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Internal structure of Earth
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<h2 id="global-properties">Global properties</h2> <p class="note">Further information: <a href="/facts/Earth/HLLmDfj0">Earth § Physical characteristics</a></p> Chemical composition of the upper internal structure of <a href="/facts/Earth/HLLmDfj0">Earth</a><a class="footnote-ref" id="fnref:1" href="#fn:1"><sup>1</sup></a><table><tbody><tr><th>Chemical element</th><th><a href="/facts/Continental_crust/cGnK3oEr">Continental crust</a> (%)</th><th><a href="/facts/Upper_mantle/5I9jq18K">Upper mantle</a> (%)</th><th><a href="/facts/Pyrolite/FQmNU4M7">Pyrolite model</a> (%)</th><th>Chondrite model (1) (%)</th><th>Chondrite model (2) (%)</th></tr><tr><td><a href="/facts/Magnesium_oxide/0GfLn47t">MgO</a></td><td>4.4</td><td>36.6</td><td>38.1</td><td>26.3</td><td>38.1</td></tr><tr><td><a href="/facts/Aluminium_oxide/wXM9P6pI">Al2O3</a></td><td>15.8</td><td>4.6</td><td>4.6</td><td>2.7</td><td>3.9</td></tr><tr><td><a href="/facts/Silicon_dioxide/A3WILp6J">SiO2</a></td><td>59.1</td><td>45.4</td><td>45.1</td><td>29.8</td><td>43.2</td></tr><tr><td><a href="/facts/Calcium_oxide/Wh9C8l7j">CaO</a></td><td>6.4</td><td>3.7</td><td>3.1</td><td>2.6</td><td>3.9</td></tr><tr><td><a href="/facts/Iron(II)_oxide/H9V7S3MG">FeO</a></td><td>6.6</td><td>8.1</td><td>7.9</td><td>6.4</td><td>9.3</td></tr><tr><td>Other oxides</td><td>7.7</td><td>1.4</td><td>1.2</td><td>N/A</td><td>5.5</td></tr><tr><td><a href="/facts/Iron/QK1JYy8E">Fe</a></td><td>N/A</td><td>N/A</td><td>N/A</td><td>25.8</td><td>N/A</td></tr><tr><td><a href="/facts/Nickel/KwMCHYRP">Ni</a></td><td>N/A</td><td>N/A</td><td>N/A</td><td>1.7</td><td>N/A</td></tr><tr><td><a href="/facts/Silicon/cgWx0hdr">Si</a></td><td>N/A</td><td>N/A</td><td>N/A</td><td>3.5</td><td>N/A</td></tr></tbody></table><p> 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).<a class="footnote-ref" id="fnref:2" href="#fn:2"><sup>2</sup></a></p><p>Measurements of the force exerted by <a href="/facts/Earth%2527s_gravity/IXe9Bh8k">Earth's gravity</a> can be used to calculate its <a href="/facts/Mass/HHdc8XmF">mass</a>. Astronomers can also calculate <a href="/facts/Earth_mass/G74DaKFv">Earth's mass</a> by observing the motion of orbiting <a href="/facts/Satellite/PTX8c68t">satellites</a>. Earth's average <a href="/facts/Density/92p6hh9I">density</a> can be determined through gravimetric experiments, which have historically involved <a href="/facts/Pendulum/D2hQXwlI">pendulums</a>. The mass of Earth is about 6×1024 kg.<a class="footnote-ref" id="fnref:3" href="#fn:3"><sup>3</sup></a> The average density of Earth is 5.515 <a href="/facts/Gram_per_cubic_centimetre/qGLL4w7D">g/cm3</a>.<a class="footnote-ref" id="fnref:4" href="#fn:4"><sup>4</sup></a> </p><h2 id="layers">Layers</h2> <p>The structure of Earth can be defined in two ways: by mechanical properties such as <a href="/facts/Rheology/KexaBNCS">rheology</a>, or chemically. Mechanically, it can be divided into <a href="/facts/Lithosphere/1mqaxASd">lithosphere</a>, <a href="/facts/Asthenosphere/lXpE97oP">asthenosphere</a>, <a href="/facts/Mesosphere_(mantle)/KQQBHWp8">mesospheric mantle</a>, <a href="/facts/Earth%2527s_outer_core/1U5pw3La">outer core</a>, and the <a href="/facts/Earth%2527s_inner_core/M2qscVcY">inner core</a>. Chemically, Earth can be divided into the crust, upper mantle, lower mantle, outer core, and inner core.