# Lithosphere: Wikis

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# Encyclopedia

The tectonic plates of the lithosphere on Earth
Earth cutaway from core to exosphere

The lithosphere (IPA: [ˈlɪθ.əˌsfɪəɹ], from the Greek λίθος [lithos] for "rocky" + σφαῖρα [sphaira] for "sphere") is the rigid[1] outermost shell of a rocky planet. It comprises the crust and the portion of the upper mantle that behaves elastically on time scales of thousands of years or greater.

## Earth's lithosphere

In the Earth, the lithosphere includes the crust and the uppermost mantle, which constitute the hard and rigid outer layer of the Earth. The lithosphere is underlain by the asthenosphere, the weaker, hotter, and deeper part of the upper mantle. The boundary between the lithosphere and the underlying asthenosphere is defined by a difference in response to stress: the lithosphere remains rigid for very long periods of geologic time in which it deforms elastically and through brittle failure, while the asthenosphere deforms viscously and accommodates strain through plastic deformation. The lithosphere is broken into tectonic plates.

The concept of the lithosphere as Earth’s strong outer layer was developed by Barrell, who wrote a series of papers introducing the concept.[2][3][4] The concept was based on the presence of significant gravity anomalies over continental crust, from which he inferred that there must exist a strong upper layer (which he called the lithosphere) above a weaker layer which could flow (which he called the asthenosphere). These ideas were expanded by Daly (1940)[5], and have been broadly accepted by geologists and geophysicists. Although these ideas about lithosphere and asthenosphere were developed long before plate tectonic theory was articulated in the 1960s, the concepts that strong lithosphere exists and that this rests on weak asthenosphere are essential to that theory.

The lithosphere provides a conductive lid atop the convecting mantle; as such, it affects heat transport through the Earth.

There are two types of lithosphere:

• Oceanic lithosphere, which is associated with Oceanic crust and exists in the ocean basins
• Continental lithosphere, which is associated with Continental crust

The thickness of the lithosphere is considered to be the depth to the isotherm associated with the transition between brittle and viscous behavior[6]. The temperature at which olivine begins to deform viscously (~1000°C) is often used to set this isotherm because olivine is generally the weakest mineral in the upper mantle. Oceanic lithosphere is typically about 50-100 km thick (but beneath the mid-ocean ridges is no thicker than the crust), while continental lithosphere has a range in thickness from about 40 km to perhaps 200 km; the upper ~30 to ~50 km of typical continental lithosphere is crust. The mantle part of the lithosphere consists largely of peridotite. The crust is distinguished from the upper mantle by the change in chemical composition that takes place at the Moho discontinuity.

### Oceanic lithosphere

Oceanic lithosphere consists mainly of mafic crust and ultramafic mantle (peridotite) and is denser than continental lithosphere, for which the mantle is associated with crust made of felsic rocks. Oceanic lithosphere thickens as it ages and moves away from the mid-ocean ridge. This thickening occurs by conductive cooling, which converts hot asthenosphere into lithospheric mantle, and causes the oceanic lithosphere to become increasingly thick and dense with age. The thickness of the mantle part of the oceanic lithosphere can be approximated as a thermal boundary layer that thickens as the square root of time.

$\, h \, \sim \, 2\, \sqrt{ \kappa t } \,$

Here, h is the thickness of the oceanic mantle lithosphere, κ is the thermal diffusivity (approximately 10-6 m2/s), and t is time.

