Abstract
We report on the presence of the serpentine-type antigorite in abyssal-serpentinized peridotite. At mid-ocean spreading ridges, antigorite crystallizes under retrograde metamorphic conditions during tectonic exhumation of the newly formed oceanic lithosphere. Using optical microscopy and micro-Raman spectroscopy, we identified antigorite in 49 samples drilled at the Hess Deep (East Pacific Rise) and the Atlantis Massif (Mid-Atlantic Ridge, 30°N), and dredged along the Southwest Indian Ridge (62°–65°E). Overall, antigorite is common, but occurs in limited modal amounts. SEM and TEM investigations reveal its frequent crystallization after lizardite and chrysotile via dissolution–recrystallization processes and a local association with olivine or talc. We explain antigorite crystallization by the interaction with seawater-derived hydrothermal fluids moderately enriched in silica (metasomatism). The origin of silica is attributed to alteration of mafic intrusions or pyroxenes. Antigorite can, therefore, be considered a marker of preferential fluid pathways under rock-dominated conditions during exhumation of a portion of the oceanic lithosphere. We also measured the in-situ major and trace-element composition of antigorite and the predating and postdating phases. Most of the elements are immobile during the mineralogical transitions. Other elements (Ni, Ca, Al, and Ti) evolve within the serpentine textures, including antigorite, as a result of chemical exchanges accompanying the development of the sequence of serpentine textures. A further category includes elements that are specifically enriched (Mn, Sn) or depleted (Fluid-Mobile Elements: B, Sr, As, U, Sb, and Cl) in antigorite compared to lizardite and chrysotile. These enrichments and depletions possibly reflect a change of the fluid physicochemical characteristics allowing a change in element mobility during the dissolution–recrystallization accommodating the lizardite/chrysotile-to-antigorite transition. Such depletion in FME is comparable to depletions described in studies of serpentinization and antigorite formation in subduction zone setting, which suggests that the origin of antigorite in some subducted samples could be reevaluated.
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Acknowledgements
O. Laurent is thanked for his help during LA-ICPMS analyses and M.E. Galvez for fruitful discussion. We acknowledge support of the Scientific Center for Optical and Electron Microscopy (ScopeM) of the ETH Zürich and thank L.F.G. Morales for the realization of the FIB sections and C. Fellah for her help during TEM investigations. This manuscript benefited from constructive comments from two anonymous reviewers and editorial handling by O. Müntener. We gratefully acknowledge funding by the Swiss National Science Foundation (SNF) project No. 200021_163187 and funding from M. Cannat and the Institut de Physique du Globe de Paris (France). We also acknowledge ECORD (European Consortium for Ocean Research Drilling) for the implementation of Expedition 357, which provided drill core samples for this study.
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410_2019_1595_MOESM1_ESM.tif
Figure S1: Examples of antigorite domains with fibrous or lamellar texture. The preferential orientation oblique to the domains walls produces a sheared aspect. However, the lack of evidences for shearing (e.g., mesh texture shifted on both sides of the antigorite domain) indicates that these textures are not associated with significant deformation. The photos on the left are taken under cross-polarized light; those on the right are the equivalent taken with the addition of a wave plate (TIFF 14319 kb)
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Figure S2: In-situ major element composition of serpentine minerals and talc. a) CaO, b) MnO, c) Cl. The concentrations are given in weight %. The right panels indicate the loss or gain associated with the transition between antigorite and the serpentine (lizardite- or chrysotile-bearing texture) precursor (in % of the precursor texture composition). The vertical line indicates 100% (i.e., no loss or gain). The concentrations were normalized to the total oxide content (EPS 853 kb)
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Figure S3: In-situ concentrations of a) Sn and b) Ti in serpentine minerals and talc. The right panels correspond to the gain of the elements associated with antigorite crystallization after lizardite or chrysotile (in % of the precursor texture composition) (EPS 594 kb)
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Figure S4: In-situ concentrations of a) Cu, b) B, and c) Sr in serpentine minerals and talc. The right panels correspond to the loss of the elements associated with antigorite crystallization after lizardite or chrysotile (in % of the precursor texture composition) (EPS 814 kb)
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Figure S5: In-situ concentrations of a) As, b) Sb, and c) U in serpentine minerals and talc. The right panels indicate the loss or gain associated with the transition between antigorite and the serpentine (lizardite- or chrysotile-bearing texture) precursor (in % of the precursor texture composition). The vertical line indicates 100% (i.e., no loss or gain) (EPS 660 kb)
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Table S1: Major element composition of serpentine minerals and talc. For each element are given: 1) the averaged concentration (wt%), 2) the number of analyses averaged, 3) the standard deviation (2 sigma error) (XLSX 108 kb)
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Table S2: Trace-element composition of serpentine minerals and talc. For each element are given: 1) the averaged concentration (in ppm), 2) the number of analyses averaged, 3) the standard deviation (2 sigma error). bdl: below detection limit (XLSX 247 kb)
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Rouméjon, S., Andreani, M. & Früh-Green, G.L. Antigorite crystallization during oceanic retrograde serpentinization of abyssal peridotites. Contrib Mineral Petrol 174, 60 (2019). https://doi.org/10.1007/s00410-019-1595-1
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DOI: https://doi.org/10.1007/s00410-019-1595-1