<a class="footnote-ref" id="fnref:5" href="#fn:5"><sup>5</sup></a> The geologic component layers of Earth are at increasing depths below the surface.<a class="footnote-ref" id="fnref:6" href="#fn:6"><sup>6</sup></a>: 146 </p> <h3>Crust and lithosphere</h3> <p class="note">Main articles: <a href="/facts/Earth%2527s_crust/VSy2u31r">Earth's crust</a> and <a href="/facts/Lithosphere/1mqaxASd">Lithosphere</a></p> <p>Earth's crust ranges from 5 to 70 kilometres (3.1–43.5 mi)<a class="footnote-ref" id="fnref:7" href="#fn:7"><sup>7</sup></a> in depth and is the outermost layer.<a class="footnote-ref" id="fnref:8" href="#fn:8"><sup>8</sup></a> The thin parts are the <a href="/facts/Oceanic_crust/0lGjI7jN">oceanic crust</a>, which underlies the ocean basins (5–10 km) and is <a href="/facts/Mafic/mVL7Ahuw">mafic</a>-rich<a class="footnote-ref" id="fnref:9" href="#fn:9"><sup>9</sup></a> (dense iron-magnesium <a href="/facts/Silicate_mineral/WclrQW2I">silicate mineral</a> or <a href="/facts/Igneous_rock/xeMJhUah">igneous rock</a>).<a class="footnote-ref" id="fnref:10" href="#fn:10"><sup>10</sup></a> The thicker crust is the <a href="/facts/Continental_crust/cGnK3oEr">continental crust</a>, which is less dense<a class="footnote-ref" id="fnref:11" href="#fn:11"><sup>11</sup></a> and is <a href="/facts/Felsic/0jpm1eSA">felsic</a>-rich (igneous rocks rich in elements that form <a href="/facts/Feldspar/DVvFnfA9">feldspar</a> and <a href="/facts/Quartz/4n86tE2G">quartz</a>).<a class="footnote-ref" id="fnref:12" href="#fn:12"><sup>12</sup></a> The rocks of the crust fall into two major categories – <a href="/facts/Sial/DupWmjRP">sial</a> (aluminium silicate) and <a href="/facts/Sima_(geology)/0n4Ytwsv">sima</a> (magnesium silicate).<a class="footnote-ref" id="fnref:13" href="#fn:13"><sup>13</sup></a> It is estimated that sima starts about 11 km below the <a href="/facts/Conrad_discontinuity/g3qb3yM3">Conrad discontinuity</a>,<a class="footnote-ref" id="fnref:14" href="#fn:14"><sup>14</sup></a> though the discontinuity is not distinct and can be absent in some continental regions.<a class="footnote-ref" id="fnref:15" href="#fn:15"><sup>15</sup></a> </p><p>Earth's lithosphere consists of the crust and the uppermost <a href="/facts/Earth%2527s_mantle/l9DjRLcc">mantle</a>.<a class="footnote-ref" id="fnref:16" href="#fn:16"><sup>16</sup></a> The crust-mantle boundary occurs as two physically different phenomena. The <a href="/facts/Mohorovi%25C4%258Di%25C4%2587_discontinuity/1NBmpcKT">Mohorovičić discontinuity</a> is a distinct change of <a href="/facts/Seismic_wave/1JTeLfac">seismic wave</a> velocity. This is caused by a change in the rock's density<a class="footnote-ref" id="fnref:17" href="#fn:17"><sup>17</sup></a> – immediately above the Moho, the velocities of primary seismic waves (<a href="/facts/P_wave/dzv94RBr">P wave</a>) are consistent with those through <a href="/facts/Basalt/uhbwGPTb">basalt</a> (6.7–7.2 km/s), and below they are similar to those through <a href="/facts/Peridotite/4NRPpWxw">peridotite</a> or <a href="/facts/Dunite/W8ECQonU">dunite</a> (7.6–8.6 km/s).