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Mid-ocean ridge
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<h2 id="global-system">Global system</h2> <p>Most mid-ocean ridges of the world are connected and form <i>the</i> Ocean Ridge, a global mid-oceanic ridge system that is part of every <a href="/facts/Ocean/8W8lYgjD">ocean</a>, making it the <a href="/facts/List_of_mountain_ranges/cmwkhCyd">longest</a> <a href="/facts/Mountain_range/L7vxtr7A">mountain range</a> in the world. The continuous mountain range is 65,000 km (40,400 mi) long (several times longer than the <a href="/facts/Andes/a4wlgG3e">Andes</a>, the longest continental mountain range), and the total length of the oceanic ridge system is 80,000 km (49,700 mi) long.<a class="footnote-ref" id="fnref:1" href="#fn:1"><sup>1</sup></a> </p> <h2 id="description">Description</h2> <h3>Morphology</h3> <p class="note">See also: <a href="/facts/Seafloor_spreading/2t2oCbTp">Seafloor spreading § Seafloor global topography: cooling models</a>, and <a href="/facts/Seafloor_depth_versus_age/atvaPcbH">Seafloor depth versus age</a></p><p>At the <a href="/facts/Spreading_center/wYdgdSW3">spreading center</a> on a mid-ocean ridge, the depth of the seafloor is approximately 2,600 meters (8,500 ft).<a class="footnote-ref" id="fnref:2" href="#fn:2"><sup>2</sup></a><a class="footnote-ref" id="fnref:3" href="#fn:3"><sup>3</sup></a> On the ridge flanks, the depth of the seafloor (or the height of a location on a mid-ocean ridge above a base-level) is correlated with its age (age of the <a href="/facts/Lithosphere/1mqaxASd">lithosphere</a> where depth is measured). The <a href="/facts/Seafloor_depth_versus_age/atvaPcbH">depth-age relation</a> can be modeled by the cooling of a lithosphere plate<a class="footnote-ref" id="fnref:4" href="#fn:4"><sup>4</sup></a><a class="footnote-ref" id="fnref:5" href="#fn:5"><sup>5</sup></a> or <a href="/facts/Seafloor_spreading/2t2oCbTp">mantle half-space.</a><a class="footnote-ref" id="fnref:6" href="#fn:6"><sup>6</sup></a> A good approximation is that the depth of the seafloor at a location on a spreading mid-ocean ridge is proportional to the square root of the age of the seafloor.<a class="footnote-ref" id="fnref:7" href="#fn:7"><sup>7</sup></a> The overall shape of ridges results from <a href="/facts/Wallace_Pratt/MCmMfGcS">Pratt</a> <a href="/facts/Isostasy/GaRMFQNP">isostasy</a>: close to the ridge axis, there is a hot, low-density mantle supporting the oceanic crust. As the oceanic plate cools, away from the ridge axis, the oceanic mantle <a href="/facts/Lithosphere/1mqaxASd">lithosphere</a> (the colder, denser part of the mantle that, together with the crust, comprises the oceanic plates) thickens, and the density increases. Thus older seafloor is underlain by denser material and is deeper.<a class="footnote-ref" id="fnref:8" href="#fn:8"><sup>8</sup></a><a class="footnote-ref" id="fnref:9" href="#fn:9"><sup>9</sup></a> </p><p><i>Spreading rate</i> is the rate at which an ocean basin widens due to seafloor spreading. Rates can be computed by mapping marine magnetic anomalies that span mid-ocean ridges. As crystallized basalt extruded at a ridge axis cools below <a href="/facts/Curie_point/ygotSuMg">Curie points</a> of appropriate iron-titanium oxides, magnetic field directions parallel to the Earth's magnetic field are recorded in those oxides. The orientations of the field preserved in the oceanic crust comprise a record of directions of the <a href="/facts/Earth%2527s_magnetic_field/73G36wmx">Earth's magnetic field</a> with time. Because the field has reversed directions at known intervals throughout its history, the pattern of <a href="/facts/Geomagnetic_reversals/dsINRz5g">geomagnetic reversals</a> in the ocean crust can be used as an indicator of age; given the crustal age and distance from the ridge axis, spreading rates can be calculated.