Oceanic lithosphere is less dense than asthenosphere for a few tens of millions of years, but after this becomes increasingly denser than asthenosphere. This is because the chemically-differentiated oceanic crust is lighter than asthenosphere, but due to thermal contraction, the mantle lithosphere is more dense than the asthenosphere. The gravitational instability of mature oceanic lithosphere has the effect that at subduction zones, oceanic lithosphere invariably sinks underneath the overriding lithosphere, which can be oceanic or continental. New oceanic lithosphere is constantly being produced at mid-ocean ridges and is recycled back to the mantle at subduction zones. As a result, oceanic lithosphere is much younger than continental lithosphere: the oldest oceanic lithosphere is about 170 million years old, while parts of the continental lithosphere are billions of years old. The oldest parts of continental lithosphere underlie cratons, and the mantle lithosphere there is thicker and less dense than typical; the relatively low density of such mantle "roots of cratons" helps to stabilize these regions.[7][8]

## Subducted lithosphere

Geophysical studies in the early 21st Century posit that large pieces of the lithosphere have been subducted into the mantle as deep as 2900 km to near the core-mantle boundary[9], while others "float" in the upper mantle,[10][11] while some stick down into the mantle as far as 400 km but remain "attached" to the continental plate above,[12] similar to the extent of the "tectosphere" proposed by Jordan in 1988.[13]

## Mantle xenoliths

Geoscientists can directly study the nature of the subcontinental mantle by examining mantle xenoliths brought up in kimberlite and other volcanic pipes. The histories of these xenoliths have been investigated by many methods, including analyses of abundances of isotopes of osmium and rhenium. Such studies have confirmed that mantle lithospheres below some cratons have persisted for periods in excess of 3 billion years, despite the mantle flow that accompanies plate tectonics.[14]

## References

### Footnotes

1. ^ Skinner, B.J. & Porter, S.C.: Physical Geology, page 17, chapt. The Earth: Inside and Out, 1987, John Wiley & Sons, ISBN 0-471-05668-5
2. ^ Barrell, J. 1914 The strength of the Earth's crust. Journal of Geology.22, 425-433.
3. ^ Barrell, J. 1914 The strength of the Earth's crust. Journal of Geology 22, 441-468.
4. ^ Barrell, J. 1914 The strength of the Earth's crust. Journal of Geology 22, 655-683.
5. ^ Daly, R. 1940 Strength and structure of the Earth. New York: Prentice-Hall.
6. ^ Parsons, B. and McKenzie, D. 1978. Mantle Convection and the thermal structure of the plates. Journal of Geophysical Research.
7. ^ Jordan, T. H. 1978 Composition and development of the continental tectosphere. Nature 274, 544-548.
8. ^ O’Reilly, Suzanne Y. et al. (2009) "Ultradeep continental roots and their oceanic remnants: A solution to the geochemical “mantle reservoir” problem?" LITHOS doi: 10.1016/j.lithos.2009.04.028
9. ^ Burke, K. and Torsvik, T. H. (2004) "Derivation of Large Igneous Provinces of the past 200 million years from long-term heterogeneities in the deep mantle Earth and Planetary Science Letters 227: pp. 531-538
10. ^ Replumaz, A. et al. (2004) "4-D evolution of SE Asia's mantle from geological reconstructions and seismic tomography" Earth and Planetary Science Letters 221: pp. 103-115, doi:10.1016/S0012-821X(04)00070-6
11. ^ Li, Chang et al. (2008) "A new global model for P wave speed variations in Earth's mantle" Geochemistry Geophysics Geosystems 9(5): Q05018, doi: 10.1029/2007GC001806
12. ^ O’Reilly, Suzanne Y. et al. (2009) "Ultradeep continental roots and their oceanic remnants: A solution to the geochemical “mantle reservoir” problem" Lithos doi:10.1016/j.lithos.2009.04.028
13. ^ Jordan, T.H. (1988) "Structure and formation of the continental tectosphere" Journal of Petrology 29(Special Lithosphere Issue): pp. 11-38
14. ^ Carlson, R. W., Pearson, D. G., and James, D. E., 2004, Physical, chemical, and chronological characteristics of continental mantle. Reviews of Geophysics 43, 8755-1209/05/2004RG000156.

