Internal structure of Earth explained

The internal structure of Earth are the layers of the Earth, excluding its atmosphere and hydrosphere. The structure consists of an outer silicate solid crust, a highly viscous asthenosphere, and solid mantle, a liquid outer core whose flow generates the Earth's magnetic field, and a solid inner core.

Scientific understanding of the internal structure of Earth is based on observations of topography and bathymetry, observations of rock in outcrop, samples brought to the surface from greater depths by volcanoes or volcanic activity, analysis of the seismic waves that pass through Earth, measurements of the gravitational and magnetic fields of Earth, and experiments with crystalline solids at pressures and temperatures characteristic of Earth's deep interior.

Global properties

Chemical composition of the upper internal structure of Earth[1] !Chemical element!Continental crust (%)!Upper mantle (%)!Pyrolite model (%)!Chondrite model (1) (%)!Chondrite model (2) (%)
MgO4.436.638.126.338.1
Al2O315.84.64.62.73.9
SiO259.145.445.129.843.2
CaO6.43.73.12.63.9
FeO6.68.17.96.49.3
Other oxides7.71.41.2N/A5.5
FeN/A N/AN/A25.8N/A
NiN/A N/AN/A1.7N/A
SiN/AN/AN/A3.5N/A
Note: In chondrite model (1), the light element in the core is assumed to be Si. Chondrite model (2) is a model of chemical composition of the mantle corresponding to the model of core shown in chondrite model (1).Measurements of the force exerted by Earth's gravity can be used to calculate its mass. Astronomers can also calculate Earth's mass by observing the motion of orbiting satellites. Earth's average density can be determined through gravimetric experiments, which have historically involved pendulums. The mass of Earth is about .[2] The average density of Earth is .[3]

Layers

The structure of Earth can be defined in two ways: by mechanical properties such as rheology, or chemically. Mechanically, it can be divided into lithosphere, asthenosphere, mesospheric mantle, outer core, and the inner core. Chemically, Earth can be divided into the crust, upper mantle, lower mantle, outer core, and inner core. The geologic component layers of Earth are at increasing depths below the surface:[4]

Crust and lithosphere

See main article: Earth's crust and Lithosphere. Earth's crust ranges from 5–[5] in depth and is the outermost layer.[6] The thin parts are the oceanic crust, which underlie the ocean basins (5–10 km) and is mafic-rich[7] (dense iron-magnesium silicate mineral or igneous rock).[8] The thicker crust is the continental crust, which is less dense[9] and is felsic-rich (igneous rocks rich in elements that form feldspar and quartz).[10] The rocks of the crust fall into two major categories – sial (aluminium silicate) and sima (magnesium silicate).[11] It is estimated that sima starts about 11 km below the Conrad discontinuity,[12] though the discontinuity is not distinct and can be absent in some continental regions.[13]

Earth's lithosphere consists of the crust and the uppermost mantle.[14] The crust-mantle boundary occurs as two physically different phenomena. The Mohorovičić discontinuity is a distinct change of seismic wave velocity. This is caused by a change in the rock's density – Immediately above the Moho, the velocities of primary seismic waves (P wave) are consistent with those through basalt (6.7–7.2 km/s), and below they are similar to those through peridotite or dunite (7.6–8.6 km/s).[15] Second, in oceanic crust, there is a chemical discontinuity between ultramafic cumulates and tectonized harzburgites, which has been observed from deep parts of the oceanic crust that have been obducted onto the continental crust and preserved as ophiolite sequences.

Many rocks making up Earth's crust formed less than 100 million years ago; however, the oldest known mineral grains are about 4.4 billion years old, indicating that Earth has had a solid crust for at least 4.4 billion years.[16]

Mantle

See main article: Earth's mantle. Earth's mantle extends to a depth of 2890km (1,800miles), making it the planet's thickest layer.[17] [This is 45% of the {{convert|6,371|km|abbr=on}} radius, and 83.7% of the volume - 0.6% of the volume is the crust].The mantle is divided into upper and lower mantle[18] separated by a transition zone.[19] The lowest part of the mantle next to the core-mantle boundary is known as the D″ (D-double-prime) layer.[20] The pressure at the bottom of the mantle is ≈140 GPa (1.4 Matm).[21] The mantle is composed of silicate rocks richer in iron and magnesium than the overlying crust.[22] Although solid, the mantle's extremely hot silicate material can flow over very long timescales.[23] Convection of the mantle propels the motion of the tectonic plates in the crust. The source of heat that drives this motion is the decay of radioactive isotopes in Earth's crust and mantle combined with the initial heat from the planet's formation[24] (from the potential energy released by collapsing a large amount of matter into a gravity well, and the kinetic energy of accreted matter).

Due to increasing pressure deeper in the mantle, the lower part flows less easily, though chemical changes within the mantle may also be important. The viscosity of the mantle ranges between 1021 and 1024 pascal-second, increasing with depth.[25] In comparison, the viscosity of water at is 0.89 millipascal-second [26] and pitch is (2.3 ± 0.5) × 108 pascal-second.[27]

Core

See main article: Earth's inner core and Earth's outer core. Earth's outer core is a fluid layer about 2260km (1,400miles) in height (i.e. distance from the highest point to the lowest point at the edge of the inner core) [36% of the Earth's radius, 15.6% of the volume] and composed of mostly iron and nickel that lies above Earth's solid inner core and below its mantle.[28] Its outer boundary lies 2890km (1,800miles) beneath Earth's surface. The transition between the inner core and outer core is located approximately 5150km (3,200miles) beneath Earth's surface. Earth's inner core is the innermost geologic layer of the planet Earth. It is primarily a solid ball with a radius of about, which is about 19% of Earth's radius [0.7% of volume] or 70% of the Moon's radius.[29] [30]

The inner core was discovered in 1936 by Inge Lehmann and is generally composed primarily of iron and some nickel. Since this layer is able to transmit shear waves (transverse seismic waves), it must be solid. Experimental evidence has at times been inconsistent with current crystal models of the core.[31] Other experimental studies show a discrepancy under high pressure: diamond anvil (static) studies at core pressures yield melting temperatures that are approximately 2000 K below those from shock laser (dynamic) studies.[32] [33] The laser studies create plasma,[34] and the results are suggestive that constraining inner core conditions will depend on whether the inner core is a solid or is a plasma with the density of a solid. This is an area of active research.

