Mantle Melting as a Function of Water Content beneath the Mariana Arc

Kelley, K. A.; Plank, Terry; Newman, Sally; Stolper, Edward M.; Grove, T. L.; Parman, S. W.; Hauri, E. H.

doi:10.1093/petrology/egq036

Cited by 200 publications

(180 citation statements)

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“…Mineral melt models of Roeder and Emslie (1970), Danyushevsky (2001), and Ariskin and Barmina (1999) were used, treating Fe 2+ /Fe 3+ as a closed system (Danyushevsky & Plechov, 2011 Kelley et al (2010) and Shaw et al (2008), respectively. The white circles are whole rock data for tephras collected at Alamagan volcano (Plank, unpublished data).…”

Section: Sensitivity Test Of Primary Melt Model Resultsmentioning

confidence: 99%

Variations in Fe3+/∑Fe of Mariana Arc Basalts and Mantle Wedge fO2

Brounce

Kelley

Cottrell

2014

Journal of Petrology

221

145

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When collecting Fe-µ-XANES spectra on olivine-hosted melt inclusions, it is important to avoid hitting the olivine crystal with the beam during analysis. Olivine contains several weight percent of Fe 2+ and even a very small amount of olivine interference will "contaminate" the pre-edge structure of Fe-µ-XANES spectra collected for melt inclusions and bias the result towards more reduced values. The region of XANES spectra at higher energies than the Fe-Kα absorption edge contains information related to Fe-coordination and can be used to distinguish glass structure (random and on average, uncoordinated) from olivine signal (strong coordination, Fig. A1). All melt inclusion and seafloor glass spectra were visually inspected and compared to spectra taken on San Carlos olivine and standard glasses from Cottrell et al. (2009) in order to screen for crystal contamination. Any spectra demonstrating signs of spectral features similar to those observed in San Carlos olivine were not considered in this study and additional spectra were collected to accommodate for this elimination. Model liquid lines of descentTo constrain the effects of fractional crystallization on magmatic Fe 3+ /∑Fe ratios, model liquid lines of descent that match the observed major element variations were generated using PetroLog3 (Danyushevsky & Plechov, 2011). The mineral-melt models that most closely replicate the natural data were chosen for each location, resulting in some variation in the models used from volcano to volcano. Individual model parameters

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Section: Sensitivity Test Of Primary Melt Model Resultsmentioning

confidence: 99%

Variations in Fe3+/∑Fe of Mariana Arc Basalts and Mantle Wedge fO2

Brounce

Kelley

Cottrell

2014

Journal of Petrology

221

145

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“…Currently, these temperatures are thought to be relatively high, mainly based on numerical models, on the composition of melt inclusions in olivine and on the composition of basalts [4, 14,39,40,41]. Numerical models now take into account a strong mechanical coupling between slab and mantle at relatively shallow depth of ∼ 50 to 80 km [4, 14,40,42].…”

Section: Temperature and Time Constraintsmentioning

confidence: 99%

“…For the hot corner of the mantle wedge at a depth of ∼ 40 to 80 km, more extreme temperatures in excess of 1300 • C are estimated [39,41,43]. These temperatures are calculated based on the assumption that the magmas erupted at arcs were initially derived from depleted harzburgitic mantle with Mg-rich olivine and orthopyroxene in the residue, and that the observed lavas have been modified by olivine fractionation and degassing [39,43].…”

Section: Temperature and Time Constraintsmentioning

confidence: 99%

Arc magmas sourced from mélange diapirs in subduction zones

2012

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At subduction zones, crustal material is recycled back into the mantle. A certain proportion, however, is returned to the overriding plate via magmatism. The magmas show a characteristic range of compositions that have been explained by three-component mixing in their source regions: hydrous fluids derived from subducted altered oceanic crust and components derived from the thin sedimentary veneer are added to the depleted peridotite in the mantle beneath the volcanoes. However, currently no uniformly accepted model exists for the physical mechanism that mixes the three components and transports them from the slab to the magma source.Here we present an integrated physico-chemical model of subduction zones that emerges from a review of the combined findings of petrology, modelling, geophysics, and geochemistry: Intensely mixed metamorphic rock formations, so-called mélanges, form along the slab-mantle interface and comprise the characteristic trace-element patterns of subduction-zone magmatic rocks. We consider mélange formation the physical mixing process that is responsible for the geochemical three-component pattern of the magmas. Blobs of low-density mélange material, so-called diapirs, rise buoyantly from the surface of the subducting slab and provide a means of transport for well-mixed materials into the mantle beneath the volcanoes, where they produce melt. Our model provides a consistent framework for the interpretation of geophysical, petrological and geochemical data of subduction zones.Geochemical studies of volcanic rocks erupted at convergent plate margins have identified element and isotopic ratios that seem to require material present in their source that is absent in volcanic rocks from other settings, such as mid-ocean ridge basalts [1]. This subduction zone geochemical fingerprint has led to the establishment of three-component mixing models to explain the composition of magmatic rocks produced at continental and island arcs [2, 3]. Their trace-element characteristics are believed to have originated from two distinct sources added to the depleted mantle source: hydrous fluids derived from subducted altered ocean crust and a component derived from the thin sedimentary veneer of the slab. However, the details of the physical process that allows the mixing of these components within the * Corresponding author. Tel: +1-508-289-2776. Fax: +1-508-457- E-mail: hmarschall@whoi.eduEmail address: hmarschall@whoi.edu (Horst R. Marschall)."subduction factory" are unknown. Current models propose that a hydrous component, enriched in incompatible trace elements, is released from the subducting slab and migrates into the overlying mantle wedge. The wedge is at much higher temperatures than the slab due to the 'corner flow' of the asthenospheric mantle, driven by viscous coupling of the mantle to the subducting slab [4]. Mantle-wedge peridotite partial melting is thought to be promoted by the influx of slab-derived fluids [5]. Yet, no uniformly accepted model exists for the actual physical mechanism tha...

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“…Large igneous provinces: Li et al (2012), Wei et al (2014), Zhang et al (2006). Through wet melting experiments and direct measurements of H 2 O in melt inclusions, many workers believe that water (H 2 O N 2%) plays a dominate role in the formation of calc-alkaline HAB (Ariskin, 1999;Beard and Lofgren, 1992;Grove et al, 2012;Kelley et al, 2010;Grove, 1993a, 1993b). Nevertheless, others proposed that a tholeiite HAB is close to an anhydrous composition in which high pressure suppresses plagioclase fractionation (Bartels et al, 1991;Crawford et al, 1987;Draper and Johnston, 1992;Eason and Sinton, 2006;Grove et al, 1982;Le Voyer et al, 2010;Sisson and Bronto, 1998).…”

Section: Factors Controlling High Al Contents In the Bogda Habsmentioning

confidence: 99%