### Notations

• Stanley Chernicoff and Donna Whitney. Geology. An Introduction to Physical Geology, 4th ed., Pearson 1990

# Study guide

Up to date as of January 14, 2010

### From Wikiversity

lithosphere is the upper, rigid layer of the earth. it consists of the crust and the top of the mantle. it is about 100 km thick. the lithosphere was discovered by seismology, which means listening to pattern of vibratons from earthquakes.

# 1911 encyclopedia

Up to date as of January 14, 2010

### From LoveToKnow 1911

LITHOSPHERE (Gr. %Coos, a stone, and a'aapa, a sphere), the crust of the earth surrounding the earth's nucleus. The superficial soil, a layer of loose earthy material from a few feet to a few hundreds of feet in thickness, lies upon a zone of hard rock many thousands of feet in thickness but varying in character, and composed mainly of sandstones, shales, clays, limestones and metamorphic rocks. These two layers form the lithosphere. All the tectonic movements of the solid nucleus produce changes in the mobile lithosphere. Volcanic and seismic activity is manifested, mountains are folded, levels change, fresh surfaces are exposed to denudation, erosion and deposition. The crust is thus subject to constant change while retaining its more or less permanent character.

# Simple English

[[File:|thumb|230px|Earth cutaway]]

File:Plates tect2
The tectonic plates of the lithosphere.

The lithosphere[1] is the solid shell of the planet Earth. That means the crust and the the part of the upper mantle that behaves elastically on time scales of thousands of years or greater.

Under the lithosphere there is the asthenosphere, the weaker, hotter, and deeper part of the upper mantle. This part can flow.

The lithosphere provides a conductive lid atop the convecting mantle; as such, it affects heat transport through the Earth.

## Types of lithosphere

There are two types of lithosphere:

1. Oceanic lithosphere, which is associated with oceanic crust and exists in the ocean basins. Oceanic lithosphere is typically about 50–100 km thick
2. Continental lithosphere, which is associated with continental crust. Continental lithosphere has a range in thickness from about 40 km to perhaps 200 km, of which about 40 km is crust.

The lithosphere is divided into tectonic plates, which move gradually relative to one another.

Oceanic lithosphere thickens as it ages and moves away from the mid-ocean ridge. This thickening occurs by conductive cooling, which converts hot asthenosphere into lithospheric mantle, and causes the oceanic lithosphere to become increasingly dense with age. Oceanic lithosphere is less dense than asthenosphere for a few tens of millions of years, but after this becomes increasingly denser than asthenosphere.

When a continental plate comes together with an oceanic plate, at subduction zones, the oceanic lithosphere always sinks beneath the continental.

New oceanic lithosphere is constantly being produced at mid-ocean ridges and is recycled back to the mantle at subduction zones. As a result, oceanic lithosphere is much younger than continental lithosphere: the oldest oceanic lithosphere is about 200 million years old, while parts of the continental lithosphere are billions of years old.

Another distinguishing characteristic of the lithosphere is its flow properties. Under the influence of the low-intensity, long-term stresses that drive tectonic motion, the lithosphere responds essentially as a rigid shell and thus deforms primarily through brittle failure, whereas the asthenosphere (the layer of the mantle below the lithosphere) is heat-softened and accommodates strain through plastic deformation.

## Other sources

• Earth's Crust, Lithosphere and Asthenosphere
• Crust and Lithosphere
• Barrell, J. 1914a The strength of the Earth's crust. Journal of Geology.22, 425-433.
• Barrell, J. 1914b The strength of the Earth's crust. Journal of Geology 22, 441-468.
• Barrell, J. 1914c The strength of the Earth's crust. Journal of Geology 22, 655-683.
• Daly, R. 1940 Strength and structure of the Earth. New York: Prentice-Hall.
• Stanley Chernicoff and Donna Whitney. Geology. An Introduction to Physical Geology, 4th ed., Pearson 2007

## References

1. IPA: lith'usfēr, from the Greek for "rocky" sphere