Experimental determination of the Si isotope fractionation factor between liquid metal and liquid silicate

Hin, Remco C.; Fitoussi, Caroline; Schmidt, Max W.; Bourdon, Bernard

doi:10.1016/j.epsl.2013.11.016

Cited by 58 publications

(78 citation statements)

References 52 publications

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“…Oxygen fugacity can be controlled by surrounding sample materials with buffer materials. In order to study Si isotope fractionation between metal and silicate, piston-cylinder experiments were run between 0.54 and 1 GPa pressure and in a temperature range between 1450 and 1800°C by Shahar et al (2009Shahar et al ( , 2011 and Hin et al (2014). The latter study used a rotating piston-cylinder apparatus (Schmidt et al, 2006) that enabled improved density separation of metal and silicate phases.…”

Section: High-pressure Experimental Methodsmentioning

confidence: 99%

“…Georg et al, 2007;Shahar et al, 2009Shahar et al, , 2011Ziegler et al, 2010;Kempl et al, 2013a;Hin et al, 2014), driven by the different chemical bonding environment of Si in silicate rocks versus metallic liquid Georg et al, 2007). If Si isotope fractionation between metal and silicate is an equilibrium process, the heavier isotopes fractionate preferentially into the stiffer bonded phase, in this case the silicate.…”

Section: The Role Of Si Stable Isotopesmentioning

confidence: 99%

“…Kempl et al (2013b) approached the study of Si isotope fractionation processes at high temperature conditions in an industrial-scale experiment by sampling metal and silicate phases from a blast furnace at Tatasteel IJmuiden, the Netherlands, with maximum temperatures reaching 1600°C during sampling. Hin et al (2014) performed experiments between 0.5 and 1 GPa pressure, and a temperature range between 1450 and 1750°C.…”

Section: The Role Of Hpt Experimentsmentioning

confidence: 99%

“…The hot-metal alloy commonly contained Hin et al (2014) were completely molten and consisted of a silicate melt and a metal alloy bearing between 4.7 and 5.8 wt% Si. Kempl et al (2013a) performed a time series at 9 GPa and 2100°C in which the silicate consisted of 80 wt% forsterite (fo) and 20 wt% diopside (di) prepared from the major element oxides SiO 2 , MgO and CaCO 3 .…”

Section: Starting Materials and Compositionsmentioning

confidence: 99%

“…Experimental HT and HPT data of Kempl (2013) and Kempl et al (2013); B. Experimental HPT data of Hin et al (2014); C. Si isotope fractionation of two differentiated stoneiron meteorites (Ziegler et al, 2010); D. Experimental HPT data of Shahar et al (2011) between 3.5 and 4.1 wt%, depending on the experimental run time. The synthesised silicate melts contain SiO 2 concentrations between 37.7 and 43.9 wt%.…”

Section: This Studymentioning

confidence: 99%

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Silicon stable isotope fractionation between metal and silicate at high-pressure, high-temperature conditions as a tracer of planetary core formation

Kempl

Vroon

Wagt

et al. 2016

Netherlands Journal of Geosciences

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The largest differentiation event in Earth and other terrestrial planets was the high-pressure, high-temperature process of metal core segregation from a silicate mantle. The abundant element silicon (Si) can be partially sequestered into the metallic core during metal-silicate differentiation, depending on pressure, temperature and planetary oxidation state. Knowledge of the Si content of a planet's core can constrain the conditions of core formation, but in the absence of direct samples from planetary cores, quantifying core Si content is challenging. One relatively new tool to study core formation in terrestrial planets is based on combining measurements of the Si stable isotopic composition of planetary crust and mantle samples with measurements of the Si stable isotope fractionation between metal and silicate at high-temperature and high-pressure conditions. In this study we present the results of a small set of high-pressure, high-temperature (HPT) experiments and combine these with a review of literature data to investigate how the Si isotope fractionation behaviour between metal and silicate varies as a function specifically of experimental run time and temperature. We show that although there is no debate about the sign of fractionation, absolute values for Si isotope fractionation between metal and silicate are difficult to constrain because the experimental database remains incomplete, and because Si isotopic measurements of metals in particular suffer from the absence of a true inter-laboratory comparison. We conclude that in order to derive accurate quantitative estimates of the Si content of the core of the Earth or other planets a wide range of additional experiments will be required.

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