Accepted Manuscript Sheared peridotite xenolith from the V. Grib Kimberlite Pipe, Arkhangelsk Diamond Province, Russia: Texture, composition, and origin A.V. Kargin, L.V. Sazonova, A.A. Nosova, V.A. Pervov, E.V. Minevrina, V.A. Chvostikov, J.P. Burmiy PII:
S1674-9871(16)30017-2
DOI:
10.1016/j.gsf.2016.03.001
Reference:
GSF 436
To appear in:
Geoscience Frontiers
Received Date: 21 August 2015 Revised Date:
15 February 2016
Accepted Date: 1 March 2016
Please cite this article as: Kargin, A.V., Sazonova, L.V., Nosova, A.A., Pervov, V.A., Minevrina, E.V., Chvostikov, V.A., Burmiy, J.P., Sheared peridotite xenolith from the V. Grib Kimberlite Pipe, Arkhangelsk Diamond Province, Russia: Texture, composition, and origin, Geoscience Frontiers (2016), doi: 10.1016/ j.gsf.2016.03.001. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.
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ACCEPTED MANUSCRIPT Sheared peridotite xenolith from the V. Grib Kimberlite Pipe, Arkhangelsk
Diamond Province, Russia: Texture, composition, and origin A.V. Kargin a,∗, L.V. Sazonova a,b, A.A. Nosova a, V.A. Pervov c, E.V. Minevrina a, V.A. Chvostikov d, J.P. Burmiy d a
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Institute of Geology of Ore Deposits, Petrography, Mineralogy, and Geochemistry, Russian Academy of Sciences (IGEM RAS), Moscow, Russia b Lomonosov Moscow State University, Moscow, Russia c Departamento de Geologia, Sociedade Mineira de Catoca, Repblica de Angola, Lunda Sul, Catoca d Institute of Technological Problems of Microelectronics and Ultrapure Materials, Russian Academy of Sciences, Chernogolovka, Russia
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*Corresponding author Email addresses:
[email protected] (A. Kargin),
[email protected] (L. Sazonova),
[email protected] (A. Nosova),
[email protected] (V. Pervov)
Abstract
The petrography and mineral composition of a mantle-derived garnet peridotite xenolith from the V. Grib kimberlite pipe (Arkhangelsk Diamond Province, Russia) was studied. Based on petrographic characteristics, the peridotite xenolith reflects a sheared peridotite. The sheared peridotite experienced a complex evolution with formation of three main mineral assemblages:
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(1) a relict harzburgite assemblage consist of olivine and orthopyroxene porphyroclasts and cores of garnet grains (Gar1) with sinusoidal rare earth elements (REE) chondrite C1 normalized patterns; (2) a neoblastic olivine and orthopyroxene assemblage; (3) the last assemblage associated with the formation of clinopyroxene and garnet marginal zones (Gar2).Major and
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trace element compositions of olivine, orthopyroxene, clinopyroxene and garnet indicate that both the neoblast and clinopyroxene-Gar2 mineral assemblages were in equilibrium with a high
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Fe-Ti carbonate-silicate metasomatic agent. The nature of the metasomatic agent was estimated based on high field strength elements (HFSE) composition of olivine neoblasts, the garnetclinopyroxene equilibrium condition and calculated by REE-composition of Gar2 and clinopyroxene. All these evidences indicate that the agent was a high temperature carbonatesilicate melt that is geochemically linked to the formation of the protokimberlite melt. Keywords: sheared peridotite, mantle metasomatism, kimberlite, olivine, garnet, clinopyroxene
1.
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Introduction
Sheared peridotite is a garnet- and spinel-bearing rock with distinct ductile deformation features. It contains large porphyroclasts embedded in a deformed and recrystallized matrix of neoblasts and shows mainly porphyroclastic–mosaic to blastomylonitic textures (Harte, 1977; Ionov et al., 2010).
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Sheared peridotite xenoliths are common within kimberlites. Based on P–T estimates, they are considered the deepest mantle nodules found in kimberlites. Kennedy et al. (2002) reviewed early models of their genesis, and at present, there are two main opinions on their origin:
these rocks are derived from shear zones concentrating melt and fluid flows in the
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(1)
transitional area between the lithosphere and asthenosphere and are resulted from the motion of
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lithospheric plates (Boyd and Nixon, 1975; Kennedy et al., 2002) and others; they are widespread at the base of the lithosphere beneath Archean cratons (O’Reilly and Griffin, 2010); (2)
they are metasomatic rocks formed along the fractures conducting kimberlite
melts and only locally occur at various levels of the lithospheric mantle (Moore and Lock, 2001; Ionov et al., 2010; Katayama et al., 2011; Agashev et al., 2013); trace-element chemistry of
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garnet and clinopyroxene in these rocks indicates their close relation to minerals of the megacrystic assemblage in kimberlites (Burgess and Harte, 2004; Solov’eva et al., 2008). Detailed studies performed for xenoliths of deformed garnet peridotites in kimberlites demonstrate a complex history of their transformation and several stages of mantle
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metasomatism (Harte, 1983; Dawson, 1984; Griffin et al., 1999; O’Reilly and Griffin, 2013). It was demonstrated for xenoliths of deformed peridotites within kimberlites of the Udachnaya
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pipe in Yakutia (Agashev et al., 2013) that at the initial stages the rock could suffer cryptic metasomatism by melt/fluid of carbonatite composition, resulting in LREE enrichment. This process was followed by silicate metasomatism under effect of asthenospheric melts with significant changes of mineralogical and chemical compositions of the deformed peridotites. The mantle processes were concluded by Fe-Ti metasomatism, which was genetically related to the formation of minerals of the megacrystic assemblage and kimberlitic magmas. The majority of petrogenetic models suggest melt or fluid with asthenospheric origin to be metasomatic agents (Ehrenberg, 1979; Burgess and Harte, 2004; Agashev et al., 2006; Solov’eva et al., 2008) and others. However, the composition and nature of these agents are still highly debatable.
