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Devonian Dike Swarms of Alkaline, Carbonatitic and Primitive Magma-Type Rocks from the South Kola Peninsula: Geochemical And

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Devonian Dike Swarms of Alkaline, Carbonatitic and Primitive Magma-Type Rocks from the South Kola Peninsula: Geochemical And DEVONIAN DIKE SWARMS OF ALKALINE, CARBONATITIC AND PRIMITIVE MAGMA-TYPE ROCKS FROM THE SOUTH KOLA PENINSULA: GEOCHEMICAL AND ISOTOPIC CONSTRAINTS ON PLUME- LITHOSPHERIC INTERACTION Ivan Mahotkin1, Hilary Downes2, Ernst Hegner3, Andy Beard2 1 De Beers, Russia; 2 School of Earth Sciences, Birkbeck University of London, UK; 3 University of Munich, Germany INTRODUCTION GEOCHEMISTRY Geochemistry and Sr-Nd-Pb isotopic compositions of The Early Devonian dikes and single Upper Devonian two dike swarms within the Devonian magmatic area of Group 1 kimberlite are classified as part of the ultra-K the south Kola peninsula (NW Russia) have been and K rock series, whereas the Late Devonian dikes are studied. One swarm is located in the north-west part of K-Na and ultra-Na rock series (Figure 1). the Kandalaksha gulf (Niva, Kandaguba areas) and the 4,0 other occurs further east on Turiy Cape. The Niva- Ultra-K K-series Na-series 3,5 series Kandaguba dike swarm also includes numerous dikes Kandaguba, Upper Devonian on islands in the Kandalaksha gulf and a kimberlite 3,0 Niva, Early Devonian dike exposed on Krestovaya mountain (Beard et al., 2,5 Turiy Cape, Upper Devonian 1996; Beard et al., 1998). Both swarms of Devonian 2,0 Alnoites dikes are situated within the Belomorian Belt of Late K2O, wt% 1,5 Aillikites Archaean crust which experienced Early Proterozoic Carbonatites 1,0 Group 1 kimberlites extension at 2.4-2.5 B.a. and collision process at 1.9-2.0 Niva, Late Devonian Ultra-Na series 0,5 Melilite picrites B.a. (Bibikova et al., 1996; Balagansky et al., 1998). To Kandaguba, Upper Devonian Alkaline picrites 0,0 Damkjernites 0,0 1,0 2,0 3,0 4,0 5,0 6,0 7,0 8,0 the south-east along the suture zone between the Melanonephelinites Na2O, wt% Belomorian Belt and the Kola craton, several fields of Melilitites Devonian melnoites and diamondiferous kimberlites Сal-nephelinites occur in the Terskiy Bereg area of the Kola Peninsula, Figure 1: K2O (wt%) vs Na2O (wt%) for the Early and Late in the Onega peninsula and Zimniy Bereg area of the Devonian dikes of the Kola peninsula. Arkhangelsk region (Kalinkin et al., 1993, Mahotkin, et al. 1997; Mahotkin et al., 2000; Beard et al., 2000). The picrites, damkjernites, melilitites and nephelinites form several distinctive clusters on the GEOLOGY SETTING CaO+Na2O+K2O vs SiO2+Al2O3 plot (Figure 2) The south Kola Devonian dike magmatism was related 30 to local extension during regional uplift of the Kola- Niva, Early Devonian K-Na&Na rock series Turiy Cape Arkhangelsk region (Mahotkin et al., 2000). Extension 25 formed two stages of dike magmatism in the south Kola Kandaguba Melilitites t %) Niva, Late Devonian w 20 Nephelinites peninsula in both Early and Late Devonian times i.e. ( 378-395 M.a. and 360-368 M.a (Bulakh & Ivannikov, Basanites +K2O 15 1984; Ivannikov & Ruchlov, 1996; Beard et al., 1996 Na2O Melnoites or Cpx-free Ol- Claesson et al. 2000). The Early Devonian magmatism + 10 melilitites (Kola, Aillikites Arkhangelsk) comprises dikes of alnoites, aillikites and potassic CaO Melilite picrites 5 carbonatites in the Niva area and Kandalaksha gulf. The Alkaline picrites Damkjernites Late Devonian magmatism comprises dikes of Group 1 0 kimberlites, melilite picrites, alkaline picrites, 30 35 40 45 50 55 60Melanoneph6e5linites damkjernites, sodalite-bearing ultra-Na carbonatites of SiO2+Al2O3 (wt %) Melilitites Cal nephelinites the Niva area, calcite-bearing nephelinites and sodium carbonatites of the Kandaguba, melilitites, Figure 2: CaO+Na2O+K2O vs SiO2+Al2O3 (wt%) for the K- melanonephelinites and sodium carbonatites of Turiy Na and Na rock series of the Kola peninsula. Cape. 8th International Kimberlite Conference Long Abstract 1 proposed by Le Bas (1989). Damkjernites and alkaline Trace element patterns of the average compositions of picrites have small chemical overlap and both rock each group of south Kola Devonian dikes (except types plot in the melilitite field. carbonatites) are shown on normalised multi-element plots in comparison with average ocean island basalts 90 (OIB) and of low-Ti Devonian melnoites of the Ol Fo =94.4 Arkhangelsk region (Figure 3 A, B, C). The latter were 80 Ol Fo =93 derived from ancient mantle sources with TDM =2.1- Ol Fo =91 Nd Niva, Later Devonian 2.3 B.a. (Mahotkin et al, 1997) and reflect chemical 70 heterogeneity in the subcontinental lithospheric mantle Mg + (BB SCLM) of the Belomorian belt prior to Devonian 60 Niva, Early Devonian Alnoites Aillikites Mg/Fe Turiy Mys Niva K-carbonatites 50 Group 1 kimberlites 1000,0 Melilite picrites Alkaline picrites Alnoites 40 Damkjernites Aillikites Kandaguba ) P OIB Niva