<a class="footnote-ref" id="fnref:10" href="#fn:10"><sup>10</sup></a><a class="footnote-ref" id="fnref:11" href="#fn:11"><sup>11</sup></a><a class="footnote-ref" id="fnref:12" href="#fn:12"><sup>12</sup></a><a class="footnote-ref" id="fnref:13" href="#fn:13"><sup>13</sup></a> </p><p>Spreading rates range from approximately 10–200 mm/yr.<a class="footnote-ref" id="fnref:14" href="#fn:14"><sup>14</sup></a><a class="footnote-ref" id="fnref:15" href="#fn:15"><sup>15</sup></a> Slow-spreading ridges such as the Mid-Atlantic Ridge have spread much less far (showing a steeper profile) than faster ridges such as the <a href="/facts/East_Pacific_Rise/mYrxownC">East Pacific Rise</a> (gentle profile) for the same amount of time and cooling and consequent bathymetric deepening.<a class="footnote-ref" id="fnref:16" href="#fn:16"><sup>16</sup></a> Slow-spreading ridges (less than 40 mm/yr) generally have large <a href="/facts/Rift_valley/UFkcaPew">rift valleys</a>, sometimes as wide as 10–20 km (6.2–12.4 mi), and very rugged terrain at the ridge crest that can have <a href="/facts/Terrain/r2lduLeI">relief</a> of up to 1,000 m (3,300 ft).<a class="footnote-ref" id="fnref:17" href="#fn:17"><sup>17</sup></a><a class="footnote-ref" id="fnref:18" href="#fn:18"><sup>18</sup></a><a class="footnote-ref" id="fnref:19" href="#fn:19"><sup>19</sup></a><a class="footnote-ref" id="fnref:20" href="#fn:20"><sup>20</sup></a> By contrast, fast-spreading ridges (greater than 90 mm/yr) such as the East Pacific Rise lack rift valleys. The spreading rate of the <a href="/facts/North_Atlantic_Ocean/EI4uChIb">North Atlantic Ocean</a> is ~ 25 mm/yr, while in the <a href="/facts/Pacific/bdxgXRVM">Pacific</a> region, it is 80–145 mm/yr.<a class="footnote-ref" id="fnref:21" href="#fn:21"><sup>21</sup></a> The highest known rate is over 200 mm/yr in the <a href="/facts/Miocene_Era/cBRRzq4g">Miocene</a> on the East Pacific Rise.<a class="footnote-ref" id="fnref:22" href="#fn:22"><sup>22</sup></a> Ridges that spread at rates <20 mm/yr are referred to as ultraslow spreading ridges<a class="footnote-ref" id="fnref:23" href="#fn:23"><sup>23</sup></a><a class="footnote-ref" id="fnref:24" href="#fn:24"><sup>24</sup></a> (e.g., the <a href="/facts/Gakkel_Ridge/fpl7wvY3">Gakkel Ridge</a> in the <a href="/facts/Arctic_Ocean/l6HS3QyV">Arctic Ocean</a> and the <a href="/facts/Southwest_Indian_Ridge/FIoer8fR">Southwest Indian Ridge</a>). </p><p>The spreading center or axis commonly connects to a <a href="/facts/Transform_fault/3VyTyvrE">transform fault</a> oriented at right angles to the axis. The flanks of mid-ocean ridges are in many places marked by the inactive scars of transform faults called <a href="/facts/Fracture_zone/7HhzWpKR">fracture zones</a>. At faster spreading rates the axes often display <a href="/facts/Overlapping_spreading_centers/bGxuuovf">overlapping spreading centers</a> that lack connecting transform faults.<a class="footnote-ref" id="fnref:25" href="#fn:25"><sup>25</sup></a><a class="footnote-ref" id="fnref:26" href="#fn:26"><sup>26</sup></a> The depth of the axis changes in a systematic way with shallower depths between offsets such as transform faults and overlapping spreading centers dividing the axis into segments. One hypothesis for different along-axis depths is variations in magma supply to the spreading center.<a class="footnote-ref" id="fnref:27" href="#fn:27"><sup>27</sup></a> Ultra-slow spreading ridges form both magmatic and amagmatic (currently lack volcanic activity) ridge segments without transform faults.<a class="footnote-ref" id="fnref:28" href="#fn:28"><sup>28</sup></a> </p> <h3>Volcanism</h3> <p>Mid-ocean ridges exhibit active <a href="/facts/Volcanism/0s6p1eFJ">volcanism</a> and <a href="/facts/Seismicity/pQTRsIKN">seismicity</a>.