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Trace-element features of garnet and clinopyroxene of the megacrystic assemblages implies their affinity to kimberlites, namely, they could be in equilibrium with protokimberlitic melts and fluids (Rawlinson and Dawson, 1979; Burgess and Harte, 2004; Moore and Belousova, 2005; Agashev et al., 2006). Close genetic relation of large porphyroclasts in the deformed peridotites with minerals of the megacrystic assemblage in kimberlites (Burgess and
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Harte, 2004; Solov’eva et al., 2008) may suggest similar models for their origin. Kimberlites from the V. Grib pipe within the Arkhangelsk Diamond Province (ADP) contain numerous unaltered mantle xenoliths (peridotite, eclogite, and diverse deep-seated metasomatites), as well as megacrysts of clinopyroxene, garnet, olivine, phlogopite, and ilmenite (Sablukov et al., 2000; Kostrovitsky et al., 2004; Shchukina et al., 2012, 2015; Afanasiev et al.,
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2013; Golubkova et al., 2013; Sazonova et al., 2015). Sablukov et al. (2000) mentioned some scarce finds of mosaic-porphyroclastic rock varieties (sheared peridotites) among mantle
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xenoliths in kimberlites of the province.
Based on the study of garnet from heavy mineral concentrates, Sablukov et al. (2009) concluded that pyropes from the V. Grib pipe were only moderately affected by mantle processes, such as garnet depletion and high-T melt-related or low-T phlogopite-accompanied metasomatism (in terms of Griffin et al., 1999). Based on the study of garnet peridotite xenoliths,
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Shchukina et al. (2015) also revealed these two types of mantle metasomatism occurred at the base of the lithospheric mantle beneath the V. Grib pipe and suggested a multistage model for these processes involving carbonatitic, picritic and basaltic metasomatic agents.
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Our paper focuses on the major and trace element characteristics of minerals of a deformed peridotite xenolith (Sample Gr-106-664) and garnet megacrysts from the V. Grib
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kimberlite pipe to get insight into the metasomatic processes in the lithospheric mantle beneath this pipe. The aim of our study is to decipher the role of carbonate and silicate components in mantle metasomatism, as well as to unravel the genetic link of metasomatic agents with kimberlite (protokimberlite) melts. Kimberlites and associated alkaline-ultrabasic rocks of the ADP are late Devonian in age
(Sablukov, 1984). The same age was determined for the carbonatite-bearing ultrabasic complexes in the Kola alkaline province located northwestward of the kimberlite province (Arzamastsev and Wu, 2014). Temporal and spatial relations of these provinces give grounds to suggest that they are products of a single tectonothermal event. The study of the role of a carbonate component in the metasomatic reworking of lithospheric mantle and its genetic link
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with kimberlite melts in ADP may provide insight in the formation of large carbonatite-bearing alkaline-ultrabasic provinces. Note that this study continues our previous work devoted to kimberlites of the V. Grib pipe, particularly to olivine porphyroclasts and neoblasts from a deformed peridotite sample
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(Sazonova et al., 2015).
Geological setting
The Arkhangelsk Diamond Province (ADP) is situated on the northern East European craton (Fig. 1). Several fields of kimberlites and related rocks were distinguished within the
Chernoozero
kimberlite
field
(Tretyachenko,
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province. The V. Grib pipe is located in the central part of the ADP and belongs to the 2008).
Petrographic
and
geochemical
characteristics of kimberlite and related rocks of the ADP are described in detail previously
Kononova et al., 2002, 2007;).
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(Beard et al., 1998; Mahotkin et al., 2000; Sablukov et al., 2000; Bogatikov et al., 2001, 2007;
The V. Grib pipe intruded Neoproterozoic sedimentary rocks and is overlain by Carboniferous siliciclastic and carbonate rocks and Quaternary sediments (Fig. 1). It is dated at 372 ± 8 Ma (Rb-Sr five-point whole-rock isochron, Shevchenko (2004)), which coincides with
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dates obtained on most magmatic complexes of the Kola Province (379 ± 5 Ma; Arzamastsev and Wu, 2014), which is located within the Kola Peninsula (Fig. 1). The upper diatreme zone is filled with pyroclastic kimberlite. This kimberlite contains
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abundant fragments and fine material of host Neoproterozoic sedimentary rocks. The majority of the diatreme zone is occupied by massive pyroclastic kimberlite with minor xenogenic material
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(Verichev et al., 2003; Kononova et al., 2007).
