Recycling of water, carbon, and sulfur during subduction of serpentinites: A stable isotope study of Cerro del Almirez, Spain

Alt, Jeffrey C; Garrido, Carlos J.; Shanks, Wayne C.; Turchyn, Alexandra V.; Padrón‐Navarta, José Alberto; Sánchez‐Vizcaíno, Vicente López; Gómez-Pugnaire, María Teresa; Marchesi, Claudio

doi:10.1016/j.epsl.2012.01.029

Cited by 167 publications

(157 citation statements)

References 89 publications

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“…Interestingly, several studies suggest that the slab flux of H 2 O is decoupled to some extent from the flux of non-volatile LILE, which supports the hypothesis of distinct fluid reservoirs within the slab (Straub & Layne 2003a;Johnson et al 2009;Ruscitto et al 2012). Regardless of the dominance of slab-derived H 2 O and chlorine in arc magmas, however, mass-balance calculations suggest that a lesser amount of subducted H 2 O and chlorine is recycled at the arc relative to the amount either trapped in the mantle wedge or returned to the deeper mantle (Straub & Layne 2003b;Sharp & Barnes 2004;Kendrick et al 2011;Alt et al 2012). In contrast, elemental systematics of undegassed fluorine in arc magmas suggests that fluorine is poorly mobilized in slab fluids (Straub & Layne 2003b).…”

Section: Devolatilization Of the Subducting Slabsupporting

confidence: 55%

“…Staudigel et al 1996;Kerrick 2002;Alt et al 2012). Seawater also pervades the slab along steep, deep-reaching faults that cut through the crust and hydrate the lithosphere up to tens of kilometres depth by bending-related faulting at the trench (Ranero et al 2003; Fig.…”

Section: Devolatilization Of the Subducting Slabmentioning

confidence: 99%

“…Janardhan et al 1979;Cameron 1988). It is likely that sulphur, chlorine and carbon in arc magmas are in large part sourced from subducted altered oceanic crust (+subducted sediment) and subcrustal serpentinite, ultimately from seawater during hydrothermal interaction close to the ridge (Alt 1995;de Leeuw et al 2007;Sharp et al 2007;Barnes et al 2008Barnes et al , 2009aBarnes & Straub 2010;Alt et al 2012Alt et al , 2013. Available data suggest that up to about one-third of the subducted H 2 O may be returned to the deep mantle for the coldest slabs (Rüpke et al 2004); much less is returned for hotter slabs, where dehydration may begin in the fore-arc (Kerrick & Connolly 2001b).…”

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confidence: 99%

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Volatiles in subduction zone magmatism

Zellmer

Edmonds

Straub

2014

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Abstract:The volatile cycle at subduction zones is key to the petrogenesis, transport, storage and eruption of arc magmas. Volatiles control the flux of slab components into the mantle wedge, are responsible for melt generation through lowering the solidi of mantle materials, and influence the crystallizing phase assemblages in the overriding crust. Globally, magma ponding depths may be partially controlled by melt volatile contents. Volatiles also affect the rate and extent of degassing during magma storage and decompression, influence magma rheology and therefore control eruption style. The style of eruptions in turn determines the injection height of environmentally sensitive gases into the atmosphere and the impact of explosive arc volcanism. In this overview we summarize recent advances regarding the role of volatiles during slab dehydration, melt generation in the mantle wedge, magmatic evolution in the overriding crust, eruption triggering, and the release of some magmatic volatiles from volcanic edifices into the Earth's atmosphere.In contrast to mid-ocean ridge magmatism, where upwelling and adiabatic decompression of the mantle is the primary cause of melt generation, subduction zone magmatism is triggered by the depression of the mantle solidus due to influx of volatiles (dominantly There is ongoing debate about the processes that form extractable melts of the hydrated mantle wedge. One model suggests that efficient melt extraction requires a degree of melting of the wedge so large that melts are generally extracted at or above the 1300 8C isotherm, that is, close to the anhydrous solidus (Kushiro 1987;Schmidt & Poli 1998). The advective flux of heat carried by this melt then perturbs the location of the anhydrous solidus upwards (England & Katz 2010b), and melts eventually penetrate the lithosphere and enter the crust by hydrofracture and dyking. Alternatively, melting is dominated by decompression in slab and mantle diapirs that may rise upwards through the wedge (Behn et al. 2011).Here, we address volatile cycling from the dehydration of the subducting slab to arc volcanic degassing into the atmosphere (Fig. 1). A product of subduction is the output of volatiles as volcanic gases; another is the sinking of the slab containing 'residual' volatiles into the deep mantle. Volcanic gases in arcs are rich in H 2 O, chlorine, bromine and iodine compared to gases at rift and ocean island settings, which directly reflects the influence of slab-derived fluids on primary melt compositions by guest on May 10, 2018 http://sp.lyellcollection.org/ Downloaded from (Pyle & Mather 2009;Kutterolf et al. 2013; Kendrick et al. 2014a, b). Arc magmas are in general far richer in sulphur than their oceanic counterparts, reflecting the higher oxygen fugacity characteristic of arc melts and their enhanced capacity to carry dissolved sulphate (Wallace & Edmonds 2011). There is little direct evidence that primary arc melts are inherently richer in CO 2 than ocean island basalts, although it has been suggested that deep and pe...

