US EPA

469312 

Journal Article 

Control of the Products of Serpentinization by the (FeMg1)-Mg-2 Exchange Potential of Olivine and Orthopyroxene 

Evans, BW 

2008 

Yes 

Journal of Petrology
ISSN: 0022-3530
EISSN: 1460-2415 

49 

10 

1873-1887 

English 

10.1093/petrology/egn050 

WOS:000261170200006 

It is argued that the high-Mg content (mg-number 95 3) of the serpentine minerals in serpentinized peridotite is a consequence of the environmental (FeMg1)-Mg-2 exchange potential imposed on the system by the abundance of olivine and orthopyroxene. Mass balance in the serpentinization reaction then requires the precipitation of an iron-rich mineral that in most cases is magnetite. This causes hydrogen to be evolved in an oxygen-conserved reaction. The low-variance mineral assemblage Ol Srp Brc Mag sets the chemical potentials of H2O, SiO2 and O-2 internally at an early stage in the process, but the paragenetic assessment of serpentinites is rendered difficult by the variable and usually unknown Fe-3 content of the serpentine minerals, particularly lizardite. Whole-rock analyses of highly to completely serpentinized peridotites reveal Fe-3/Fe ratios 04, with an average value (069) similar to that of magnetite (067). This feature may be attributed to the presence of high-Fe-3 lizardite, as has been found in Mssbauer spectroscopy studies. Electron microprobe and scanning electron microcope analyses in the literature exhibit element trends (e.g. decreasing Si vs Fe a.p.f.u.) for olivine-pseudomorph lizardite and, with some exceptions, for bastite lizardite, that show a substitution of the cronstedtite component (Fe-3 charge-balanced on T and M sites). Cronstedtite substitution will be favoured at low temperature and/or low hydrogen fugacity, and in these circumstances less magnetite will be evolved during serpentinization, in some cases none at all. Some bastite lizardites from sea-floor settings show evidence of M-site vacancy substitution of Fe-3 for Fe-2. In the course of progressive serpentinization, micrometer to millimeter-scale variations in SiO2 potential may well be present, but their influence on Fe in lizardite seems to be limited to a few cases of lizardite associated with orthopyroxene. Chrysotile is on average more Mg-rich and less variable in Fe/Mg ratio than lizardite, facts that may be attributed to the greater Fe-3 content of lizardite. Chrysotile veins provide the best record available to us of the environmental (FeMg1)-Mg-2 exchange potential in the pore fluid attending serpentinization. This potential serves as a robust control on serpentine and brucite compositions, although it may fail after olivine and orthopyroxene have been armoured or eliminated, and in more open-system environments (high water/rock ratio) such as on the sea floor or at serpentinite host-rock contacts. The default assumption in microprobe analyses that measured iron is all Fe-2 can lead to inappropriate petrological conclusions in the case of serpentinites. 

hydrothermal systems; lost-city; abyssal peridotites; crystal-structure; ultramafic rocks; british-columbia; subduction; zones; midocean ridges; lizardite 1t; chrysotile