Analytical techniques
Detailed petrographic studies of sheared peridotite xenolith were performed using a Jeol
JSM-6480LV scanning electron microscope (Laboratory of local analytical methods of the Faculty of Geology, Moscow State University, Petrology department, Moscow, Russia). Electron images were obtained in the backscattered electron mode. Electron microprobe analysis (EMPA) of garnet, orthopyroxene and clinopyroxene were carried out using Jeol JXA-8200 electron microprobe equipped with five wavelength spectrometers and an energy dispersive system (Institute of Geology of Ore Deposits,
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Petrography, Mineralogy, and Geochemistry Russian Academy of Sciences, Moscow, Russia). Minerals were studied at an accelerating voltage of 20 kV, beam current of 20 ηA, and beam diamter of 1–2 µm. Counting times were 10 s for major elements and 20–40 s for trace elements. The measurements were corrected using the ZAF (JEOL) routine. Standardization for major elements was done using phases of compositions similar to those of the studied minerals.
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Concentration of trace elements (Ti, Cr, Sr, Zr, Ba, Th, Y, Nb, B, Li, Be, REE) in olivine, garnet and clinopyroxene were determined in situ in polished sections by secondary-ion massspectrometry (SIMS) using Cameca IMS ion probe (Institute of Microelectronics of the Russian Academy of Sciences, Yaroslavl, Russia). The relative uncertainties of element contents were no higher than 10% at contents >1 ppm and no higher than 15–20% at contents from 0.1 to 1 ppm.
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The detailed technical description of SIMS is provided in the Supplementary data 1.
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The geochemical study of olivine was carried out by LA-ICP-MS on an X-Series II inductively coupled plasma mass-spectrometer (Institute of the Problems of Microelectronics Technology and Extra Pure Materials Russian Academy of Sciences) using 1400 W plasma power, gas flow rates of 13 L/min and 0.90 L/min for the sample and Ar-auxiliary gas, respectively; 0.6 L/min for the He carrier gas, and 0.6 L/min for He-Ar mixture, and resolution of 0.4 and 0.8 M. A UP266 MACRO laser microprobe coupled to the mass spectrometer
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operated at a wavelength of 266 µm, a pulse frequency up to 10 Hz, pulse intensity up to 5 mJ, counting time of 4 ns, and crater diameter from 30 to 300 µm. The geochemical composition of garnet and clinopyroxene was also analyzed by LA-
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ICP-MS on an X-Series II coupled with NWR-213 laser ablation sampler (Laboratory of mineral analysis of the Institute of Geology of Ore Deposits, Petrography, Mineralogy, and
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Geochemistry Russian Academy of Sciences, Moscow, Russia). The measurement errors were 1–3% for REE, U, Th, and Pb, and 30–50% for Ni, Cu, Zn, and Co. The detailed technical description of LA-ICP-MS is provided in the Supplementary data 1. We used two approaches to estimate T and P parameters for mineral equilibria in the rock
studied. The first one assumed that all minerals of peridotite are in equilibrium. The mineral compositions meeting the equilibrium criteria suggested by Nimis and Grütter (2010) were used to calculate T and P by Opx-Cpx thermometer (Taylor, 1998) and Gar-Opx barometer (Nickel and Green, 1985). In the second approach, P–T parameters were calculated separately for the relict harzburgitic assemblage (the central parts of the olivine and orthopyroxene porphyroclasts and garnet Gar1) and for pairs of clinopyroxene and outer zones of garnet grains (Gar2). We used Opx and Ol thermometers (Brey and Kohler, 1990; De Hoog et al., 2010) and Opx-Gar
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barometers (MacGregor, 1974; Brey and Kohler, 1990), which do not require equilibrium with Cpx. T and P data for experimental and natural systems are reproduced with uncertainties of ± 30 °C and ± 2.2 kb (Brey and Kohler, 1990; De Hoog et al., 2010). The temperature of equilibrium of clinopyroxene and outer zones of the garnet grains (Gar2) were determined using Cpx-Gar thermometers (Ellis and Green, 1979; Powell, 1985;
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Krogh, 1988), which fit well to experimental data at T=1150–1200°C (Nakamura and Hirajima, 2005). The pressure was assumed at 60 and 40 kb according to values estimated at 3.7–6.8 GPa for crystallization of Cpx megacryst in kimberlite of the V. Grib pipe (Kostrovitsky et al., 2004; Golubkova et al., 2013). The calculation was performed with the PTEXL code created in the mid-1990s by Thomas Kohler, maintained and modified then by Andrei Girnis (personal
4.
Petrography
4.1.
Sheared peridotite
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communication).
