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(Na,Al)-rich silicate glass commonly associated with the carbonates is a major host for many incompatible lithophile elements in the carbonate-bearing pockets. The carbonates are rich in Sr and Ba, but have low contents of rare earth elements. Carbonates in the xenoliths occur in fine-grained pockets that appear to have been produced by reaction of carbonate-rich melts with the host peridotites. The trace element compositions of carbonate, clinopyroxene, amphibole and silicate glass were determined in four mantle lherzolite xenoliths in alkali basalts from Spitsbergen and Mongolia by laser ablation ICP-MS. Battlefield the songJapan is the second biggest economy in the world and one of the most.Mantle Cell Lymphoma Consortium Member: Lymphoma Research Foundation: 2011: Career Development Award, Mentored (K08) NIH, National Heart, Lung, and Blood Institute: 2010: Post-Doctoral Fellow, Career Development Award: Leukemia and Lymphoma Society: 2008: Yamaguchi Award in Hematology Research: Childrens Hospital, Boston MA: 1999: Pre-Doctoral. Clinopyroxene and amphibole outside the carbonate-bearing pockets in the xenoliths from Spitsbergen have high contents of incompatible trace elements, indicating that the lherzolites also experienced metasomatic enrichment before the formation of the carbonates.the processes of changes in the handling of the power mantles at these levels. However, the absolute incompatible element abundances estimated for those liquids cannot provide the extremely strong enrichments invoked by some models of carbonate mantle metasomatism. Trace element patterns estimated for liquids that may have produced the carbonate-bearing pockets are consistent with general characteristics of carbonate-related metasomatism (enrichments in light rare earth elements, Th, U, Ba and negative anomalies for high field strength elements). ![]() It is not clear, however, whether such data are relevant in this case because liquid immiscibility may not have played an important role in their formation ( Lee & Wyllie, 1998). Experimental data on element partitioning between immiscible silicate and carbonate liquids have also been used to assess the composition of mantle carbonates and primary carbonate-rich melts. Unfortunately, crustal carbonatites show a wide range in chemical compositions and few workers believe that carbonatites reflect liquid compositions. The present work is based on laser ablation ICP-MS analyses for a large number of trace elements in carbonates and coexisting silicate minerals in mantle peridotite xenoliths in alkali basaltic rocks from Spitsbergen and Mongolia. (1996) reported high contents of Sr and Ba in carbonates and S in clinopyroxene in these xenoliths determined in situ by proton microprobe analyses. They found enrichments in light rare earth elements (LREE) and Sr relative to heavy rare earth elements (HREE) and high field strength elements (HFSE) in plots normalized to their abundances in chondrites or primitive mantle (PM), and concluded that these trace element signatures are characteristic of the carbonate material in the xenoliths Ionov et al. (1993) provided analyses of whole-rock carbonate-bearing peridotite xenoliths from Spitsbergen and of acid leaches from these rocks done by solution inductively coupled plasma mass spectrometry (ICP-MS). Nonmatrix-matched calibration standards have been successively used for quantitative carbonate analysis by Feng (1994), who employed the NIST 612 silicate glass as a calibration standard to determine Sr, Y, Ba and REE in calcite and dolomite.In-run signal intensity for indicative major and minor elements was monitored during analysis of small mineral grains and glass pockets ( Fig. Details of ICP-MS and laser operating conditions have been published by Norman et al. Analytical precision is ≤5% at the ppm lev. For carbonate and silicate glass, detection limits were higher when a low-energy, defocused beam was used. Estimates of major element contents (Si, Al, Mg) obtained by LAM–ICP-MS agree well with electron microprobe (EMP) analyses of the same minerals. Rb and Ba were monitored for small clinopyroxene grains to check for contamination by silicate glass. Ablation of carbonates was aborted when signal intensity for Al, Si, Cr or Ni increased well above background levels, and carbonate analyses with considerable levels of these elements were discarded. Cengage book instructor siteDetailed data on petrography and major element composition of the Spitsbergen xenoliths (including the samples in this study) have already been published ( Ionov et al., 1996). Table 1 gives a summar of petrography, mg–number of olivine, Cr 2O 3 content of spinel and estimates of equilibration temperatures for these samples. Sample DescriptionTrace element data were obtained for three spinel lherzolite xenoliths from NW Spitsbergen an one spinel lherzolite xenolith from SE Mongolia (Dariganga). Some differences may be due to significant chemical zoning and grain-to-grain variations in carbonate and carbonate-related clinopyroxene ( Ionov et al., 1996). Average contents of Sr, Y and Zr determine by PIXE in primary and carbonate-related clinopyroxene in the same samples are largely within 15% of corresponding LAM–ICP-MS data. The pockets typically make up ≤ 2–3% of the rock and are 0.2–2 mm in size. These pockets also contain small (<100 μm) euhedral grains of clinopyroxene and olivine, Fe–Ni sulphides and (Na,Al)–rich silicate glass with microphenocrysts of Cr-rich spinel ( Fig. Amphibole is more abundant and its grains are larger in xenolith 21-6, which also contains rare equant grains of apatit 0.1–0.5 mm in size.Carbonates analysed in this work occur in fine-grained pockets replacing minerals of host peridotite, most commonly spinel, orthopyroxene and amphibole ( Ionov et al., 1996). Xenolith 4-90-9 contains rare, small (0.5–1 mm) amphibole grains. Typical grain sizes range from 2–6 mm for olivine and orthopyroxene to 1–2 mm for clinopyroxene and spinel. Dark spots in minerals in (a) and (b) are laser ablation pits. (a–c) Sample 4-36-90 from Spitsbergen field of view is 1.2 mm. Carbonate in xenolith BY-44 from SE Mongolia occurs in fine-grained pockets and also as interstitial grains texturally equilibrated with the host lherzolite.Photomicrographs of carbonate-bearing pockets in peridotite xenoliths. The carbonates in the pockets occur as mosaic aggregates with smooth curvilinear boundaries made up of interlocking grains 20–50 μm in size these aggregates contain no silicate or oxide minerals ( Fig. (b) Same pocket as in (a) in reflected light: dark (Na,Al)-rich silicate glass (gl) with bright microlites of Cr-spinel (sp) and small sulphide droplets encloses euhedral clinopyroxene, olivine and small round carbonate aggregates adjacent large mosaic carbonate segregation contains no silicate or oxide minerals.
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