<a class="footnote-ref" id="fnref:18" href="#fn:18"><sup>18</sup></a> Second, in oceanic crust, there is a chemical discontinuity between <a href="/facts/Ultramafic/7qAapP1d">ultramafic</a> cumulates and tectonized <a href="/facts/Peridotite/4NRPpWxw">harzburgites</a>, which has been observed from deep parts of the oceanic crust that have been <a href="/facts/Obduction/5qSAGQhr">obducted</a> onto the continental crust and preserved as <a href="/facts/Ophiolites/vX9Kg940">ophiolite sequences</a>. </p><p>Many rocks making up Earth's crust formed less than 100 <a href="/facts/Million_years/DXcnXuAw">million years</a> ago; however, the oldest known mineral grains are about 4.4 <a href="/facts/Billion_years/KrcuDaHm">billion years</a> old, indicating that Earth has had a solid crust for at least 4.4 billion years.<a class="footnote-ref" id="fnref:19" href="#fn:19"><sup>19</sup></a> </p> <h3>Mantle</h3> <p class="note">Main article: <a href="/facts/Earth%2527s_mantle/l9DjRLcc">Earth's mantle</a></p> <p>Earth's mantle extends to a depth of 2,890 km (1,800 mi), making it the planet's thickest layer.<a class="footnote-ref" id="fnref:20" href="#fn:20"><sup>20</sup></a> [This is 45% of the 6,371 km (3,959 mi) radius, and 83.7% of the volume - 0.6% of the volume is the crust]. The mantle is divided into <a href="/facts/Upper_mantle/5I9jq18K">upper</a> and <a href="/facts/Lower_mantle/KQQBHWp8">lower mantle</a><a class="footnote-ref" id="fnref:21" href="#fn:21"><sup>21</sup></a> separated by a <a href="/facts/Transition_zone_(Earth)/ID58Q6W7">transition zone</a>.<a class="footnote-ref" id="fnref:22" href="#fn:22"><sup>22</sup></a> The lowest part of the mantle next to the <a href="/facts/Core-mantle_boundary/EWHuuEdT">core-mantle boundary</a> is known as the D″ (D-double-prime) layer.<a class="footnote-ref" id="fnref:23" href="#fn:23"><sup>23</sup></a> The <a href="/facts/Pressure/eyc37GRG">pressure</a> at the bottom of the mantle is ≈140 G<a href="/facts/Pascal_(unit)/Am1To2Qm">Pa</a> (1.4 M<a href="/facts/Atmosphere_(unit)/aTbYALII">atm</a>).<a class="footnote-ref" id="fnref:24" href="#fn:24"><sup>24</sup></a> The mantle is composed of <a href="/facts/Silicate/7NdthSRM">silicate</a> rocks richer in iron and magnesium than the overlying crust.<a class="footnote-ref" id="fnref:25" href="#fn:25"><sup>25</sup></a> Although solid, the mantle's extremely hot silicate material can <a href="/facts/Ductility/SBJsahEk">flow</a> over very long timescales.<a class="footnote-ref" id="fnref:26" href="#fn:26"><sup>26</sup></a> <a href="/facts/Convection/E8vsCPhu">Convection</a> of the mantle propels the <a href="/facts/Plate_tectonics/RtRG5lY4">motion of the tectonic plates</a> in the crust. The <a href="/facts/Earth%2527s_internal_heat_budget/WhygNFuJ">source of heat</a> that drives this motion is the decay of <a href="/facts/Radioactive_isotopes/5WpCfbdq">radioactive isotopes</a> in Earth's crust and mantle combined with the initial heat from the planet's formation<a class="footnote-ref" id="fnref:27" href="#fn:27"><sup>27</sup></a> (from the <a href="/facts/Potential_energy/I03KLbmn">potential energy</a> released by collapsing a large amount of matter into a <a href="/facts/Gravity_well/x4ITT4gY">gravity well</a>, and the <a href="/facts/Kinetic_energy/aJRxUd4p">kinetic energy</a> of accreted matter). </p><p>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 <a href="/facts/Pascal_second/QLVfrdCz">pascal-second</a>, increasing with depth.