The xenolith of sheared garnet peridotite is angular in shape, approximately 10 cm × 15 cm in size (Fig. 2a). It is weakly altered by secondary processes. The xenolith is coated with a rim (up to 1 cm thick) of fine-grained kimberlite, which also penetrates into the peridotite nodule
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along thin fractures.
The xenolith consists of olivine porphyroclasts (∼ 35 vol.%), olivine neoblasts (∼ 35 vol.%), orthopyroxene (∼10 vol.%), clinopyroxene (∼15 vol.%), garnet (∼5 vol.%), and accessory
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ilmenite and titanomagnetite. Phlogopite and chrome spinel are subordinate. The sheared peridotite shows intense ductile deformations with porphyroclastic, fine-grained mosaic, locally
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lenticular-banded textures (Fig. 2b). Based on structural-textural features, this xenolith may be ascribed to the porphyroclastic type after Harte (1977) and mosaic type characterized by olivine and orthopyroxene porphyroclasts enclosed in an olivine-rich polygonal matrix after (Baptiste et al., 2012).
4.1.1. Olivine
Olivine forms two types of grains. The first type (around 50% of all olivine) is represented by large (from 1 to 7–10 mm) relict equant-lenticular porphyroclasts, which have clear signs of ductile deformations (intracrystalline sliding) such as deformation lamellae (Fig. 2b–c) and blocky extinction. The lamellae are visible in cross polarized light by a slight change in birefringence across them. The lamellae represent the active slip plane in the deformed olivine (Raleigh, 1968). The grains of the second type are fine (up to 0.1 mm) weakly rounded olivine
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neoblasts, which form a mosaic matrix around large porphyroclasts (Fig. 2b). Serpentine is developed along fractures in porphyroclasts and contacts of fine grains. 4.1.2. Orthopyroxene Orthopyroxene (1–5 mm across) forms irregularly-shaped isometric grains evenly distributed over the rock and is only locally grouped in patches or lenticles. Under stress effects,
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the mineral acquires elongated shape and locally displays kink banding structure, it is grinded and recrystallized into the finest neoblast aggregate along margins and fractures (Fig. 2d). 4.1.3. Clinopyroxene
Clinopyroxene (1–3 mm across) forms polycrystalline aggregates and separate grains of
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irregular shape, it is developed in interstices between orthopyroxene and olivine. In many cases clinopyroxene partially replaces orthopyroxene, and orthopyroxene relicts are preserved (Fig. 2d
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and 2e). Distinct deformation features (kink bands or deformation lamellae) are not seen in clinopyroxene. Thus, this mineral crystallized later than olivine and orthopyroxene. 4.1.4. Garnet
Garnet is observed as strongly fractured equant grains up to 5–7 mm across with smoothed edges and zoned structure. Inner zones (Gar1) occupy 80–95%. Outer zones (Gar2) are
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patchy with embayed outlines and sharp boundaries (Fig. 2f); more rarely the boundaries between the zones are blurred and gradual. Garnet is rimmed by a narrow fringe consisting of phlogopite, Cr-spinel, and subordinate carbonate. 4.2.
Garnet megacryst
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Garnet megacrysts are rounded or ellipsoidal, up to 2–3 cm in size, and generally orange in color. In many cases, garnet megacrysts show evidence of intense fragmentation and
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mylonitization. Phlogopite and carbonate locally exist in the megacryst fractures.
Results
The representative major and trace element compositions of olivine, orthopyroxene,
clinopyroxene and garnet, from peridotite xenoliths and garnet megacrysts are provided in Tables 1–3. The full data set is given in Supplementary data 2. 5.1.
Garnet megacryst Garnet (Pyr0.72−0.78 Alm0.12−0.14 Gros0.04−0.08 Adr0.04−0.08) is comparable with Cr-poor garnet
megacrysts from kimberlite by Cr2O3 (2.28–3.24 wt.%), CaO (3.18–5.60 wt.%), and TiO2 (0.53–
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1.18 wt.%) contents (Table 1) and corresponds to the type G1 megacryst by the Grütter et al. (2004) classification scheme (Fig. 3). The Mg# value is 0.81–0.83. Garnets from the Cr-poor megacryst suite have an HREE-enriched plateau at 6–10 times chondrite values, with LREE and MREE rising smoothly to the plateau from 0.02 to 0.1 times chondrite values for La (Fig. 4a). Megacrysts have strong enrichment in HFSE relative to REE
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contents (Fig. 4b). These are typical profiles and concentrations for many Cr-poor garnet megacrysts from kimberlites. 5.2.
Mineral chemistry of the sheared peridotite
5.2.1. Olivine
is presented in (Sazonova et al., 2015).