<a class="footnote-ref" id="fnref:29" href="#fn:29"><sup>29</sup></a> The oceanic crust is in a constant state of 'renewal' at the mid-ocean ridges by the processes of seafloor spreading and plate tectonics. New magma steadily emerges onto the ocean floor and intrudes into the existing <a href="/facts/Oceanic_crust/0lGjI7jN">ocean crust</a> at and near rifts along the ridge axes. The rocks making up the crust below the seafloor are youngest along the axis of the ridge and age with increasing distance from that axis. New magma of basalt composition emerges at and near the axis because of <a href="/facts/Igneous_rock/xeMJhUah">decompression melting</a> in the underlying <a href="/facts/Earth%2527s_mantle/l9DjRLcc">Earth's mantle</a>.<a class="footnote-ref" id="fnref:30" href="#fn:30"><sup>30</sup></a> The <a href="/facts/Isentropic/BYMe7V5P">isentropic</a> upwelling solid mantle material exceeds the <a href="/facts/Solidus_(chemistry)/BLbHPYH8">solidus</a> temperature and melts. </p><p>The crystallized magma forms a new crust of <a href="/facts/Basalt/uhbwGPTb">basalt</a> known as MORB for mid-ocean ridge basalt, and <a href="/facts/Gabbro/79gTqpyg">gabbro</a> below it in the <a href="/facts/Lower_oceanic_crust/MXCHRgll">lower oceanic crust</a>.<a class="footnote-ref" id="fnref:31" href="#fn:31"><sup>31</sup></a> Mid-ocean ridge basalt is a <a href="/facts/Tholeiitic_basalt/e93b58Nj">tholeiitic basalt</a> and is low in <a href="/facts/Incompatible_element/RqEMlFUu">incompatible elements</a>.<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> <a href="/facts/Hydrothermal_vent/0xPqNUkY">Hydrothermal vents</a> fueled by magmatic and volcanic heat are a common feature at oceanic spreading centers.<a class="footnote-ref" id="fnref:34" href="#fn:34"><sup>34</sup></a><a class="footnote-ref" id="fnref:35" href="#fn:35"><sup>35</sup></a> A feature of the elevated ridges is their relatively high heat flow values, of about 1–10 μcal/cm2s,<a class="footnote-ref" id="fnref:36" href="#fn:36"><sup>36</sup></a> or roughly 0.04–0.4 W/m2. </p><p>Most crust in the ocean basins is less than 200 million years old,<a class="footnote-ref" id="fnref:37" href="#fn:37"><sup>37</sup></a><a class="footnote-ref" id="fnref:38" href="#fn:38"><sup>38</sup></a> which is much younger than the 4.54 billion year <a href="/facts/Age_of_Earth/MxNh2Q11">age of Earth</a>. This fact reflects the process of lithosphere recycling into the Earth's mantle during <a href="/facts/Subduction/rkasNdTo">subduction</a>. As the oceanic crust and lithosphere moves away from the ridge axis, the <a href="/facts/Peridotite/4NRPpWxw">peridotite</a> in the underlying mantle lithosphere cools and becomes more rigid. The crust and the relatively rigid peridotite below it make up the <a href="/facts/Oceanic_lithosphere/1mqaxASd">oceanic lithosphere</a>, which sits above the less rigid and viscous <a href="/facts/Asthenosphere/lXpE97oP">asthenosphere</a>.<a class="footnote-ref" id="fnref:39" href="#fn:39"><sup>39</sup></a> </p> <h2 id="driving-mechanisms">Driving mechanisms</h2> <p class="note">Further information: <a href="/facts/Plate_tectonics/RtRG5lY4">Plate tectonics</a></p> <p>The oceanic lithosphere is formed at an oceanic ridge, while the lithosphere is subducted back into the asthenosphere at ocean <a href="/facts/Oceanic_trench/sbp2PRk4">trenches</a>. Two processes, <a href="/facts/Ridge-push/uF6Y3FwA">ridge-push</a> and <a href="/facts/Slab_pull/ljhNsVHo">slab pull</a>, are thought to be responsible for spreading at mid-ocean ridges.<a class="footnote-ref" id="fnref:40" href="#fn:40"><sup>40</sup></a> Ridge push refers to the gravitational sliding of the ocean plate that is raised above the hotter asthenosphere, thus creating a body force causing sliding of the plate downslope.