<a class="footnote-ref" id="fnref:28" href="#fn:28"><sup>28</sup></a> In comparison, the viscosity of water at 300 K (27 °C; 80 °F) is 0.89 millipascal-second <a class="footnote-ref" id="fnref:29" href="#fn:29"><sup>29</sup></a> and <a href="/facts/Pitch_(resin)/GpdKnQMa">pitch</a> is (2.3 ± 0.5) × 108 pascal-second.<a class="footnote-ref" id="fnref:30" href="#fn:30"><sup>30</sup></a> </p> <h3>Core</h3> <p class="note">Main articles: <a href="/facts/Earth%2527s_inner_core/M2qscVcY">Earth's inner core</a> and <a href="/facts/Earth%2527s_outer_core/1U5pw3La">Earth's outer core</a></p> <p>Earth's outer core is a fluid layer about 2,260 km (1,400 mi) 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 <a href="/facts/Iron/QK1JYy8E">iron</a> and <a href="/facts/Nickel/KwMCHYRP">nickel</a> that lies above Earth's solid <a href="/facts/Earth%2527s_inner_core/M2qscVcY">inner core</a> and below its <a href="/facts/Mantle_(geology)/RpDdtjCr">mantle</a>.<a class="footnote-ref" id="fnref:31" href="#fn:31"><sup>31</sup></a> Its outer boundary lies 2,890 km (1,800 mi) beneath Earth's surface. The transition between the inner core and outer core is located approximately 5,150 km (3,200 mi) beneath Earth's surface. Earth's inner core is the innermost <a href="/facts/Structure_of_the_Earth/678dYXU7">geologic layer</a> of the planet <a href="/facts/Earth/HLLmDfj0">Earth</a>. It is primarily a solid ball with a radius of about 1,220 km (760 mi), which is about 19% of <a href="/facts/Earth_radius/PVsf0g2I">Earth's radius</a> [0.7% of volume] or 70% of the <a href="/facts/Moon/zKHqEMPb">Moon</a>'s radius.<a class="footnote-ref" id="fnref:32" href="#fn:32"><sup>32</sup></a><a class="footnote-ref" id="fnref:33" href="#fn:33"><sup>33</sup></a> </p><p>The inner core was discovered in 1936 by <a href="/facts/Inge_Lehmann/hx70xaw4">Inge Lehmann</a> and is 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.<a class="footnote-ref" id="fnref:34" href="#fn:34"><sup>34</sup></a> 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.<a class="footnote-ref" id="fnref:35" href="#fn:35"><sup>35</sup></a><a class="footnote-ref" id="fnref:36" href="#fn:36"><sup>36</sup></a> The laser studies create plasma,<a class="footnote-ref" id="fnref:37" href="#fn:37"><sup>37</sup></a> 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. </p><p>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 <a href="/facts/Planetary_differentiation/fvjC1107">planetary differentiation</a> (see also the <a href="/facts/Iron_catastrophe/UmxnxFcg">iron catastrophe</a>), while less-dense materials would have migrated to the <a href="/facts/Crust_(geology)/FYG1kP4F">crust</a>. The core is thus believed to largely be composed of iron (80%), along with <a href="/facts/Nickel/KwMCHYRP">nickel</a> and one or more light elements, whereas other dense elements, such as <a href="/facts/Lead/EYljasJN">lead</a> and <a href="/facts/Uranium/n2sGWBzU">uranium</a>, either are too rare to be significant or tend to bind to lighter elements and thus remain in the crust (see <a href="/facts/Felsic/0jpm1eSA">felsic materials</a>). Some have argued that the inner core may be in the form of a single iron <a href="/facts/Crystal/e2R2mk3E">crystal</a>.