Diamondiferous kimberlites in central India synchronous with Deccan flood basalts

Lehmann, Bernd; Burgess, R.; Frei, Dirk; Belyatsky, B. V.; Mainkar, Datta; Rao, N. V. Chalapathi; Heaman, Larry M.

doi:10.1016/j.epsl.2009.12.014

Cited by 97 publications

(30 citation statements)

References 34 publications

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“…A detailed investigation on global cratons indicates that lithospheric thinning of the cratonic mantle is commonly related to mantle plumes. For example, it has been suggested that lithospheric thinning in the India Craton was related to the Reunion mantle plume, which also led to the eruption of Deccan flood basalts [52]. Despite the general occurrence of lithospheric thinning, the cratonic nature is still preserved in most cratons, without development of strong intracrustal ductile deformation and extensive magmatic activities.…”

Section: Mechanism Of the Ncc Destructionmentioning

confidence: 98%

Timing, scale and mechanism of the destruction of the North China Craton

Zhu

Chen

et al. 2011

Sci. China Earth Sci.

589

364

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The North China Craton (NCC) is a classical example of ancient destroyed cratons. Since the initiation of the North China Craton Destruction Project by the National Natural Science Foundation of China, numerous studies have been conducted on the timing, scale, and mechanism of this destruction through combined interdisciplinary research. Available data suggest that the destruction occurred mainly in the eastern NCC, whereas the western NCC was only locally modified. The sedimentation, magmatic activities and structural deformation after cratonization at ~1.8 Ga indicate that the NCC destruction took place in the Mesozoic with a peak age of ca 125 Ma. A global comparison suggests that most cratons on Earth are not destroyed, although they have commonly experienced lithospheric thinning; destruction is likely to occur only when the craton has been disturbed by oceanic subduction. The destruction of the NCC was coincident with globally active plate tectonics and high mantle temperatures during the Cretaceous. The subducted Pacific slab destabilized mantle convection beneath the eastern NCC, which resulted in cratonic destruction in the eastern NCC. Delamination and/or thermal-mechanical-chemical erosion resulted from the destabilization of mantle convection. timing, scale and mechanism, craton destruction, North China Craton Citation:Zhu R X, Chen L, Wu F Y, et al. Timing, scale and mechanism of the destruction

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Section: Mechanism Of the Ncc Destructionmentioning

confidence: 98%

Timing, scale and mechanism of the destruction of the North China Craton

Zhu

Chen

et al. 2011

Sci. China Earth Sci.

589

364

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“…The highly diamondiferous nature of the Cretaceous Group II kimberlites (Lehmann et al 2010;Chalapathi Rao et al 2011a) from the nearby (~150 km) Mainpur kimberlite field of the Bastar craton demonstrates the presence of diamondiferous roots in this domain of peninsular India at the time of eruption of the Tokapal kimberlite. If so, an important question arises: Why the Tokapal kimberlite lacks diamond, garnet and other indicator minerals, even though some of the spinel macrocrysts were obviously derived from the diamond stability field?…”

Section: Discussionmentioning

confidence: 96%

Diamond-facies chrome spinel from the Tokapal kimberlite, Indrāvati basin, central India and its petrological significance