Na-carbonatites , K Melanonephelinites , b 100,0 R 30 Melilitites t 0 5 10 15 20 25 30 Turiy Na-carbonatites BB SCLM excep MgO, wt% Cal nepheliites ( Kandaguba Na-carbonatites ite 10,0 Chondr / Figure 3: Plot of 100*Mg/(Mg+Fe) vs MgO for the Kola k (A) Devonian dikes and its fields. The thick horizontal solid lines Roc are mg-number of melts which are equilibrium with olivine 1,0 composition Fo94.4, Fo93 and Fo91 under Kd=0.29. Dashed line Rb Ba Th K Nb La Ce Pb Sr Nd P Sm Zr Ti Tb Y Yb Lu curves show Mg-numbers of the evolved melts from which Group I kimberlites 1000,0 different portions of Fo94.4 olivine were fractionated. Melilite picrites Alkaline picrites Evolution of the Devonian Kola dike melts has been Damkjernites P) , , K estimated from Mg-number (Figure 3) and Ni b 100,0 abundances. The evolution curves of Mg-number BB SCLM OIB shown in Figure 3 were calculated for Kd= 0.29 and for ite (except R different starting compositions. These plots show that hondr 10,0 ck/C Late Devonian alkaline picrites and melilite picrites o R from the Niva area are primitive melts derived from (B) mantle peridotites characterised by Fo92-93. Both rock 1,0 groups plot on slightly different olivine fractionation Rb Ba Th K Nb La Ce Pb Sr Nd P Sm Zr Ti Tb Y Yb Lu curves suggesting that their primary melts are slightly Turiy melanonephelinites 1000,0 different. The Group 1 kimberlites are primitive melts Turiy melilitites derived from mantle peridotites also characterised by Kandaguba Cal nephelinites Fo92-93 or were derived from more depleted mantle P) K, peridotites characterized by Fo94 However, they have 100,0 Rb, also accumulated olivine Fo92 (Beard et al., 1998). Ni except BB SCLM e ( t abundances (550-1050 ppm) in these rocks are very i OIB high and typical for primitive magmas (Figure 4). The Chondr 10,0 Early Devonian alnoites and aillikites and Late Rock/ (C) Devonian damkjernites from the Niva have mg- numbers of 63-72 and high Ni contents (150-500 ppm). 1,0 They are slightly evolved as a result of fractionation of Rb Ba Th K Nb La Ce Pb Sr Nd P Sm Zr Ti Tb Y Yb Lu olivine Fo91-92 from primary melts with 16-18 wt% MgO. The Late Devonian melanophelinites and melilitites from Turiy Cape are moderately evolved Figure 4 (A, B, C). Trace elements patterns for Early magmas and have low-moderate Ni abundances (50- Devonian alnoites and aillikites from Niva (A); Late 200 ppm). The Late Devonian calcite nephelinites from Devonian kimberlites, melilite picrites, alkaline picrites and Kandaguba are strongly evolved magmas with very low damkjernites from Niva (B); Late Devonian Ni contents (34 ppm). melanonephelinites from Turiy and Late Devonian cal nephelinites from Kandaguba (C). 8th International Kimberlite Conference Long Abstract 2 magmatic activity. The Niva dikes of the both K-and magmatism, in contrast to the Devonian kimberlite- Na- rock series are enriched in LREE, Th, Nb, Ba, Sr melnoite magmatism of the Arkhangelsk region. Only and to some extent in Rb relative to OIB and they show Late Devonian Kandaguba rocks show slight distinct negative K and Pb anomalies. Patterns for Late enrichment in radiogenic source that could be the Devonian Turiy and Kandaguba melilitites and influence of EM-1 mantle source. nephelinites differ from those of the Niva rocks in 20 Alnoites having a positive Pb anomaly and a small negative K Aillikites 15 DM (A) K carbonatite anomaly. Generally inter-element variations (Ba/Nb, Group 1 kimberlites 10 La/Ba and others) and patterns of the south Kola rocks OIB Later Devonian Melilite picrites Alkaline picrites 5 HIMU are similar to those of OIB and are strongly different Damkjernites Early Devonian 0 Na carbonatites from melts derived from the SCLM beneath the d Belomorian belt (BB SCLM). E N -5 Mixing line of plume-lithospheric -10 interction in the Arkhangelsk region EM-2 Trace element variations in primitive and slightly -15 evolved members of the south Kola dike swarms were Low-crust granulites -20 used to estimate the degree of melting and mantle EM-1 -25 source mineralogy. These variations indicate that all -60 -40 -20 0 20 40 60 80 100 120 140 dike rocks were derived from a phlogopite-bearing E Sr garnet lherzolite mantle source. Low degrees of melting Turiy Cape: of this source (0.7-3 %) influenced the preservation of 20 phlogopite in the restitic mineral assemblage, giving Melilitites 15 (B) Melanonephelinites DM rise to K-troughs on the chondrite-normalised trace Carbonatites 10 element patterns of the dike rocks. A comparison of OIB Turiy Cape Kandaguba: 5 HIMU Cal nephelinites Early and Late Devonian melting conditions indicates Terskiy Bereg 0 Carbonatites an increase in the proportions of melts (up to 3-5 %) in d E N -5 Late Devonian times and an increase in the depth of Kandaguba Mixing line of plume-lithospheric interction in the Arkhangelsk region melting in the mantle that resulted in the generation of -10 EM-2 kimberlite magma.
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