lithosphere to the asthenosphere (the LAB) is shallower than for the continental mantle (about 60 km in some old oceanic regions) with a sharp and large velocity drop (5–10%).[13] At the mid-ocean ridges, the LAB rises to within a few kilometers of the ocean floor.

The upper part of the asthenosphere is believed to be the zone upon which the great rigid and brittle lithospheric plates of the Earth's crust move about. Due to the temperature and pressure conditions in the asthenosphere, rock becomes ductile, moving at rates of deformation measured in cm/yr over lineal distances eventually measuring thousands of kilometers. In this way, it flows like a convection current, radiating heat outward from the Earth's interior. Above the asthenosphere, at the same rate of deformation, rock behaves elastically and, being brittle, can break, causing faults. The rigid lithosphere is thought to "float" or move about on the slowly flowing asthenosphere, allowing the movement of tectonic plates.[14][15]

See also[edit]


  1. ^ Barrel, J. (1914). "The strength of the crust, Part VI. Relations of isostatic movements to a sphere of weakness – the asthenosphere". The Journal of Geology. 22 (7): 655–683. Bibcode:1914JG.....22..655B. doi:10.1086/622181. JSTOR 30060774. S2CID 224832862.
  2. ^ Harsh Gupta (29 June 2011). Encyclopedia of Solid Earth Geophysics. Springer Science & Business Media. p. 1062. ISBN 978-90-481-8701-0.
  3. ^ Lev Eppelbaum; Izzy Kutasov; Arkady Pilchin (29 April 2014). Applied Geothermics. Springer Science & Business. p. 318. ISBN 978-3-642-34023-9.
  4. ^ Czechowski, L.; Grad, M. (19 February 2018). "Two mechanisms of formation of asthenospheric layers". arXiv:1802.06843 [physics.geo-ph]. Bibcode:2018arXiv180206843C.
  5. ^ Czechowski, Leszek; Grad, Marek (2014). "Evolution of asthenospheric layers as a result of changing stress field" (PDF). Geophysical Research Abstracts. EGU General Assembly. 16 (EGU2014-10790): 10790. Bibcode:2014EGUGA..1610790C.
  6. ^ Hofmann, A. W. (1997). "Mantle geochemistry: the message from oceanic volcanism". Nature. 385 (6613): 219–228. Bibcode:1997Natur.385..219H. doi:10.1038/385219a0. S2CID 11405514.
  7. ^ Self, Steve; Rampino, Mike (2012). "The Crust and Lithosphere". Geological Society of London. Retrieved 27 January 2013.
  8. ^ Forsyth, Donald W. (1975). "The early structural evolution and anisotropy of the oceanic upper mantle". Geophysical Journal International. 43 (1): 103–162. Bibcode:1975GeoJ...43..103F. doi:10.1111/j.1365-246X.1975.tb00630.x.
  9. ^ Philip Kearey (17 July 2009). The Encyclopedia of the Solid Earth Sciences. John Wiley & Sons. pp. 36–. ISBN 978-1-4443-1388-8.
  10. ^ Lev Eppelbaum; Izzy Kutasov; Arkady Pilchin (29 April 2014). Applied Geothermics. Springer Science & Business. pp. 318–. ISBN 978-3-642-34023-9.
  11. ^ Condie, Kent C. (1997). Plate tectonics and crustal evolution. Butterworth-Heinemann. p. 123. ISBN 978-0-7506-3386-4. Retrieved 21 May 2010.
  12. ^ Kearey, Philip; Vine, Frederick J. (1996). Global Tectonics (2 ed.). Wiley-Blackwell. pp. 41–42. ISBN 978-0-86542-924-6. Retrieved 21 May 2010.
  13. ^ Rychert, Catherine A.; Shearer, Peter M. (2011). "Imaging the lithosphere-asthenosphere boundary beneath the Pacific using SS waveform modeling". Journal of Geophysical Research: Solid Earth. 116 (B7): B07307. Bibcode:2011JGRB..116.7307R. doi:10.1029/2010JB008070.
  14. ^ Mark Hendrix; Graham R. Thompson (24 January 2014). EARTH2. Cengage Learning. pp. 493–. ISBN 978-1-305-43687-9.
  15. ^ Tom S. Garrison; Robert Ellis (5 December 2016). Essentials of Oceanography. Cengage Learning. pp. 19–. ISBN 978-1-337-51538-2.


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