Matches in SemOpenAlex for { <https://semopenalex.org/work/W2016060298> ?p ?o ?g. }
- W2016060298 endingPage "1641" @default.
- W2016060298 startingPage "1621" @default.
- W2016060298 abstract "The Xinjie mafic–ultramafic layered intrusion in the Emeishan large igneous province (ELIP) hosts Cu–Ni–platinum group element (PGE) sulfide ore layers within the lower part and Fe–Ti–V oxide-bearing horizons within the middle part. The major magmatic Cu–Ni–PGE sulfide ores and spatially associated cumulate rocks are examined for their PGE contents and Re–Os isotopic systematics. The samples yielded a Re–Os isochron with an age of 262 ± 27 Ma and an initial 187Os/188Os of 0.12460 ± 0.00011 (γOs(t) = −0.5 ± 0.1). The age is in good agreement with the previously reported U–Pb zircon age, indicating that the Re–Os system remained closed for most samples since the intrusion emplacement. They have near-chondritic γOs(t) values ranging from −0.7 to −0.2, similar to those of the Lijiang picrites and Song Da komatiites. Exceptionally, two samples from the roof zone and one from upper sequence exhibit radiogenic γOs(t) values (+0.6 to +8.6), showing minor contamination by the overlying Emeishan basalts. The PGE-rich ores contain relatively high PGE and small amounts of sulfides (generally less than 2%) and the abundance of Cu and PGE correlate well with S, implying that the distribution of these elements is controlled by the segregation and accumulation of a sulfide liquid. Some ore samples are poor in S (mostly <800 ppm), which may due to late-stage S loss caused by the dissolution of FeS from pre-existing sulfides through their interaction with sulfide-unsaturated flowing magma. The combined study shows that the Xinjie intrusion may be derived from ferropicritic magmas. The sharp reversals in Mg#, Cr/FeOT and Cr/TiO2 ratios immediately below Units 2–4, together with high Cu/Zr ratios decreasing from each PGE ore layer within these cyclic units, are consistent with multiple magma replenishment episodes. The sulfides in the cumulate rocks show little evidence of PGE depletion with height and thus appear to have segregated from successive inputs of fertile magma. This suggests that the Xinjie intrusion crystallized from in an open magma system, e.g., a magma conduit. The compositions of the disseminated sulfides in most samples can be modeled by applying an R factor (silicate–sulfide mass ratio) of between 1000 and 8000, indicating the segregation of only small amounts of sulfide liquid in the parental ferropicritic magmas. Thus, continuous mixing between primitive ferropicritic magma and differentiated resident magma could lead to crystallization of chromite, Cr-bearing magnetite and subsequently abundant Fe–Ti oxides, thereby the segregation of PGE-rich Cu-sulfide. When considered in the light of previous studies on plume-derived komatiites and picrites worldwide, the close-to-chondritic Os isotopic composition for most Xinjie samples, Lijiang picrites and Song Da komatiites suggest that the ferropicritic magma in the ELIP were generated from a plume. This comprised recycled Neoproterozic oceanic lithosphere, including depleted peridotite mantle embedded with geochemically enriched domains. The ascending magmas thereafter interacted with minor (possibly <10%) subducted/altered oceanic crust. This comparison suggests that the komatiitic melts in the ELIP originated from a greater-than normal degree of melting of incompatible trace element depleted, refractory mantle components in the plume source." @default.
- W2016060298 created "2016-06-24" @default.
- W2016060298 creator A5040185651 @default.
- W2016060298 creator A5041038245 @default.
- W2016060298 creator A5041184888 @default.
- W2016060298 creator A5050072653 @default.
- W2016060298 creator A5061202307 @default.
- W2016060298 creator A5071668095 @default.
- W2016060298 creator A5082651070 @default.
- W2016060298 creator A5086608598 @default.
- W2016060298 date "2011-03-01" @default.
- W2016060298 modified "2023-10-13" @default.
- W2016060298 title "Rhenium–osmium isotope and platinum-group elements in the Xinjie layered intrusion, SW China: Implications for source mantle composition, mantle evolution, PGE fractionation and mineralization" @default.