In early stages of Earth's formation about 4.6 billion years ago, melting would have caused denser substances to sink toward the center in a process called planetary differentiation (see also the iron catastrophe), while less-dense materials would have migrated to the crust. The core is thus believed to largely be composed of iron (80%), along with nickel and one or more light elements, whereas other dense elements, such as lead and uranium, either are too rare to be significant or tend to bind to lighter elements and thus remain in the crust (see felsic materials). Some have argued that the inner core may be in the form of a single iron crystal.[35] [36]

Under laboratory conditions a sample of iron–nickel alloy was subjected to the core-like pressure by gripping it in a vise between 2 diamond tips (diamond anvil cell), and then heating to approximately 4000 K. The sample was observed with x-rays, and strongly supported the theory that Earth's inner core was made of giant crystals running north to south.[37] [38]

The composition of Earth bears strong similarities to that of certain chondrite meteorites, and even to some elements in the outer portion of the Sun.[39] [40] Beginning as early as 1940, scientists, including Francis Birch, built geophysics upon the premise that Earth is like ordinary chondrites, the most common type of meteorite observed impacting Earth. This ignores the less abundant enstatite chondrites, which formed under extremely limited available oxygen, leading to certain normally oxyphile elements existing either partially or wholly in the alloy portion that corresponds to the core of Earth.

Dynamo theory suggests that convection in the outer core, combined with the Coriolis effect, gives rise to Earth's magnetic field. The solid inner core is too hot to hold a permanent magnetic field (see Curie temperature) but probably acts to stabilize the magnetic field generated by the liquid outer core. The average magnetic field in Earth's outer core is estimated to measure 2.5mT, 50 times stronger than the magnetic field at the surface.[41]

The magnetic field generated by core flow is essential to protect life from interplanetary radiation and prevent the atmosphere from dissipating in the solar wind. The rate of cooling by conduction and convection is uncertain,[42] but one estimate is that the core would not be expected to freeze up for approximately 91 billion years, which is well after the Sun is expected to expand, sterilize the surface of the planet, and then burn out.[43]

Seismology

See main article: Seismology. The layering of Earth has been inferred indirectly using the time of travel of refracted and reflected seismic waves created by earthquakes. The core does not allow shear waves to pass through it, while the speed of travel (seismic velocity) is different in other layers. The changes in seismic velocity between different layers causes refraction owing to Snell's law, like light bending as it passes through a prism. Likewise, reflections are caused by a large increase in seismic velocity and are similar to light reflecting from a mirror.

See also

Further reading

Notes and References

  1. Book: The Structure of Earth and Its Constituents . Princeton University Press . 4.
  2. ME = 5·9722×1024 kg ± 6×1020 kg. "2016 Selected Astronomical Constants " in
  3. Web site: Planetary Fact Sheet . 2 January 2009 . Lunar and Planetary Science . NASA . 24 March 2016 . https://web.archive.org/web/20160324033129/http://nssdc.gsfc.nasa.gov/planetary/factsheet/ . live .
  4. Encyclopedia: Earth's structure, global . Encyclopedia of solid earth geophysics . Springer Science & Business Media . Montagner . Jean-Paul . 2011 . Gupta . Harsh . 9789048187010.
  5. News: What are the layers of the Earth? . 21 August 2018 . 28 June 2019 . Mihai . Andrei . ZME Science . 12 May 2020 . https://web.archive.org/web/20200512013554/https://www.zmescience.com/other/science-abc/layers-earth-structure/ . live .
  6. News: Earth's Structure From the Crust to the Inner Core . 25 April 2017 . 28 June 2019 . Lisa . Chinn . Sciencing . Leaf Group Media . 30 July 2020 . https://web.archive.org/web/20200730091442/https://sciencing.com/earths-structure-crust-inner-core-16911.html . live .
  7. Book: An Introduction to Our Dynamic Planet . 2008 . . 978-0-521-49424-3 . Rogers . N. . 19 . 2022-08-08 . 2016-05-02 . https://web.archive.org/web/20160502212957/https://books.google.com/books?id=WA9ST5S_2v0C&pg=PA44 . live .
  8. Book: Glossary of geology. . 1997 . American Geological Institute . 0922152349 . Jackson . Julia A. . Fourth . Alexandria, Virginia . mafic.
  9. Britannica, The Editors of Encyclopaedia. "continental crust". Encyclopedia Britannica, 5 Sep. 2023, https://www.britannica.com/science/continental-crust. |access-date=12 October 2023 |url-status=live
  10. Book: Schmidt . Victor A. . Planet Earth and the New Geosciences . Harbert . William . 1998 . 978-0-7872-4296-1 . 3rd . 442 . The Living Machine: Plate Tectonics . Kendall/Hunt Publishing Company . 2008-01-28 . https://web.archive.org/web/20100124060304/http://geoinfo.amu.edu.pl/wpk/pe/a/harbbook/other/contents.html . 2010-01-24 . dead. Web site: Unit 3: The Living Machine: Plate Tectonics . dead . https://web.archive.org/web/20100328212854/http://geoinfo.amu.edu.pl/wpk/pe/a/harbbook/c_iii/chap03.html . 2010-03-28.
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