et al. 2012

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Widespread and abundant spinel is the only primary mineral of petrogenetic significance preserved in the hydrothermally altered, crater-facies, Neoproterozoic (≥620 Ma) Tokapal kimberlite pipe that intruded the Indrā-vati basin, Bastar craton, Central India. Two distinct spinel populations occur: (i) finer-grained (<50 μm) microcrysts which are zoned from titaniferous magnesiochromitechromite to magnetite; and (ii) larger macrocrysts (>400 μm) with cores having distinctly chromium-rich (Cr 2 O 3 up to 63.67 wt%), and TiO 2 -poor (<0.68 wt%) compositions. Based on their morphology and chemical composition the macrocrysts are inferred to be disaggregated mantle xenocrysts and their compositional range extends well into the diamond stability field. However, the reported absence of diamond and other indicator minerals (such as pyrope garnet, chrome diopside and magnesian ilmenite) in the Tokapal pipe is intriguing since diamondiferous cratonic roots are indeed preserved in the Bastar craton, and also the kimberlite itself was derived from a similar source region(s) as that of the well-known diamondiferous Mesoproterozoic (ca. 1,100 Ma) kimberlites from Wajrakarur, Dharwar craton, southern India. Given the large areal extent (>550 ha) of kimberlite, there is a possibility that it contains diamonds but they were not recovered during the sampling. Alternately, highly oxidising conditions imparted by the metasomatic fluids/melts derived from (i) asthenosphere-lithosphere interaction, or (ii) the kimberlite itself might have played an important role in the destruction of diamond, and other indicator minerals.

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“…The Chelima lamproite in the Nallamalai field of the Dharwar Craton, which has yielded a 40 Ar/ 39 Ar phlogopite age of 1,417 My (Chalapathi Rao et al 1999), is significantly older than the Nuapada lamproites. The kimberlites of the Bastar Craton, which have been dated as 65 My old (Lehmann et al 2010), are much younger than the Nuapada lamproites. Sum (X site) …”

Section: Ar/ 39 Ar Datingmentioning

confidence: 99%

Petrology of Lamproites from the Nuapada Lamproite Field, Bastar Craton, India

Sahu

Gupta²,

Patel³

et al. 2013

Proceedings of 10th International Kimberlite Conference

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This work presents the first mineralogical, geochemical and 40 Ar/ 39 Ar geochronological data on hypabyssal facies lamproites near Kalmidadar and Darlimunda in the Nuapada Lamproite Field of the Bastar Craton. The Kalmidadar lamproite is a diamondiferous intrusion with surface dimension of *320 m 9 160 m, whereas the Darlimunda lamproite is a dyke swarm comprising clusters of several narrow (\5 m wide) and elongated bodies. Indicator mineral suite around the Kalmidadar lamproite is marked by abundance of Cr-spinel, rarity of garnet and absence of Cr-diopside and picroilmenite. Mineralogically, the Kalmidadar lamproite comprises phenocrysts of olivine (pseudomorphed by calcite and talc) and microphenocrysts of phlogopite set in a groundmass of chlorite and calcite. The phlogopite is Ti rich (5.4-7.4 wt % TiO 2 ), and the relationship between its Ti content and octahedral site deficiency indicates two substitution mechanisms, viz. Ti + ' $ 2 Mg and Ti ? 2Al $ Mg ? 2Si. The Darlimunda lamproites have undergone pervasive hydrothermal and/or deuteric alteration, which has resulted in complete chloritisation of phlogopite and extensive silicification of the rocks. Tiny grains of rutile and apatite are commonly scattered in the groundmass of both Kalmidadar and Darlimunda lamproites. The Nuapada lamproites have high contents of compatible elements such as V, Cr and Ni and of incompatible elements such as Ba, Zr, Nb and Hf. They also show high abundance of REE and enrichment in LREE relative to HREE. The incompatible element distribution patterns of the lamproites are marked by Nb, Sr, P, Hf and Zr anomalies relative to REE. The observed petrological and geochemical characteristics of the Nuapada lamproites are consistent with the derivation of the magma from a metasomatised subcontinental lithospheric mantle source. Whole-rock 40 Ar/ 39 Ar isotopic data yields an age of 1055 ± 10 Ma for the Nuapada lamproites.

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Diamondiferous kimberlites in central India synchronous with Deccan flood basalts

Cited by 97 publications

References 34 publications

Timing, scale and mechanism of the destruction of the North China Craton

Timing, scale and mechanism of the destruction of the North China Craton

Diamond-facies chrome spinel from the Tokapal kimberlite, Indrāvati basin, central India and its petrological significance

Petrology of Lamproites from the Nuapada Lamproite Field, Bastar Craton, India

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