<a class="footnote-ref" id="fnref:38" href="#fn:38"><sup>38</sup></a><a class="footnote-ref" id="fnref:39" href="#fn:39"><sup>39</sup></a> </p><p>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 (<a href="/facts/Diamond_anvil_cell/vpsaLRrr">diamond anvil cell</a>), 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.<a class="footnote-ref" id="fnref:40" href="#fn:40"><sup>40</sup></a><a class="footnote-ref" id="fnref:41" href="#fn:41"><sup>41</sup></a> </p><p>The composition of Earth bears strong similarities to that of certain <a href="/facts/Chondrite/mbzbGm5A">chondrite</a> meteorites, and even to some elements in the outer portion of the Sun.<a class="footnote-ref" id="fnref:42" href="#fn:42"><sup>42</sup></a><a class="footnote-ref" id="fnref:43" href="#fn:43"><sup>43</sup></a> Beginning as early as 1940, scientists, including <a href="/facts/Francis_Birch_(geophysicist)/YB9zyluj">Francis Birch</a>, 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 <a href="/facts/Enstatite/PlsXlhLq">enstatite</a> 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. </p><p><a href="/facts/Dynamo_theory/CVMamd1s">Dynamo theory</a> suggests that convection in the outer core, combined with the <a href="/facts/Coriolis_effect/SqCyUY6d">Coriolis effect</a>, gives rise to <a href="/facts/Earth%2527s_magnetic_field/73G36wmx">Earth's magnetic field</a>. The solid inner core is too hot to hold a permanent magnetic field (see <a href="/facts/Curie_temperature/ygotSuMg">Curie temperature</a>) 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 2.5 milliteslas (25 gauss), 50 times stronger than the magnetic field at the surface.<a class="footnote-ref" id="fnref:44" href="#fn:44"><sup>44</sup></a> </p><p>The magnetic field generated by core flow is essential to protect life from interplanetary radiation and prevent the atmosphere from dissipating in the <a href="/facts/Solar_wind/BvuB3dT8">solar wind</a>. The rate of cooling by conduction and convection is uncertain,<a class="footnote-ref" id="fnref:45" href="#fn:45"><sup>45</sup></a> 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.<a class="footnote-ref" id="fnref:46" href="#fn:46"><sup>46</sup></a>[<i>better source needed</i>] </p> <h2 id="seismology">Seismology</h2> <p class="note">Main article: <a href="/facts/Seismology/Lony1LYX">Seismology</a></p> <p>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 (<a href="/facts/Seismic_velocity/1JTeLfac">seismic velocity</a>) is different in other layers. The changes in seismic velocity between different layers causes refraction owing to <a href="/facts/Snell%2527s_law/cE0rhDXd">Snell's law</a>, 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. </p> <h2 id="see-also">See also</h2> <ul><li><a href="/facts/Hollow_Earth/jNdSySBK">Hollow Earth</a></li> <li><a href="/facts/Geological_history_of_Earth/Jx7ClmF4">Geological history of Earth</a></li> <li><a href="/facts/Large_low-shear-velocity_provinces/xfcluSMY">Large low-shear-velocity provinces</a></li> <li><a href="/facts/Lehmann_discontinuity/4SvssIMk">Lehmann discontinuity</a></li> <li><a href="/facts/Rain-out_model/aKVTQNv5">Rain-out model</a></li> <li><a href="/facts/Seismic_tomography/xlRG9zac">Seismic tomography</a> – technique for imaging the subsurface of Earth using seismic waves</li> <li><a href="/facts/Travel_to_the_Earth%2527s_center/njeFGe3z">Travel to the Earth's center</a></li> <li><a href="/facts/Solid_earth/9cTx04Rb">Solid earth</a></li></ul> <h2 id="further-reading">Further reading</h2> <ul><li>Drollette, Daniel (October 1996). "A Spinning Crystal Ball". <i>Scientific American</i>. 