<a class="footnote-ref" id="fnref:41" href="#fn:41"><sup>41</sup></a> In slab pull the weight of a tectonic plate being subducted (pulled) below an overlying plate at a subduction zone drags the rest of the plate along behind it. The slab pull mechanism is considered to be contributing more than the ridge push.<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> </p><p>A process previously proposed to contribute to plate motion and the formation of new oceanic crust at mid-ocean ridges is the "mantle conveyor" due to deep <a href="/facts/Mantle_convection/YV2IE8KQ">convection</a> (see image).<a class="footnote-ref" id="fnref:44" href="#fn:44"><sup>44</sup></a><a class="footnote-ref" id="fnref:45" href="#fn:45"><sup>45</sup></a> However, some studies have shown that the <a href="/facts/Upper_mantle_(Earth)/5I9jq18K">upper mantle</a> (<a href="/facts/Asthenosphere/lXpE97oP">asthenosphere</a>) is too plastic (flexible) to generate enough <a href="/facts/Friction/d0108Rpu">friction</a> to pull the tectonic plate along.<a class="footnote-ref" id="fnref:46" href="#fn:46"><sup>46</sup></a><a class="footnote-ref" id="fnref:47" href="#fn:47"><sup>47</sup></a> Moreover, mantle upwelling that causes magma to form beneath the ocean ridges appears to involve only its upper 400 km (250 mi), as deduced from <a href="/facts/Seismic_tomography/xlRG9zac">seismic tomography</a> and observations of the seismic discontinuity in the upper mantle at about 400 km (250 mi). On the other hand, some of the world's largest tectonic plates such as the <a href="/facts/North_American_plate/2H28Etp0">North American plate</a> and <a href="/facts/South_American_plate/fpp0v8nK">South American plate</a> are in motion, yet only are being subducted in restricted locations such as the <a href="/facts/Lesser_Antilles/e3kYAgTY">Lesser Antilles Arc</a> and <a href="/facts/Scotia_Arc/AsehDNLy">Scotia Arc</a>, pointing to action by the ridge push body force on these plates. Computer modeling of the plates and mantle motions suggest that plate motion and mantle convection are not connected, and the main plate driving force is slab pull.<a class="footnote-ref" id="fnref:48" href="#fn:48"><sup>48</sup></a> </p> <h2 id="impact-on-global-sea-level">Impact on global sea level</h2> <p>Increased rates of <a href="/facts/Seafloor_spreading/2t2oCbTp">seafloor spreading</a> (i.e. the rate of expansion of the mid-ocean ridge) have caused the global (<a href="/facts/Eustatic_sea_level/wpYwdlHI">eustatic</a>) sea level to rise over very long timescales (millions of years).<a class="footnote-ref" id="fnref:49" href="#fn:49"><sup>49</sup></a><a class="footnote-ref" id="fnref:50" href="#fn:50"><sup>50</sup></a> Increased seafloor spreading means that the mid-ocean ridge will then expand and form a broader ridge with decreased average depth, taking up more space in the ocean basin. This displaces the overlying ocean and causes sea levels to rise.<a class="footnote-ref" id="fnref:51" href="#fn:51"><sup>51</sup></a> </p><p><a href="/facts/Sea_level_rise/Pb5MGJxb">Sealevel change</a> can be attributed to other factors (<a href="/facts/Thermal_expansion/BP2vjX0N">thermal expansion</a>, ice melting, and <a href="/facts/Mantle_convection/YV2IE8KQ">mantle convection</a> creating <a href="/facts/Dynamic_topography/WLVWG18d">dynamic topography</a><a class="footnote-ref" id="fnref:52" href="#fn:52"><sup>52</sup></a>). Over very long timescales, however, it is the result of changes in the volume of the ocean basins which are, in turn, affected by rates of seafloor spreading along the mid-ocean ridges.