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Chemical composition of olivine porphyroclasts and neoblasts studied in detail by EMPA
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Porphyroclasts have Mg# from 92.8 to 90.7, this value normally varies within a narrow interval for individual porphyroclasts (91.9 to 90.7 was the maximum range determined). The Ti content in large porphyroclasts (7–10 mm in size) widely varies from a few tens of ppm to 250 ppm, averaging 135 ± 58 ppm. The distribution of Ti contents along the sections crossing the grains is distinctly U-shaped in all porphyroclasts studied with Ti enrichment to the grain
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boundaries (Fig. 5). However, consistently symmetrical Mg# distribution has not been found, and this value gradually increases along the demonstrated profile. Neoblasts are less magnesian with average Mg# = 89.6 ± 0.7 and high Ti contents of 244 ± 56 ppm. As compared to porphyroclasts, the neoblasts are richer in Mn, Zn, V and poorer in Ni
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5.2.2. Garnet
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and Cr (Table 2).
Inner zones of the garnet grains (Gar1) are composed of pyrope (Pyr0.69−0.75 Alm0.09−0.15
Gros0.10−0.15 Adr0−0.05) with high Cr2O3 (5.96–6.98 wt.%) and CaO (5.61–6.03 wt.%) at Mg# = 0.82–0.86 and low TiO2 (0.05–0.32 wt.%) contents (Table 1). In the CaO–Cr2O3 diagram (Fig. 3), Gar1 corresponds to the G9 type from garnet lherzolite (Grütter et al., 2004). The REE distribution patterns of Gar1 (Fig. 4a) show distinct sinusoidal shape at (Sm/Dy)n >1 and (Dy/Yb)n 0.7 wt.%), could reflect the impact of high-temperature melt-related metasomatism (Griffin et al., 1999) most likely of essentially carbonate nature (Sokol et al., 2013). Garnets with high LREE, Ti, and Zr contents were also found in a xenolith of deformed
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peridotite in kimberlite of the Udachnaya pipe (Sample 00-92) Solov’eva et al. (2008). This sample also contains clinopyroxene with compositions similar to those of our deformed peridotite sample (Fig. 8c–d). Solov’eva et al. (2008) suggested that deformed peridotites originated by penetration of the asthenospheric material through the matrix accompanied by
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fractional crystallization. The LREE enrichment of marginal garnet zones can be accounted for by magmatic fractionation by a model of chromatographic separation.
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Using a model by Burgess and Harte (2004), we can recalculate Gar2 and Cpx
compositions to equilibrium melt compositions and estimate the nature of the metasomatic agent. Fig. 13 shows REE spectra for hypothetical asthenospheric silicate melts, which could be in equilibrium with Gar2 and clinopyroxene. Calculations with partition coefficients from Burgess and Harte (2004) revealed that Gar2 and clinopyroxene could be in equilibrium with silicate melts with different REE enrichment levels. The melts equilibrated with Cpx should be poorer in REE as compared to those in equilibrium with Gar2. In this case, in compliance with the Burgess and Harte (2004) model, clinopyroxenes were transformed prior to alteration of the marginal zones of garnet grains (Gar2) by addition of more fractionated melts enriched in LREE. Thus, two stages of metasomatic
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processes should be implied when the later process related to LREE-rich melts did not affect clinopyroxene. It looks doubtful, given the fact that LREE preferentially enter clinopyroxene in equilibrium with silicate melts (see mineral/melt partition coefficients in Burgess and Harte (2004)). To estimate trace-equilibrium of Gar2 and clinopyroxene we compared experimentally garnet-clinopyroxene trace-element
partition
coefficients
Dgar/melt/Dcpx/melt with
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derived
XiGar/XiCpx ratios (Fig. 14), where Xi is the concentration of ith element in mineral. The calculation results are compiled in Table 5.
The XiGar/XiCpx values widely vary depending on the crystallization conditions
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(temperature) and composition of equilibrium melt. Experimental works on melting of the peridotite-carbonate (Dasgupta et al., 2009; Girnis et al., 2013; Kuzyura et al., 2014) and
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eclogite-carbonate (Kuzyura et al., 2010) systems, and carbonate-bearing sediments (Grassi and Schmidt, 2011) revealed that LREE affinity to garnet is higher than to clinopyroxene in the presence of a carbonate matter, in spite of the simultaneous crystallization of clinopyroxene (Table 5). With a temperature decrease (Burgess and Harte, 2004) and increase of silicate component in coexisting melts (Johnson, 1998), LREE are redistributed into clinopyroxene.