275 (4): 28–33. <a href="/facts/Bibcode_(identifier)/9HtdQSGB">Bibcode</a>:<a href="https://ui.adsabs.harvard.edu/abs/1996SciAm.275d..28D">1996SciAm.275d..28D</a>. <a href="/facts/Doi_(identifier)/muM9Etpq">doi</a>:<a href="https://doi.org/10.1038%2Fscientificamerican1096-28">10.1038/scientificamerican1096-28</a>.</li> <li>Kruglinski, Susan (June 2007). <a href="http://discovermagazine.com/2007/jun/journey-to-the-center-of-the-earth">"Journey to the Center of the Earth"</a>. <i>Discover</i>. <a href="https://web.archive.org/web/20160526021214/http://discovermagazine.com/2007/jun/journey-to-the-center-of-the-earth">Archived</a> from the original on 26 May 2016. Retrieved 9 July 2016.</li> <li>Lehmann, I (1936). "Inner Earth". <i>Bur. Cent. Seismol. Int</i>. 14: 3–31.</li> <li>Wegener, Alfred (1966). <a href="https://archive.org/details/originsofcontine0000unse"><i>The origin of continents and oceans</i></a>. New York: Dover Publications. <a href="/facts/ISBN_(identifier)/15AdSPa9">ISBN</a> 978-0-486-61708-4.</li></ul> <h2 id="external-links">External links</h2> <ul><li> Media related to Structure of the Earth at Wikimedia Commons</li></ul> <h2 id="references">References</h2> <ol> <li id="fn:1"><p>The Structure of Earth and Its Constituents (PDF). Princeton University Press. p. 4. <a href="http://assets.press.princeton.edu/chapters/s7559.pdf" target="_blank">http://assets.press.princeton.edu/chapters/s7559.pdf</a> <a href="#fnref:1" class="footnote-back-ref">↩</a></p></li> <li id="fn:2"><p>The Structure of Earth and Its Constituents (PDF). Princeton University Press. p. 4. <a href="http://assets.press.princeton.edu/chapters/s7559.pdf" target="_blank">http://assets.press.princeton.edu/chapters/s7559.pdf</a> <a href="#fnref:2" class="footnote-back-ref">↩</a></p></li> <li id="fn:3"><p>ME = 5·9722×1024 kg ± 6×1020 kg. "2016 Selected Astronomical Constants Archived 2016-02-15 at the Wayback Machine" in The Astronomical Almanac Online (PDF), USNO–UKHO, archived from the original on 2016-12-24, retrieved 2016-02-18 <a href="http://asa.usno.navy.mil/static/files/2016/Astronomical_Constants_2016.pdf" target="_blank">http://asa.usno.navy.mil/static/files/2016/Astronomical_Constants_2016.pdf</a> <a href="#fnref:3" class="footnote-back-ref">↩</a></p></li> <li id="fn:4"><p>"Planetary Fact Sheet". Lunar and Planetary Science. NASA. Archived from the original on 24 March 2016. Retrieved 2 January 2009. <a href="https://nssdc.gsfc.nasa.gov/planetary/factsheet/" target="_blank">https://nssdc.gsfc.nasa.gov/planetary/factsheet/</a> <a href="#fnref:4" class="footnote-back-ref">↩</a></p></li> <li id="fn:5"><p>Montagner, Jean-Paul (2011). "Earth's structure, global". In Gupta, Harsh (ed.). Encyclopedia of solid earth geophysics. Springer Science & Business Media. 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