<a class="footnote-ref" id="fnref:53" href="#fn:53"><sup>53</sup></a> </p><p>The 100 to 170 meters higher sea level of the <a href="/facts/Cretaceous/nwKtFtKx">Cretaceous Period</a> (144–65 Ma) is partly attributed to plate tectonics because thermal expansion and the absence of ice sheets only account for some of the extra sea level.<a class="footnote-ref" id="fnref:54" href="#fn:54"><sup>54</sup></a> </p> <h2 id="impact-on-seawater-chemistry-and-carbonate-deposition">Impact on seawater chemistry and carbonate deposition</h2> <p class="note">Main article: <a href="/facts/Ocean_chemistry/AKV3gkUk">Ocean chemistry</a></p> <p>Seafloor spreading on mid-ocean ridges is a global scale <a href="/facts/Ion_exchange/C2DPoGqg">ion-exchange</a> system.<a class="footnote-ref" id="fnref:55" href="#fn:55"><sup>55</sup></a> Hydrothermal vents at spreading centers introduce various amounts of <a href="/facts/Iron/QK1JYy8E">iron</a>, <a href="/facts/Sulfur/IK0amTfM">sulfur</a>, <a href="/facts/Manganese/j9ELd1TL">manganese</a>, <a href="/facts/Silicon/cgWx0hdr">silicon</a>, and other elements into the ocean, some of which are recycled into the ocean crust. <a href="/facts/Helium-3/SmPC5oT3">Helium-3</a>, an isotope that accompanies volcanism from the mantle, is emitted by hydrothermal vents and can be detected in plumes within the ocean.<a class="footnote-ref" id="fnref:56" href="#fn:56"><sup>56</sup></a> </p><p>Fast spreading rates will expand the mid-ocean ridge causing basalt reactions with seawater to happen more rapidly. The magnesium/calcium ratio will be lower because more magnesium ions are being removed from seawater and consumed by the rock, and more calcium ions are being removed from the rock and released into seawater. Hydrothermal activity at the ridge crest is efficient in removing magnesium.<a class="footnote-ref" id="fnref:57" href="#fn:57"><sup>57</sup></a> A lower Mg/Ca ratio favors the precipitation of low-Mg <a href="/facts/Calcite/gKMHYQJo">calcite</a> <a href="/facts/Polymorphism_(materials_science)/bu2tqsB9">polymorphs</a> of <a href="/facts/Calcium_carbonate/UQ1wLFna">calcium carbonate</a> (<a href="/facts/Calcite_sea/fe3tY6Cs">calcite seas</a>).<a class="footnote-ref" id="fnref:58" href="#fn:58"><sup>58</sup></a><a class="footnote-ref" id="fnref:59" href="#fn:59"><sup>59</sup></a> </p><p>Slow spreading at mid-ocean ridges has the opposite effect and will result in a higher Mg/Ca ratio favoring the precipitation of <a href="/facts/Aragonite/QGcD3SLs">aragonite</a> and high-Mg calcite polymorphs of <a href="/facts/Calcium_carbonate/UQ1wLFna">calcium carbonate</a> (<a href="/facts/Aragonite_sea/MDc8IWSL">aragonite seas</a>).<a class="footnote-ref" id="fnref:60" href="#fn:60"><sup>60</sup></a> </p><p>Experiments show that most modern high-Mg calcite organisms would have been low-Mg calcite in past calcite seas,<a class="footnote-ref" id="fnref:61" href="#fn:61"><sup>61</sup></a> meaning that the Mg/Ca ratio in an organism's skeleton varies with the Mg/Ca ratio of the seawater in which it was grown. </p><p>The mineralogy of reef-building and sediment-producing organisms is thus regulated by chemical reactions occurring along the mid-ocean ridge, the rate of which is controlled by the rate of sea-floor spreading.<a class="footnote-ref" id="fnref:62" href="#fn:62"><sup>62</sup></a><a class="footnote-ref" id="fnref:63" href="#fn:63"><sup>63</sup></a> </p> <h2 id="history">History</h2> <h3>Discovery</h3> <p class="note">Main article: <a href="/facts/Plate_tectonics/RtRG5lY4">Plate tectonics § Development of the theory</a></p> <p>The first indications that a ridge bisects the <a href="/facts/Atlantic_Ocean/EI4uChIb">Atlantic Ocean</a> basin came from the results of the British <a href="/facts/Challenger_expedition/9Em9JqWY">Challenger expedition</a> in the nineteenth century.