- W2016060298 cites W1963825843 @default.
- W2016060298 cites W1967359802 @default.
- W2016060298 cites W1977366308 @default.
- W2016060298 cites W1978484550 @default.
- W2016060298 cites W1980383181 @default.
- W2016060298 cites W1981080939 @default.
- W2016060298 cites W1981316911 @default.
- W2016060298 cites W1983176626 @default.
- W2016060298 cites W1984787349 @default.
- W2016060298 cites W1985417304 @default.
- W2016060298 cites W1985531665 @default.
- W2016060298 cites W1986740297 @default.
- W2016060298 cites W1992929460 @default.
- W2016060298 cites W1994259091 @default.
- W2016060298 cites W1996590499 @default.
- W2016060298 cites W1997606350 @default.
- W2016060298 cites W1999502028 @default.
- W2016060298 cites W1999985630 @default.
- W2016060298 cites W2001989120 @default.
- W2016060298 cites W2004856555 @default.
- W2016060298 cites W2004984013 @default.
- W2016060298 cites W2006739903 @default.
- W2016060298 cites W2011250343 @default.
- W2016060298 cites W2012348468 @default.
- W2016060298 cites W2013259970 @default.
- W2016060298 cites W2015499205 @default.
- W2016060298 cites W2016845353 @default.
- W2016060298 cites W2017062745 @default.
- W2016060298 cites W2019068836 @default.
- W2016060298 cites W2021130482 @default.
- W2016060298 cites W2026299727 @default.
- W2016060298 cites W2028476972 @default.
- W2016060298 cites W2030279977 @default.
- W2016060298 cites W2031194632 @default.
- W2016060298 cites W2031929480 @default.
- W2016060298 cites W2034077731 @default.
- W2016060298 cites W2034706864 @default.
- W2016060298 cites W2037386539 @default.
- W2016060298 cites W2037740207 @default.
- W2016060298 cites W2039533225 @default.
- W2016060298 cites W2039535921 @default.
- W2016060298 cites W2039932144 @default.
- W2016060298 cites W2040022671 @default.
- W2016060298 cites W2041258049 @default.
- W2016060298 cites W2042692134 @default.
- W2016060298 cites W2043127376 @default.
- W2016060298 cites W2044129104 @default.
- W2016060298 cites W2045068986 @default.
- W2016060298 cites W2047274210 @default.
- W2016060298 cites W2048022862 @default.
- W2016060298 cites W2049891776 @default.
- W2016060298 cites W2051704045 @default.
- W2016060298 cites W2055839245 @default.
- W2016060298 cites W2056583736 @default.
- W2016060298 cites W2056670083 @default.
- W2016060298 cites W2064067585 @default.
- W2016060298 cites W2064174314 @default.
- W2016060298 cites W2066300646 @default.
- W2016060298 cites W2066563289 @default.
- W2016060298 cites W2068198751 @default.
- W2016060298 cites W2069266540 @default.
- W2016060298 cites W2076755830 @default.
- W2016060298 cites W2077430827 @default.
- W2016060298 cites W2078741558 @default.
- W2016060298 cites W2079396235 @default.
- W2016060298 cites W2079855039 @default.
- W2016060298 cites W2082384972 @default.
- W2016060298 cites W2084322477 @default.
- W2016060298 cites W2086173842 @default.
- W2016060298 cites W2087791495 @default.
- W2016060298 cites W2088176011 @default.
- W2016060298 cites W2088427407 @default.
- W2016060298 cites W2088868264 @default.
- W2016060298 cites W2090035514 @default.
- W2016060298 cites W2091758632 @default.
- W2016060298 cites W2091806877 @default.
- W2016060298 cites W2092208675 @default.
- W2016060298 cites W2097228887 @default.
- W2016060298 cites W2102148551 @default.
- W2016060298 cites W2104024149 @default.
- W2016060298 cites W2108538927 @default.
- W2016060298 cites W2109353358 @default.
- W2016060298 cites W2114110021 @default.
- W2016060298 cites W2114949821 @default.
- W2016060298 cites W2115021200 @default.