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In the case of equilibrium carbonate melt, XiGar/XiCpx ratios for high-field strength elements (Th, U, Nb, Ta, Zr, Hf, and Ti) and LREE increase up to values above 1 (Fig. 13a). In turn, the XiGar/XiCpx ratios for Th, U, Nb, La-Eu in minerals that are in equilibrium with essentially silicate basaltic melts (Johnson, 1998), as well as XiGar/XiCpx ratios in natural garnet
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pyroxenites and peridotites are below 1 (Fig. 14a) (see review in Ziberna et al., 2013). The REE XiGar/XiCpx ratios for Gar2 and clinopyroxene are located between the lines of
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Dgar/melt/Dcpx/melt values for silicate and carbonate experimental systems at approximately equal temperatures (Fig. 14b). Our data overlap with data for the deformed peridotite sample in kimberlite of the Udachnaya pipe (Sample 00-92, Solov’eva et al. (2008)). Interpolation of Dgar/melt / Dcpx/melt values between the lines for carbonate (Dasgupta et al., 2009) and silicate (Johnson, 1998) experimental systems shows that XiGar/XiCpx ratios for Ce fall on the lines corresponding to the system with 80-60% carbonate component, and these ratios for La – on the lines for the system with 80-100% carbonate component (Fig. 14b). The XiGar/XiCpx ratios for HFSE show also an intermediate location. The carbonate-rich nature of melt/fluid in equilibrium with Gar2 and clinopyroxene is also supported by redistribution of Zr, Hf, and Ti into garnet. This is expressed in a positive anomaly of XiGar/XiCpx
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ratios for these elements relative to XiGar/XiCpx ratios for REE in Fig. 14c. The XiGar/XiCpx ratios for Zr, Hf, and Ti indicate a possible 20-40% content of carbonate component in equilibrium melts, which is generally consistent with estimate of carbonate proportion in melt/fluid obtained by calculation of composition of the metasomatic agent participating in rock recrystallization during the formation of olivine neoblasts. The comparison of calculated XiGar/XiCpx ratios with experimental garnet/clinopyroxene partition coefficients showed that Gar1 having sinusoidal
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REE distribution pattern and low Ti contents was not in equilibrium with clinopyroxene (Fig. 14). This verifies the above-mentioned conclusion on the relict nature of Gar1.
Thus, the calculation of XiGar/XiCpx ratios for Gar2 and clinopyroxenes from the sheared peridotite confirm that these mineral most probably were in equilibrium with each other and
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carbonate-silicate melt. High HFSE concentrations in Gar2 and similarity in their HREE distribution with that of megacrysts (Fig. 4) may indicate a possible genetic relation of melts
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equilibrated with these minerals (Gar2 and Cpx) with kimberlite magmatism. In order to estimate the composition of the metasomatic agent, we calculated melt compositions that could be in equilibrium with Gar2 and clinopyroxene within the sheared peridotite xenolith. The calculation depends on the mineral/liquid partition coefficients. The conditions estimated above for Gar2-clinopyroxene equilibrium include the presence of
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carbonate melt. Thus, we used mineral/melt partition coefficients obtained by experimental melting of carbonated peridotites under conditions of the base of cratonic lithosphere (Dasgupta et al., 2009).
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Model melts in equilibrium with Gar2 and clinopyroxene have strongly fractionated REE patterns (Fig. 15) and differ in level of LREE abundances (Fig. 15). The REE patterns in melts
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that could be in equilibrium with Gar2 are identical to the composition of kimberlite rim of a pelletal lapillus from the V. Grib kimberlite pipe, while the compositions of melts that could be in equilibrium with clinopyroxenes correspond to 1.5% partial melt from carbonated depleted mantle (Grassi and Schmidt, 2011). In general, the calculated melt composition have parallel REE patterns with REE concentrations of close-to-primary Group I South Africa kimberlites (Becker and Le Roex, 2005) (Fig. 15). These similarities suggest that such equilibrium melts could represent the early portions of protokimberlite melts, prior to fractional crystallization of megacrystic assemblage. The general compositional similarity of clinopyroxene in the rock studied with clinopyroxene from the sheared peridotite xenoliths in kimberlite of the Kaapvaal craton (samples JAG90-19 and JJG1773; Gregoire et al., 2003) also agrees with the model of
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participation of metasomatic agents which were related to the formation of Group I South Africa kimberlites. 6.4.
Sequence of textural and structural transformations and mantle metasomatism The origin of deformed peridotites is still disputable. Their formation only at the base of
the lithosphere, where the rock can suffer deformations due to motion of lithospheric plates
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(Boyd and Nixon, 1975; Kennedy et al., 2002; O’Reilly and Griffin, 2010) does not match geophysical data (Goetze, 1975; Skemer and Karato, 2008). The rock’s derivation from various depths where they could be influenced by deformational and metasomatic processes related to evolution and ascent of kimberlitic melts ( Green and Gueguen, 1974; Moore and Lock, 2001; Ionov et al., 2010; Katayama et al., 2011; Baptiste et al., 2012; Agashev et al., 2013) meets an
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important objection that the ascent of kimberlitic melts could not lead to significant deformations and result in dynamic recrystallization (Arndt et al., 2010; Cordier et al., 2015). A combined
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model comprises transformation by protokimberlitic and basaltic melts of peridotites already deformed in the deep lithosphere closely (within several days) before the entrapment of the rock fragment by kimberlitic melt (Cordier et al., 2015).
The analysis of textural and structural features of the xenolith studied shows that having a mosaic structure it is devoid of lineation, mylonitic matrix, or fluidal texture, and small grains –
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neoblasts are free of any intracrystalline deformation features. Such features can indicate annealing with participation of a fluid, i.e., a stage of fluid-assisted static recrystallization occurred (Baptiste et al., 2012).