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Section: Devolatilization Of the Subducting Slabsupporting

confidence: 55%

Section: Devolatilization Of the Subducting Slabmentioning

confidence: 99%

mentioning

confidence: 99%

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Volatiles in subduction zone magmatism

Zellmer

Edmonds

Straub

2014

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“…(a) Ocean floor metamorphism and metasomatism induced serpentinization stage of the ultramafic rocks and rodingitization of the intruded doleritic dykes (Puga et al [10,17,19]; Alt et al [22]). It also produced paragenesis of very high gradient in amphibolite facies, characteristic of ocean floor metamorphism, preserved in some gabbros and basalts [11,14,21,40].…”

Section: Petrology and Metamorphic Evolutionmentioning

confidence: 99%

“…This criticism on the oceanic nature of the BOA has been largely bypassed by recent papers which coupled radiometric dating to new petrological and geochemical studies (such as those in [13][14][15][16][17][18][19][20][21][22][23], among others), certainly ascribing the provenance of some BOA outcrops to a MORB-type tectonic setting, or to an Ocean-Continent-Setting (OCT). This hypothesis conforms to the interpretations proposed for ophiolite sequences of the Alps and Apennines as shown in [24][25][26][27][28][29][30][31].…”

Section: Introductionmentioning

confidence: 99%

The Betic Ophiolites and the Mesozoic Evolution of the Western Tethys

et al. 2017

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Abstract:The Betic Ophiolites consist of numerous tectonic slices, metric to kilometric in size, of eclogitized mafic and ultramafic rocks associated to oceanic metasediments, deriving from the Betic oceanic domain. The outcrop of these ophiolites is aligned along 250 km in the Mulhacén Complex of the Nevado-Filábride Domain, located at the center-eastern zone of the Betic Cordillera (SE Spain). According to petrological/geochemical inferences and SHRIMP (Sensitive High Resolution Ion Micro-Probe) dating of igneous zircons, the Betic oceanic lithosphere originated along an ultra-slow mid-ocean ridge, after rifting, thinning and breakup of the preexisting continental crust. The Betic oceanic sector, located at the westernmost end of the Tethys Ocean, developed from the Lower to Middle Jurassic (185-170 Ma), just at the beginning of the Pangaea break-up between the Iberia-European and the Africa-Adrian plates. Subsequently, the oceanic spreading migrated northeastward to form the Ligurian and Alpine Tethys oceans, from 165 to 140 Ma. Breakup and oceanization isolated continental remnants, known as the Mesomediterranean Terrane, which were deformed and affected by the Upper Cretaceous-Paleocene Eo-Alpine high-pressure metamorphic event, due to the intra-oceanic subduction of the Jurassic oceanic lithosphere and the related continental margins. This process was followed by the partial exhumation of the subducted oceanic rocks onto their continental margins, forming the Betic and Alpine Ophiolites. Subsequently, along the Upper Oligocene and Miocene, the deformed and metamorphosed Mesomediterranean Terrane was dismembered into different continental blocks collectively known as AlKaPeCa microplate (Alboran, Kabylian, Peloritan and Calabrian). In particular, the Alboran block was displaced toward the SW to occupy its current setting between the Iberian and African plates, due to the Neogene opening of the Algero-Provençal Basin. During this translation, the different domains of the Alboran microplate, forming the Internal Zones of the Betic and Rifean Cordilleras, collided with the External Zones representing the Iberian and African margins and, together with them, underwent the later alpine deformation and metamorphism, characterized by local differences of P-T (Pressure-Temperature) conditions. These Neogene metamorphic processes, known as Meso-Alpine and Neo-Alpine events, developed in the Nevado-Filábride Domain under Ab-Ep amphibolite and greenschists facies conditions, respectively, causing retrogradation and intensive deformation of the Eo-Alpine eclogites.

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Light Stable Isotopic Compositions of Enriched Mantle Sources: Resolving the Dehydration Paradox

Dixon

Bindeman

Kingsley

et al. 2017

Geochem Geophys Geosyst

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Volatile and stable isotope data provide tests of mantle processes that give rise to mantle heterogeneity. New data on enriched mid‐oceanic ridge basalts (MORB) show a diversity of enriched components. Pacific PREMA‐type basalts (H2O/Ce = 215 ± 30, δDSMOW = −45 ± 5 ‰) are similar to those in the northern Atlantic (H2O/Ce = 220 ± 30; δDSMOW = −30 to −40 ‰). Basalts with EM‐type signatures have regionally variable volatile compositions. Northern Atlantic EM‐type basalts are wetter (H2O/Ce = 330 ± 30) and have isotopically heavier hydrogen (δDSMOW = −57 ± 5 ‰) than northern Atlantic MORB. Southern Atlantic EM‐type basalts are damp (H2O/Ce = 120 ± 10) with intermediate δDSMOW (−68 ± 2 ‰), similar to δDSMOW for Pacific MORB. Northern Pacific EM‐type basalts are dry (H2O/Ce = 110 ± 20) and isotopically light (δDSMOW = −94 ± 3 ‰). A multistage metasomatic and melting model accounts for the origin of the enriched components by extending the subduction factory concept down through the mantle transition zone, with slab temperature a key variable. Volatiles and their stable isotopes are decoupled from lithophile elements, reflecting primary dehydration of the slab followed by secondary rehydration, infiltration, and re‐equilibration by fluids derived from dehydrating subcrustal hydrous phases (e.g., antigorite) in cooler, deeper parts of the slab. Enriched mantle sources form by addition of <1% carbonated eclogite ± sediment‐derived C‐O‐H‐Cl fluids to depleted mantle at 180–280 km (EM) or within the transition zone (PREMA).

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Recycling of water, carbon, and sulfur during subduction of serpentinites: A stable isotope study of Cerro del Almirez, Spain

Cited by 167 publications

References 89 publications

Volatiles in subduction zone magmatism

Volatiles in subduction zone magmatism

The Betic Ophiolites and the Mesozoic Evolution of the Western Tethys

Light Stable Isotopic Compositions of Enriched Mantle Sources: Resolving the Dehydration Paradox

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