A review of melt migration processes in the adiabatically upwelling mantle beneath oceanic spreading ridges

Kelemen, P. B.; Hirth, G.; Shimizu, N.; Spiegelman, Marc; Dick, H. J.

doi:10.1017/cbo9780511600050.005

Cited by 226 publications

(416 citation statements)

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“…Viscosities in the low end of this range probably require both dissolved hydrogen [Mei and Kohlstedt, 2000;Hirth and Kohlstedt, 1996;Kohlstedt et al, 1996], as might be expected in the relatively H 2 O-rich mantle above a subduction zone, and melt fractions greater than ~ 3 % [Kelemen et al, 1997;Hirth and Kohlstedt, 1995a;Hirth and Kohlstedt, 1995b].…”

Section: A Experimentally Constrained Mantle Viscositiesmentioning

confidence: 82%

Thermal structure due to solid-state flow in the mantle wedge beneath arcs

Kelemen

Rilling

Parmentier

et al. 2003

Inside the Subduction Factory

186

177

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We summarize petrological and seismic constraints on the temperature of arc lower crust and shallow mantle, and show that published thermal models are inconsistent with these constraints. We then present thermal models incorporating temperature-dependent viscosity, using widely accepted values for activation energy and asthenospheric viscosity. These produce thin thermal boundary layers in the wedge corner, and an overall thermal structure that is consistent with other temperature constraints. Some of these models predict partial melting of subducted sediment and/or basalt, even though we did not incorporate the effect of shear heating We obtain these results for subduction of 50 Myr old oceanic crust at 60 km/Myr, and even for subduction of 80 Myr old crust at 80 km/Myr, suggesting that melting of subducted crust may not be not restricted to slow subduction of young oceanic crust.

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Section: A Experimentally Constrained Mantle Viscositiesmentioning

confidence: 82%

Thermal structure due to solid-state flow in the mantle wedge beneath arcs

Kelemen

Rilling

Parmentier

et al. 2003

Inside the Subduction Factory

186

177

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“…However, studies of rocks from the upper mantle and experimental simulations of liquid migration in porous media have shown that liquid may ascend a partly molten rock column (e.g., peridotite) either through a pervasive porous flow or through a channelized flow (Kelemen et al 1995(Kelemen et al , 1997Ertan and Leeman 1996;Beccaluva et al 2004;Van Den Bleeken et al 2010). In the mantle wedge, whether the liquid migrates as a porous flow or as a channel flow depends on processes of reactive infiltration-dissolution (Daines and Kohlstedt 1994;Morgan and Liang 2003) and also on the grain size of the porous medium (Wark and Watson 2000).…”

Section: Insight From Plagioclase Compositional Profilesmentioning

confidence: 99%

Efficiency of compaction and compositional convection during mafic crystal mush solidification: the Sept Iles layered intrusion, Canada

Namur

Charlier

2012

Contrib Mineral Petrol

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Adcumulate formation in mafic layered intrusions is attributed either to gravity-driven compaction, which expels the intercumulus melt out of the crystal matrix, or to compositional convection, which maintains the intercumulus liquid at a constant composition through liquid exchange with the main magma body. These processes are length-scale and time-scale dependent, and application of experimentally derived theoretical formulations to magma chambers is not straightforward. New data from the Sept Iles layered intrusion are presented and constrain the relative efficiency of these processes during solidification of the mafic crystal mush. Troctolites with meso-to ortho-cumulate texture are stratigraphically followed by Fe-Ti oxide-bearing gabbros with adcumulate texture. Calculations of intercumulus liquid fractions based on whole-rock P, Zr, V and Cr contents and detailed plagioclase compositional profiles show that both compaction and compositional convection operate, but their efficiency changes with liquid differentiation. Before saturation of Fe-Ti oxides in the intercumulus liquid, convection is not active due to the stable liquid density distribution within the crystal mush. At this stage, compaction and minor intercumulus liquid crystallization reduce the porosity to 30%. The velocity of liquid expulsion is then too slow compared with the rate of crystal accumulation. Compositional convection starts at Fe-Ti oxide-saturation in the pore melt due to its decreasing density. This process occurs together with crystallization of the intercumulus melt until the residual porosity is less than 10%. Compositional convection is evidenced by external plagioclase rims buffered at An 61 owing to continuous exchange between the intercumulus melt and the main liquid body. The change from a channel flow regime that dominates in troctolites to a porous flow regime in gabbros results from the increasing efficiency of compaction with differentiation due to higher density contrast between the cumulus crystal matrix and the equilibrium melts and to the bottom-up decreasing rate of crystal accumulation in the magma chamber.

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“…Geosystems G 3 G a function of porosity in partially molten mantle rocks Kohlstedt, 1995a, 1995b;Kelemen et al, 1997]) becomes equal to the rate of unstable formation of pore space due to reactive porous flow of ascending melt. Width/frequency measurements for very large dunites, for example, in the Oman ophiolite, may help provide constraints on this question.…”

Section: Geochemistry Geophysicsmentioning

confidence: 99%

“…Therefore some dunites may form purely as a result of reactive porous flow processes, and the presence of melt filled cracks is not required to explain them. Furthermore, Kelemen et al [1997] showed that focused flow of melt in porous conduits can satisfy melt velocity constraints derived from uranium series disequilibria in MORB [Lundstrom et al, 1995[Lundstrom et al, , 1999Sims et al, 1995;Volpe and Goldstein, 1993] and from the timing of volcanism due to decompression melting following deglaciation in Iceland [Slater et al, 1998;M. Jull and D. McKenzie, The effect of deglaciation on mantle melting beneath Iceland, submitted to Journal of Geophysical Research, 1995], so that melt transport in cracks is not required by these data, either.…”

Section: Introductionmentioning

confidence: 99%

Spatial distribution of melt conduits in the mantle beneath oceanic spreading ridges: Observations from the Ingalls and Oman ophiolites

Kelemen

Braun

Hirth

2000

Geochem Geophys Geosyst

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[1] Ophiolites are on-land exposures of igneous crust and residual upper mantle formed beneath submarine spreading ridges. Upper mantle outcrops in ophiolites provide insight into focusing of melt transport from a $100 km wide region of partial melting into an $5 km wide zone of igneous crustal accretion beneath the ridges. Dunite veins, composed of the minerals olivine and spinel, mark conduits for melt transport through at least the uppermost 30 km of the mantle. New data in this paper, on dunite veins in the Ingalls ophiolite, central Washington Cascades, show a power law relationship between frequency and width, in which frequency/m %0.02 width À3 over a size interval from $0.1 to 2 m. There may be several ways to generate this relationship, but we favor the hypothesis that the dunites represent a coalescing melt transport network. This conclusion is broadly consistent with the related hypothesis that mantle melt extraction occurs in a fractal, branching network, and with recent results on formation of a coalescing network of dissolution channels via flow of a solvent through a partially soluble, compacting porous medium.

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A review of melt migration processes in the adiabatically upwelling mantle beneath oceanic spreading ridges

Cited by 226 publications

References 0 publications

Thermal structure due to solid-state flow in the mantle wedge beneath arcs

Thermal structure due to solid-state flow in the mantle wedge beneath arcs

Efficiency of compaction and compositional convection during mafic crystal mush solidification: the Sept Iles layered intrusion, Canada

Spatial distribution of melt conduits in the mantle beneath oceanic spreading ridges: Observations from the Ingalls and Oman ophiolites

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