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Serpentinization is a hydration and Metamorphic rock transformation of ferromagnesian minerals, such as olivine and pyroxene, in mafic and ultramafic rock to produce serpentinite. Minerals formed by serpentinization include the serpentine group minerals (antigorite, lizardite, chrysotile), brucite, talc, Ni-Fe alloys, and magnetite. The mineral alteration is particularly important at the sea floor at plate tectonics boundaries.
During serpentinization, large amounts of water are absorbed into the rock, increasing the volume, reducing the density and destroying the original structure. The density changes from with a concurrent volume increase on the order of 30-40%. The reaction is highly exothermic, releasing up to per mole of water reacting with the rock, and rock temperatures can be raised by about , Serpentinization: The heat engine at Lost City and sponge of the oceanic crust
Reaction 1a tightly binds silica, lowering its chemical activity to the lowest values seen in common rocks of the Earth's crust. Serpentinization then continues through the hydration of olivine to yield serpentine and brucite (Reaction 1b). The mixture of brucite and serpentine formed by Reaction 1b has the lowest silica activity in the serpentinite, so that the brucite phase is very important in understanding serpentinization. However, the brucite is often blended in with the serpentine such that it is difficult to identify except with X-ray diffraction, and it is easily altered under surface weathering conditions.
A similar suite of reactions involves pyroxene-group minerals:
Reaction 2a quickly comes to a halt as silica becomes unavailable, and Reaction 2b takes over. When olivine is abundant, silica activity drops low enough that talc begins to react with olivine:
This reaction requires higher temperatures than those at which brucite forms.
The final mineralogy depends both on rock and fluid compositions, temperature, and pressure. Antigorite forms in reactions at temperatures that can exceed during metamorphism, and it is the serpentine group mineral stable at the highest temperatures. Lizardite and chrysotile can form at low temperatures very near the Earth's surface.
This raises both the pH, often to very high values, and the calcium content of the fluids involved in serpentinization. These fluids are highly reactive and may transport calcium and other elements into surrounding mafic rocks. Fluid reaction with these rocks may create metasomatism reaction zones enriched in calcium and depleted in silica, called .
Studies of serpentinites suggest that in nature iron minerals are first converted to brucite, that is, brucite containing , which then undergoes the Schikorr reaction in the anaerobic conditions of serpentinization:
Maximum reducing conditions, and the maximum rate of production of hydrogen, occur when the temperature of serpentinization is between and when fluids are carbonate undersaturated. If the original ultramafic rock (the protolith) is peridotite, which is rich in olivine, considerable magnetite and hydrogen are produced. When the protolith is pyroxenite, which contains more pyroxene than olivine, iron-rich talc is produced with no magnetite and only modest hydrogen production. Infiltration of silica-bearing fluids during serpentinization can suppress both the formation of brucite and the subsequent production of hydrogen.
Chromite present in the protolith will be altered to chromium-rich magnetite at lower serpentinization temperatures. At higher temperatures, it will be altered to iron-rich chromite (ferrit-chromite). During serpentinization, the rock is enriched in chlorine, boron, fluorine, and sulfur. Sulfur will be reduced to hydrogen sulfide and sulfide minerals, though significant quantities are incorporated into serpentine minerals, and some may later be reoxidized to sulfate minerals such as anhydrite. The sulfides produced include nickel-rich sulfides, such as mackinawite.
Infiltration of -bearing fluids into serpentinite causes distinctive Talc carbonate. Brucite rapidly converts to magnesite and serpentine minerals (other than antigorite) are converted to talc. The presence of of the original serpentinite minerals shows that this alteration takes place after serpentinization.
Serpentinite may contain chlorite group (a phyllosilicate mineral), tremolite (Ca2(Mg5.0-4.5Fe2+0.0-0.5)Si8O22(OH)2), and metamorphic olivine and diopside (calcium-rich pyroxene). This indicates that the serpentinite has been subject to more intense metamorphism, reaching the upper greenschist or amphibolite metamorphic facies.
Above about , antigorite begins to break down. Thus serpentinite does not exist at higher metamorphic facies.
Using data from the Cassini probe flybys obtained in 2010–12, scientists were able to confirm that Saturn's moon Enceladus likely has a liquid water ocean beneath its frozen surface. A model suggests that the ocean on Enceladus has an alkaline pH of 11–12. The high pH is interpreted to be a key consequence of serpentinization of chondrite, that leads to the generation of , a geochemical source of energy that can support both abiotic and biological synthesis of organic molecules.
Serpentinization at slow spreading mid-ocean ridges can cause the seismic Moho discontinuity to be placed at the serpentinization front, rather than the base of the crust as defined by normal petrological criteria. The Lanzo Massif of the Italian Alps shows a sharp serpentinization front that may be a relict seismic Moho.