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Evidence of deformations, namely, blocky and undulose extinctions, kink bends, deformation lamellae were noted in olivine and orthopyroxene porphyroclasts and do not exist in
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clinopyroxene. Additionally, clinopyroxene locally replaces orthopyroxene neoblasts and exhibits mobile grain boundaries and its irregular amoeboid shapes (Fig. 2d–e). Complete transformation of small olivine fragments to neoblasts with decreased Mg# and
Ni and increased Ti, Mn, V, and some other elements, partial transformation of porphyroclasts with similar trends, and relict Ti diffusion profiles can indicate the peridotitic protolith had suffered metasomatic influence related to Fe-Ti melt/fluid. It is interesting that all neoblasts have similar Mg proportions equal to Fo = 0.89, which coincide with maximum Mg# = 0.89 in all marginal zones of olivines in a fragment of deformed dunite in kimberlites from the Kangamiut region, Greenland (Cordier et al., 2015). These authors believe that orthopyroxene assimilation continues until the percolating melt reaches the
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composition equilibrated with Fo = 0.89, after that the melt becomes saturated in olivine, and crystallization of this mineral begins. This similarity serves as an additional confirmation of metasomatic transformation of the deformed peridotite in our sample. Relationships of deformation features in minerals and their chemical compositions enable us to suggest the following scheme of the peridotite evolution: Harzburgite formation by removing of high-degree melting magmas from primary
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(1)
peridotite and its possible early metasomatic transformations. Large grains of olivine, orthopyroxene, and garnet were formed at this stage. Their remnants were partially preserved in
(2)
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the central parts of olivine and orthopyroxene porphyroclasts and garnet grains (Gar1); Plastic deformations of harzburgite occurred under conditions of the garnet depth
facies. They led to crushing and fragmentation of some large olivine and orthopyroxene grains
(3)
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and to the formation of fine clastic matrix;
Strong heating and recrystallization of the fine clastic matrix under effect of
carbonate-silicate Fe-Ti melt/fluid, formation of olivine and orthopyroxene neoblasts, and cryptic metasomatic transformation of porphyroclasts. The rocks acquired a mosaic-
(4)
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porphyroclastic texture;
Crystallization of clinopyroxene and marginal zones of garnet grains (Gar2) in
equilibrium with silicate-carbonate ±K melt/fluid (probably the portion less contaminated by lithospheric material (orthopyroxene) from the same source provided the melt/fluid at stage 3).
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Phlogopite rims around garnet can also form at this stage. The processes at stages 3 and 4 may occur closely before the entrapment of the rock fragment by kimberlitic melt. This is verified by
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Ti diffusion profiles preserved in the olivine porphyroclasts; (5)
Capture of the xenolith by kimberlite melt and filling of thin fractures in the rock
by kimberlitic material. According to trends of chemical alteration of minerals and comparison of calculated melt composition of stage 4 with megacrysts and kimberlites of the V. Grib pipe (Fig. 15) the melts/fluids of stages 3 and 4 can be considered as protokimberlitic. 6.5.
Carbonate metasomatism related to the Devonian tectonothermal event on the northern
East European craton Late Paleozoic tectonothermal activity on the northeastern East European craton was marked by not only emplacement of the V. Grib kimberlite pipe and other ADP objects, but also by the formation of the Kola alkaline province. According to the last geochronological summary
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(Arzamastsev and Wu, 2014), this province was generated within an interval of around 30 Ma, starting from alkaline-ultrabasic magmatism at 383 ± 7 Ma in the Khibiny and Lavozero calderas to the formation of carbonatite-bearing complexes at 379 ± 7 Ma (Kovdor, Afrikanda, etc.). The age of the V. Grib kimberlite pipe (372 ± 8 Ma) indicates that the kimberlites were formed simultaneously with the early stage magmatism of the Kola alkaline province, which
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produced alkaline ultrabasic, sometimes, carbonatite bearing complexes. With allowance for this fact, the metasomatic transformation of a deformed peridotite xenolith under the effect of high temperature carbonate-silicate melt, which is geochemically similar to a protokimberlite melt, may indicate that lithospheric mantle beneath the northern East European craton was subjected to the global carbonate metasomatism, which led to the formation of large alkaline-ultrabasic
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complexes on the Kola Peninsula and kimberlites within ADP. In this case, the formation of large alkaline provinces and closely spaced kimberlite occurrences may be considered as a
7.
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manifestation of a single tectonothermal event.
Conclusions
Based on petrographic characteristics, the peridotite xenolith reflects a sheared peridotite. The sheared peridotite experienced a complex evolution. Relationships of deformation features
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in minerals and their chemical compositions enable us to suggest the same stages of the peridotite transformation with forming of three main mineral assemblages. There are: (1) relict harzburgite assemblage consists of olivine and orthopyroxene porphyroclasts and cores of garnet grains (Gar1) with sinusoidal REE-normalized patterns; (2) neoblast assemblage of olivine and
(Gar2).