<a class="footnote-ref" id="fnref:64" href="#fn:64"><sup>64</sup></a> Soundings from lines dropped to the seafloor were analyzed by oceanographers <a href="/facts/Matthew_Fontaine_Maury/6BP3PQAC">Matthew Fontaine Maury</a> and <a href="/facts/Charles_Wyville_Thomson/nVmqmEF6">Charles Wyville Thomson</a> and revealed a prominent rise in the seafloor that ran down the Atlantic basin from north to south. <a href="/facts/Sonar/0Rg2G40e">Sonar</a> <a href="/facts/Echo_sounding/El22TcqE">echo sounders</a> confirmed this in the early twentieth century.<a class="footnote-ref" id="fnref:65" href="#fn:65"><sup>65</sup></a> </p><p>It was not until after <a href="/facts/World_War_II/2efV5L1U">World War II</a>, when the ocean floor was surveyed in more detail, that the full extent of mid-ocean ridges became known. The <i><a href="/facts/Research_Vessel_Vema/2U1uFeTo">Vema</a></i>, a ship of the <a href="/facts/Lamont%25E2%2580%2593Doherty_Earth_Observatory/b6U0PoCl">Lamont–Doherty Earth Observatory</a> of <a href="/facts/Columbia_University/Hlf1gw53">Columbia University</a>, traversed the Atlantic Ocean, recording echo sounder data on the depth of the ocean floor. A team led by <a href="/facts/Marie_Tharp/Rq5kE4pD">Marie Tharp</a> and <a href="/facts/Bruce_C._Heezen/2jhfAF6j">Bruce Heezen</a> concluded that there was an enormous mountain chain with a rift valley at its crest, running up the middle of the Atlantic Ocean. Scientists named it the 'Mid-Atlantic Ridge'. Other research showed that the ridge crest was seismically active<a class="footnote-ref" id="fnref:66" href="#fn:66"><sup>66</sup></a> and fresh lavas were found in the rift valley.<a class="footnote-ref" id="fnref:67" href="#fn:67"><sup>67</sup></a> Also, crustal heat flow was higher here than elsewhere in the Atlantic Ocean basin.<a class="footnote-ref" id="fnref:68" href="#fn:68"><sup>68</sup></a> </p><p>At first, the ridge was thought to be a feature specific to the Atlantic Ocean. However, as surveys of the ocean floor continued around the world, it was discovered that every ocean contains parts of the mid-ocean ridge system. The <a href="/facts/German_Meteor_expedition/P4nqRGA5">German Meteor expedition</a> traced the mid-ocean ridge from the <a href="/facts/South_Atlantic/EI4uChIb">South Atlantic</a> into the <a href="/facts/Indian_Ocean/Kv0crwKG">Indian Ocean</a> early in the twentieth century. Although the first-discovered section of the ridge system runs down the middle of the Atlantic Ocean, it was found that most mid-ocean ridges are located away from the center of other ocean basins.<a class="footnote-ref" id="fnref:69" href="#fn:69"><sup>69</sup></a><a class="footnote-ref" id="fnref:70" href="#fn:70"><sup>70</sup></a> </p> <h3>Impact of discovery: seafloor spreading</h3> <p><a href="/facts/Alfred_Wegener/sXu37sav">Alfred Wegener</a> proposed the theory of <a href="/facts/Continental_drift/o7Nfr101">continental drift</a> in 1912. He stated: "the Mid-Atlantic Ridge ... zone in which the floor of the Atlantic, as it keeps spreading, is continuously tearing open and making space for fresh, relatively fluid and hot <a href="/facts/Sima_(geology)/0n4Ytwsv">sima</a> [rising] from depth".<a class="footnote-ref" id="fnref:71" href="#fn:71"><sup>71</sup></a> However, Wegener did not pursue this observation in his later works and his theory was dismissed by geologists because there was no mechanism to explain how <a href="/facts/Continent/Pysd9Sw8">continents</a> could plow through ocean <a href="/facts/Crust_(geology)/FYG1kP4F">crust</a>, and the theory became largely forgotten. </p><p>Following the discovery of the worldwide extent of the mid-ocean ridge in the 1950s, geologists faced a new task: explaining how such an enormous geological structure could have formed. In the 1960s, geologists discovered and began to propose mechanisms for <a href="/facts/Seafloor_spreading/2t2oCbTp">seafloor spreading</a>. The discovery of mid-ocean ridges and the process of seafloor spreading allowed for <a href="/facts/Alfred_Wegener/sXu37sav">Wegener's</a> theory to be expanded so that it included the movement of oceanic crust as well as the continents.