Because serpentinization lowers the density of the original rock, serpentinization may lead to uplift or exhumation of serpentinites to the surface, as has taken place with the serpentinite exposed at the Presidio of San Francisco following cessation of subduction.
Serpentinized ultramafic rock is found in many . Ophiolites are fragments of oceanic lithosphere that has been thrust onto continents, a process called obduction. They typically consist of a layer of serpentinized harzburgite (sometimes called alpine peridotite in older writings), a layer of hydrothermally altered and , and a layer of deep water sediments containing radiolarian ribbon chert.
(2026). 9780875904092 ISBN 9780875904092 providing an energy source for formation of non-volcanic hydrothermal vents. The hydrogen, methane, and hydrogen sulfide produced during serpentinization are released at these vents and provide energy sources for deep sea chemotroph . (2026). 9780875904092 ISBN 9780875904092
Formation of serpentine minerals
Olivine is a solid solution of forsterite, the magnesium endmember of , and fayalite, the iron endmember, with forsterite typically making up about 90% of the olivine in ultramafic rocks. Serpentine can form from olivine via several reactions:
Breakdown of diopside and formation of rodingites
Ultramafic rocks often contain calcium-rich pyroxene (diopside), which breaks down according to the reaction:
Formation of magnetite and hydrogen
In most crustal rock, the chemical activity of oxygen is prevented from dropping to very low values by the fayalite-magnetite-quartz (FMQ) buffer. The very low chemical activity of silica during serpentinization eliminates this buffer, creating highly reducing conditions that allow water to oxidize ferrous () ions in fayalite. This reaction modifies minerals and liberates hydrogen gas:
Methane and other hydrocarbons
Laboratory experiments have confirmed that at a temperature of and pressure of 500 bars, olivine serpentinizes with release of hydrogen gas. In addition, methane and complex hydrocarbons are formed through reduction of carbon dioxide. The process may be catalyzed by magnetite formed during serpentinization. One reaction pathway is:
Metamorphism at higher pressure and temperature
Lizardite and chrysotile are stable at low temperatures and pressures, while antigorite is stable at higher temperatures and pressure. Its presence in a serpentinite indicates either that serpentinization took place at unusually high pressure and temperature or that the rock experienced higher grade metamorphism after serpentinization was complete.
Extraterrestrial production of methane by serpentinization
The presence of traces of methane in the atmosphere of Mars has been hypothesized to be a possible evidence for life on Mars if methane was produced by activity. Serpentinization has been proposed as an alternative non-biological source for the observed methane traces. In 2022, it was reported that microscopic examination of the ALH 84001 meteorite, which came from Mars, shows that indeed the organic matter it contains was formed by serpentinization, not by life processes.
Environment of formation
Serpentinization occurs at mid-ocean ridges, in the forearc mantle of subduction zone zones, in ophiolite packages, and in ultramafic intrusions.
Mid-ocean ridges
Conditions are highly favorable for serpentinization at slow to ultraslow spreading mid-ocean ridges. Here the rate of crustal extension is high compared with the volume of magmatism, bringing ultramafic mantle rock very close to the surface where fracturing allows seawater to infiltrate the rock.
Subduction Zones
Forearc mantle
Serpentinization is an important phenomenon in subduction zones that has a strong control on the water cycle and geodynamics of a subduction zone. Here mantle rock is cooled by the subducting slab to temperatures at which serpentinite is stable, and fluids are released from the subducting slab in great quantities into the ultramafic mantle rock. Direct evidence that serpentinization is taking place in the Mariana Islands island arc is provided by the activity of serpentinite . of harzburgite and (less commonly) dunite are occasionally erupted by the mud volcanoes, giving clues to the nature of the protolith.
(2026). 9780521880060, Cambridge University Press. ISBN 9780521880060
Implications
Limitation on earthquake depth
Seismic wave studies can detect the presence of large bodies of serpentinite in the crust and upper mantle, since serpentinization has a huge impact on shear wave velocity. A higher degree of serpentinization will lead to lower shear wave velocity and higher Poisson's ratio. Seismic measurements confirm that serpentinization is pervasive in forearc mantle. The serpentinization can produce an inverted Moho discontinuity, in which seismic velocity abruptly decreases across the crust-mantle boundary, which is the opposite of the usual behavior. The serpentinite is highly deformable, creating an aseismic zone in the forearc, at which serpentinites slide at stable plate velocity. The presence of serpentinite may limit the maximum depth of megathrust earthquakes as they impede rupture into the forearc mantle.
See also
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