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orthopyroxene; (3) the latest assemblage of clinopyroxene and marginal zones of garnet grains
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The trace-element composition of neoblast assemblage, marginal zones of garnet grains
(Gar2), and clinopyroxene suggests their chemical equilibrium with a high-Fe-Ti metasomatic agent with variable proportions of carbonate and silicate components. The estimate of the metasomatic agent composition is that of a high temperature carbonate-silicate melt with geochemical links to a protokimberlite melt.
8.
Acknowledgments The part of this research was conducted at the Laboratory of Analytical Techniques of
High Spatial Resolution, Department of Petrology, Moscow State University. The purchase of the microprobe was financially supported by the Program for Development MSU. Microprobe studies of minerals were assisted by S. Borisovskii, E. Kovalchuk (IGEM RAS), and N.
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Korotaeva (Lomonosov Moscow State University). We are grateful to V. Karandashev (IPTM RAS) for help in LA-ICP-MS study of olivines; S.G. Simakin and E.V. Potapov (Yaroslavl Branch of the Physicotechnical Institute of RAS) are thanked for SIMS study of garnets and clinopyroxenes, and Ya. Bychkova (IGEM RAS), for LA-ICP-MS study of these minerals. We would further like to thank Karoly Hidas and an anonymous reviewer for extremely thorough
project Nos. 15-05-03778a and 16-05-00298a.
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Doyle, B. J., 2002. Subduction signature for quenched carbonatites from the deep lithosphere. Geology 30 (8), 743–746. Veksler, I. V., Petibon, C., Jenner, G. A., Dorfman, A. M., Dingwell, D. B., 1998. Trace Element Partitioning in Immiscible Silicate-Carbonate Liquid Systems: an Initial Experimental Study Using a Centrifuge Autoclave. Journal of Petrology 39 (11-12), 2095–2104.
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Verichev, E. M., Garanin, V. K., Garanin, K. V., 2003. Geology, composition, formation, and method of prospecting of V. Grib kimberlite pipe (in Russian). In: Problems of Prediction, Search, and Study of Mineral Deposits at the Turn of 21th Century, Voronezh. pp. 43—-48. Ziberna, L., Nimis, P., Zanetti, A., Marzoli, A., Sobolev, N. V., 2013. Metasomatic Processes in the Central Siberian Cratonic Mantle: Evidence from Garnet Xenocrysts from the
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Zagadochnaya Kimberlite. Journal of Petrology 54 (11), 2379–2409.
List of Figures Figure 1
Location of the V. Grib kimberlite pipe within Arkhangelsk Diamond
SC
Province (ADP). (a) ADP location within the northern the East European Craton, after Samsonov et al. (2009): (1–3) Archean blocks: (1) Mesoarchean, (2) Neoarchean, (3) undefined; (4) Belomorian mobile belt; (5–12) Paleoproterozoic structures: (5) initial Paleoproterozoic (2.45
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Ga), (6) with established multistage development (2.45–1.75 Ga), (7) Svecofennian domain (2.0–1.7 Ga); (8–12) Lapland-Kola and Zimniy suture zones: (8) metasediments (2.0 Ga), (9) tonalite-trondhjemite-granodiorite orthogneisses, granitoids (2.0–1.8 Ga), (10) enderbites, charnokites (1.91–1.94 Ga), (11) anorthosites (2.45 and 1.9 Ga), (12) collisional melange; (13) tectonic fractures; MC – Murmansk Craton; KC – Kola Craton; KAP – Kola alkaline province
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after Arzamastsev and Wu (2014). (b) Geological map of the central part of ADP, after Tretyachenko (2008): (1–3) Platform deposits: (1) Neoproterozoic siliciclastic sediments, (2) Carboniferous siliciclastic and carbonate sediments, and (3) early Permian chemogenic and carbonate rocks; (4) position of pipes of kimberlites and related rocks under platform deposits;
Figure 2
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and (5) contour of a kimberlite field. Age of the V. Grib kimberlite pipe by Shevchenko (2004). (a) Macro-photo of sheared peridotite xenolith: Sp – sheared peridotite,
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rim – kimberlite rim with microlitic-microporphyritic texture, kimb – massive pyroclastic kimberlite, white line traces a boundary of pelletal lapillus with sheared peridotite core; (b–d) optical micrograph (cross polarizers) showing the characteristic textural features of sheared peridotite xenolith: (b) porphyroclastic-mosaic texture, (c) olivine porphyroclast with deformation lamellae, (d) development of later clinopyroxene along rims and fractures in orthopyroxene with kink bands and deformation lamellae; (e–f) back-scattered electron images: (e) orthopyroxene (Opx) replaced by clinopyroxene (Cpx); (f) fragments of zoned garnet (Gar1 and Gar2 zones). Figure 3
Garnet chemical classification after Grütter et al. (2004). G1 – low-Cr
megacrysts (grey field, G1 differs from G4, G5, G9, and G12 by higher TiO2 concentrations); G3
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– eclogitic garnets; G4, G5 – pyroxenitic garnets (G5 garnets are distinguished from G9 garnets by Mg-number