<a class="footnote-ref" id="fnref:72" href="#fn:72"><sup>72</sup></a> Plate tectonics was a suitable explanation for seafloor spreading, and the acceptance of plate tectonics by the majority of geologists resulted in a major <a href="/facts/Paradigm_shift/Bj24vT0p">paradigm shift</a> in geological thinking. </p><p>It is estimated that along Earth's mid-ocean ridges every year 2.7 km2 (1.0 sq mi) of new seafloor is formed by this process.<a class="footnote-ref" id="fnref:73" href="#fn:73"><sup>73</sup></a> With a crustal thickness of 7 km (4.3 mi), this amounts to about 19 km3 (4.6 cu mi) of new ocean crust formed every year.<a class="footnote-ref" id="fnref:74" href="#fn:74"><sup>74</sup></a> </p> <h2 id="list-of-mid-ocean-ridges">List of mid-ocean ridges</h2> <p class="note">Main category: Oceanic ridges</p> <ul><li><a href="/facts/Aden_Ridge/5j4bqC5N">Aden Ridge</a> – Rift portion in Gulf of Aden</li> <li><a href="/facts/Cocos_Ridge/zgJ9g0oV">Cocos Ridge</a> – Aseismic ridge within the Cocos plate</li> <li><a href="/facts/Explorer_Ridge/Lx4eyDWr">Explorer Ridge</a> – Mid-ocean ridge west of British Columbia, Canada</li> <li><a href="/facts/Cocos%25E2%2580%2593Nazca_spreading_centre/904BNS7y">Cocos–Nazca spreading centre</a> – Spreading centre under central eastern Pacific Ocean <ul><li><a href="/facts/Gal%25C3%25A1pagos_spreading_centre/RoaWFkzA">Galápagos spreading centre</a> – Western part of the Cocos–Nazca spreading centre</li></ul></li> <li><a href="/facts/Gorda_Ridge/4kG7ra8G">Gorda Ridge</a> – Tectonic spreading center off the northern coast of California and southern Oregon</li> <li><a href="/facts/Juan_de_Fuca_Ridge/FNMX6mgj">Juan de Fuca Ridge</a> – Divergent plate boundary off the coast of the Pacific Northwest region of North America</li> <li><a href="/facts/South_American%25E2%2580%2593Antarctic_Ridge/W7e3d6Po">South American–Antarctic Ridge</a> – Mid-ocean ridge in the South Atlantic between the South American plate and the Antarctic plate</li> <li><a href="/facts/Chile_Rise/Lc1FDyYn">Chile Rise</a> – Submarine oceanic ridge in the Pacific OceanPages displaying short descriptions of redirect targets</li> <li><a href="/facts/East_Pacific_Rise/mYrxownC">East Pacific Rise</a> – Mid-oceanic ridge at a divergent tectonic plate boundary on the floor of the Pacific Ocean</li> <li><a href="/facts/Gakkel_Ridge/fpl7wvY3">Gakkel Ridge</a> – Mid-oceanic ridge under the Arctic Ocean(Mid-Arctic Ridge)</li> <li><a href="/facts/Pacific-Antarctic_Ridge/fBcabFPj">Pacific-Antarctic Ridge</a> – Tectonic plate boundary in the South Pacific OceanPages displaying short descriptions of redirect targets</li> <li><a href="/facts/Central_Indian_Ridge/LB7WN7Cv">Central Indian Ridge</a> – A north-south-trending mid-ocean ridge in the western Indian Ocean <ul><li><a href="/facts/Carlsberg_Ridge/Sap5e4ju">Carlsberg Ridge</a> – Tectonic plate ridge</li></ul></li> <li><a href="/facts/Southeast_Indian_Ridge/RhDdreoq">Southeast Indian Ridge</a> – Mid-ocean ridge in the southern Indian Ocean</li> <li><a href="/facts/Southwest_Indian_Ridge/FIoer8fR">Southwest Indian Ridge</a> – A mid-ocean ridge on the bed of the south-west Indian Ocean and south-east Atlantic Ocean</li> <li><a href="/facts/Mid-Atlantic_Ridge/q1Fgk4P1">Mid-Atlantic Ridge</a> – Atlantic Ocean tectonic plate boundary <ul><li><a href="/facts/Kolbeinsey_Ridge/rALUxFwp">Kolbeinsey Ridge</a> – Segment of the Mid-Atlantic Ridge north of Iceland in the Arctic Ocean</li> <li><a