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Using of clinopyroxene thermobarometry for the eclogites and omphacite diamond inclusions of Yakutian and worldwide kimberlites .. Igor Ashchepkov (1), Zdislav Spetsius (2), Hilary Downes (3), Alla Logvinova (1), Subramanian Ravi (4), T heodoros Ntaflos (5).

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Using of clinopyroxenethermobarometry for the eclogites and omphacite

diamond inclusions of Yakutian and worldwide kimberlites ..

Igor Ashchepkov (1), ZdislavSpetsius (2), Hilary Downes (3), AllaLogvinova (1), Subramanian Ravi (4), TheodorosNtaflos (5).

Sobolev Institute of Geology and Mineralogy SD RAS, Koptyugave 3, Novosibirsk, Russia

Alrosa Stock Company, Lenina str. 6 Mirny, Russia, (3) Birkbeck College, University of London, UK,

(4) Geological Survey of India, Bandlaguda Complex, Hyderabad 500068, Ind, (5) Vienna University, A-1090Vienna, Austria

Fig. 1. PTXFO2 estimates for the minerals from xenocrysts and xenoliths from Udachnaya pipe, Daldyn field. Fe# is calculate Fe number of olivines, coexisting with Garnets, pyroxenes chromite and ilmenites.

1. Clinopyroxene thermobarometry ToC (Nimis and Taylor, 2000) - P(GPa) (Ashchepkov, 2003) for xenoliths (Boyd et al., 1997; Pokhilenko et al., 2000; Malygina et al., 2005; Pokhilenko et al., 2007). 2. The same for Cr-diopsides from heavy mineral separates. 3. The same for pyroxenites (Kuligin, 1997). 4. The same for common eclogites. 5. The same for diamond inclusions of eclogite affinity (Beard et al., 1996; Snyder et al .,1997; Taylor et al., 2003). 6. The same for diamond inclusions peridotite affinity (Sobolev et al., 1997; 2003; 2004; Logvinova et al., 2005). 7. The same for diamond eclogites (Jacob et al., 1999; etc). 8. Orthopyroxene thermobarometry: ToC (Brey, Kohler, 1990) - P(GPa) (McGregor, 1974) for peridotites. 9. The same for diamond inclusions. 10. Garnet thermobarometry for peridotites (Ashchepkov, 2006). 11. The same for garnets from heavy mineral separates. 12. The same for diamond inclusions. 13. Cr-spinel thermobarometry: ToC (Taylor et al., 1998) - P(GPa) (Ashchepkov, Vishnyakova, 2006) for xenoliths. 14. The same for grains from heavy mineral separates; 15. the same for diamond inclusions. 16. Ilmenite thermobarometry: ToC (Taylor et al., 1998) – P(GPa) (Ashchepkov, Vishnyakova, 2006) for grains from heavy mineral separates. 17. The same for ilmenites from xenoliths



  • Modified clinopyroxenethermobarometry (Ashchepkov et al., 2010) in combination with (Krogh, 1988) or (Nimis, Taylor, 2000) thermometers checked using 570 published runs in eclogite system clarified position of eclogitesin Siberian and Worldwide SCLM (Ashchepkov et al, 2010; 2012; 2013). In Siberia Fe- eclogites related to Fe- basalts or TTG cumulates sediments and are found in the middle pyroxenite layer formed in Early Archean when eclogites can’t be subducted and were remelted in near 100 -130 km (3.5-4GPa) (Udachnaya, Mir, Prianabarie). In Middle and late Archean they locate _5 GPa forming several deeper levels (Udachnaya). Hi- Mg arc cumulates (Horodyskyj ea, 2007) are related to the different depth and relate to Low-T geotherms starting from 7.5 to 4 GPa. Diamond omphacite inclusions from melt metasomatizedeclogites or protokimberlite cumulates often trace HT geotherm. In Siberia eclogites positions in SCLM differ. In Magan terrain abundant eclogites of varying (Mg’) correspond to different types. Majority (4-5 GPa, MaloBotupbinsky and Khramai) form several trends decreasing P- Fe corresponding to melt differentiation and reaction with kimberlites referring to high –T conditions. The 3.0-3.5 GPa lens traced by both high and low-Fe eclogites. Cold low Fe type are probably referring to subduction type eclogites (LT) but HT -to protokimberlite crystallization .
  • In West Daldyn (Alakit) terrain eclogites locate in middle SCLM part. In Daldyn West they are distributed in all section. In Nakyn field (Markhaterrane) Fe-rich eclogites dominate in lower SCLM like in Upper Muna fields. In northern Siberian craton part in Hapchan (Kuoyka) and Birekte terrain most eclogites belong to middle part. Those from Upper part may corresponds to TTG cumulates. Abundant eclogite diamond inclusions suggest that they should be also in the low SCLM.
  • Proterozoickimberlites commonly carry hot eclogites from middle part like in Wajrakarur field (KL-4) in India where Ca- rich eclogites and grospydites reflect reactions of Ca- rich mater with mantle peridotites. In South Africa Proterozoic Roberts Victor and Premier kimberlites HT eclogite and diamond inclusions mostly came from deeper part of SCLM 5.5-4 GPa and show Fe rising upward in section. Mzkimberlites in Lesotho carry omphacites from 5.5-4.0 GPa showing several P- Fe # trends. In Namibia diamond inclusions 5.5-7.5 GPa show Fe# rise with depth. In Angola eclogite lens is found at 5-6 GPa (Ashchepkov et al., 2013).
  • In Wyoming craton Devonian kimberlites carry eclogites from upper SCLM forming three clusters: near Mohoat Gar-Sp boundary and Fe 3.5-2.5 interval. Fe – enriched varieties locate 4.5-5 GPa interval and Mg rich at 7-6 GPa.
  • In Slave craton Mg eclogites (Heaman ea, 2006) correspond to LSCLM while Fe-rich are from middle part. In Karelian cratoneclogites of varying Fe# are in LSCLM. Spider diagrams of eclogiteclinopyroxenes demonstrates four types of patterns. Smooth rounded one corresponds to protokimberlites. Flatter or inclined with HFSE troughs and U, Pb peaks are of MORB. The jugged highly inclined patterns refer to TTG cumulates showing LILE enrichments and HFSE through. TRE of metasomaticclinopyroxeneseclogites are variable . RFBR 11-05-00060


Trace elements

Eclogites Udachnaya

Pkbar and To correlations

Of experimental and

Calculated values

North America


Trace elements

Eclogites KL4 India