Nature of diversity of diamonds in kimberlites

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Abstract

The one-way evolution of inclusions in diamonds and its ultra-long duration (more than 2.8 Ga) provide evidence that the crystallization of diamonds took place from the fractionated peridotitic layer in the global magmatic ocean. Diamonds were formed as a result of accumulation of carbon in residual kimberlitic melts. The increment of SiO2 concentration in the melts caused increase in its viscosity, decrease of diffusion velocity and degree of carbon oversaturation. These resulted that the layered diamond crystallization mode was changed by the radial one, diamond octahedrons transformed into rhombic dodecahedrons and cubes, varied sculptures were created on diamond crystals faces.

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About the authors

Vladimir S. Shkodzinskiy

Diamond and Precious Metal Geology Institute of Siberian Branch Russian Academy of Sciences

Author for correspondence.
Email: shkodzinskiy@diamond.ysn.ru
ORCID iD: 0000-0001-7749-1264
SPIN-code: 7797-7586

doctor of geology, research worker

Russian Federation, 677000, Yakutsk, Lenin st. 39

Viktor V. Beskrovanov

North-Eastern Federal University named after M.K. Ammosov

Email: vv.beskrovanov@s-vfu.ru

doctor of geology, professor

Russian Federation, Yakutsk, Kulakovskogo st., 48

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Supplementary files

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2. Fig. 1. Average isotope ages of mantle rocks from xenoliths in kimberlites (line ПО), inclusions in diamonds (line ВА), average temperature of formation of mantle xenoliths under 5 GPa pressure (line T), and average MgO content in rocks (line MgO).

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3. Fig. 2. MgO–CaO ratio in mantle rocks. Lines outline fields of compositions of xenoliths in kimberlites (В — websterite, Г — harzburgite, Д — dunite, Л — lherzolite, Э — eclogite) and fields of magmatic rocks (К — kimberlites, Ка — carbonatites, Ла — lamproites). Continuous and dashed arrows show the evolution of cumulate and residual melt composition respectively (Shkodzinskiy, 2015).

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4. Fig. 3. Summary contents of minor components in different octahedrons of diamond: colorless (ОБ), with trigonal growth layers (ОТ), with ditrigonal growth layers (ОД), with splintery sculpture (ОЗ), light-brown (СОП) and dark-brown (ТОП) with polycentrical faces; the same in aggregates (А) and cabonado (К). Composed after data of Argunov, 2005.

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5. Fig. 4. Correlation between the value of specific X-ray luminescence (I/m) and morphology of diamond crystals, their color and photoluminescence, the nitrogen content, isotopic composition of carbon, formation temperature, their age and composition of the melt while crystallization. Points show average values of I/m while formation of diamonds of different morphology, coloring, etc. Rows Ка and Ла are crystals in kimberlites with, respectively, carbonatite (Ка) and lamproite (Ла) trends of differentiation, the intermediate row — crystals occurring in various kimberlites.

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6. Fig. 5. Dependence of the fraction of resorbed diamond crystals (K) on the CO2 content in kimberlites. Composed after data of Argunov, 2005.

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7. Fig. 6. Dependence of the mean weight of rounded diamond crystals (M) on their fraction in kimberlite pipes of Yakutia (1), in placers at the area of kimberlite fields (2), in placers far distanced from kimberlite pipes of Yakutia (3), in placers of Vishersky district at the Urals (4). Composed after data of Argunov, 2005, and Grakhanov et al., 2007.

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8. Fig. 7. Scheme of solidification of the magmatic ocean and crystallization conditions of different types of diamonds in the peridotite layer: octahedrons (О, 1), dodecahedroids (Д, 2), cubes (К, 2), aggregates (Аг, 3), intermediate varieties (П, 1), varieties I—VIII by Orlov (1973), and giant diamonds (Ги).

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