href="/facts/Mohns_Ridge/tXdDM4FT">Mohns Ridge</a> – Geographical region in the Atlantic basin</li> <li><a href="/facts/Nikolai_Mikhailovich_Knipovich/5FcqhqCm">Knipovich</a> – Russian zoologistPages displaying short descriptions of redirect targets Ridge (between Greenland and Spitsbergen)</li> <li><a href="/facts/Reykjanes_Ridge/q1Fgk4P1">Reykjanes Ridge</a> – Atlantic Ocean tectonic plate boundaryPages displaying short descriptions of redirect targets (south of Iceland)</li></ul></li></ul> <h3>List of ancient oceanic ridges</h3> <ul><li><a href="/facts/Aegir_Ridge/WFDf44RX">Aegir Ridge</a> – Extinct mid-ocean ridge in the far-northern Atlantic Ocean</li> <li><a href="/facts/Alpha_Ridge/l2pLlARm">Alpha Ridge</a> – Major volcanic ridge under the Arctic Ocean</li> <li><a href="/facts/Gal%25C3%25A1pagos_Rise/TKuXE3s8">Galápagos Rise</a> – Fossil divergent boundary</li> <li><a href="/facts/Kula-Farallon_Ridge/ntXHgEJc">Kula-Farallon Ridge</a> – Ancient mid-ocean ridgePages displaying short descriptions of redirect targets</li> <li><a href="/facts/Mid-Labrador_Ridge/F7hcxnBp">Mid-Labrador Ridge</a> – Mid-ocean ridge in the Labrador Sea</li> <li><a href="/facts/Pacific-Farallon_Ridge/Ha1eQcjK">Pacific-Farallon Ridge</a> – Spreading ridge during the Late CretaceousPages displaying short descriptions of redirect targets</li> <li><a href="/facts/Pacific-Kula_Ridge/1pVY0N2A">Pacific-Kula Ridge</a> – Former mid-ocean ridgePages displaying short descriptions of redirect targets</li> <li><a href="/facts/Phoenix_Ridge/m4IBHfAD">Phoenix Ridge</a> – Ancient mid-ocean ridge between the Phoenix and Pacific platesPages displaying short descriptions of redirect targets</li></ul> <h2 id="see-also">See also</h2> <ul> <li>Oceans portal</li><li>Volcanoes portal</li><li>Geography portal</li><li>Geology portal</li></ul> <ul><li><a href="/facts/Afar_Triangle/mx3gxv7W">Afar Triangle</a> – Geological depression caused by the Afar triple junction</li> <li><a href="/facts/Geography_of_Iceland/AxsxwpQV">Geography of Iceland</a></li> <li><a href="/facts/List_of_landforms/kpx9gKmj">List of oceanic landforms</a></li> <li><a href="/facts/Ocean_chemistry/AKV3gkUk">Ocean chemistry</a></li> <li><a href="/facts/Oceanic_crust/0lGjI7jN">Oceanic crust</a></li> <li><a href="/facts/Petrological_Database_of_the_Ocean_Floor/WmIQWNK5">Petrological Database of the Ocean Floor</a></li> <li><a href="/facts/Project_FAMOUS/1Dz9l90y">Project FAMOUS</a> – first crewed submersible study of the rift valley of the Mid-Atlantic Ridge</li> <li><a href="/facts/RISE_project_(oceanography)/RxmEXLHw">RISE project</a> – discovery of black smokers hydrothermal systems on the East Pacific Rise</li> <li><a href="/facts/Slab_window/aglYmrKk">Slab window</a> – Type of gap in a subducted oceanic plate</li> <li><a href="/facts/Submarine_volcano/HD4HjUgb">Submarine volcano</a> – Underwater vents or fissures in the Earth's surface from which magma can erupt</li> <li><a href="/facts/Vine%25E2%2580%2593Matthews%25E2%2580%2593Morley_hypothesis/va8DANvB">Vine-Matthews-Morely</a> hypothesis; explains relation of marine magnetic anomalies to seafloor spreading.</li></ul> <h2 id="external-links">External links</h2> Wikimedia Commons has media related to Mid-ocean ridges. <ul><li><a href="http://www.tectonic-forces.org">An explanation of relevant tectonic forces</a></li> <li><a href="https://pubs.usgs.gov/gip/dynamic/baseball.html">Mid-Oceanic ridge, like baseball seam (The Dynamic Earth, USGS)</a></li> <li><a href="https://web.archive.org/web/20160601003941/http://www.ridge2000.org/index.php">Ridge2000, Studying Mid-Ocean Ridges from Mantle to Microbe</a></li></ul> <h2 id="references">References</h2> <ol> <li id="fn:1"><p>"What is the longest mountain range on earth?". 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