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RUSSIAN JOURNAL OF EARTH SCIENCES, VOL. 4, NO. 3, PAGES 187-209, JUNE 2002
Rare earth elements in rocks and minerals from alkaline plutons of the Kola Peninsula, NW Russia, as indicators of alkaline magma evolution
A. A. Arzamastsev1, F. Bea2, L. V. Arzamastseva1, and P. Montero2
1 Geological Institute, Kola Science Center, Russian Academy of Sciences, Apatity
2 University of Granada, Dept. of Mineralogy and Petrology, Fuentenueva s/n., 18002, Granada, Spain
Abstract. In order to elucidate evolutionary paths for the alkaline ultramafic series of the Kola province, we studied distribution of rare earth elements (REE) in rocks and constituent minerals of the rock sequence dunite, clinopyroxenite, melilitolite, meltejgite, ijolite, nepheline syenite. Abundances of REE and other trace elements were measured in olivine, melilite, clinopyroxene, nepheline, apatite, perovskite, titanite, and magnetite. Distribution of most trace elements in Kovdor-type rocks is shown to differ fundamentally from that in the Khibiny alkaline ultramafic suite and to have been controlled by perovskite crystallization. Primary olivine melanephelinitic melts of the Kovdor series are demonstrated to be characterized by early crystallization of perovskite, the most important REE mineral. Perovskite co-precipitating with olivine and clinopyroxene leads to a sharp REE depletion of the residual melt, to produce REE-depleted derivatives, ijolites and nepheline syenites. By contrast, the genesis of the Khibiny alkaline ultramafic series was complicated by mixing of minor batches of phonolitic melt with the primary olivine melanephelinitic magma, which led to changes in the crystallization order of REE-bearing titanates and Ti-silicates and to enrichment of late melt batches in the most incompatible elements. As a result, Khibiny ijolites have the highest REE abundances, which are accommodated by high-REE apatite and titanite.
1. Introduction
In the northeastern Baltic Shield, the Paleozoic stage of tectonic and magmatic reactivation involved generation of alkaline plutonic complexes, which have been customarily divided into two rock suites: (i) alkaline ultramafic rocks associated with carbonatites (Kovdor, Vuoriyarvi, Afrikanda, Seblyavr, etc., massifs) and (ii) agpaitic nepheline syenites, represented in the vast Khibiny and Lovozero plutons. Available isotope ages indicate that all the Paleozoic alkaline massifs of the Kola province were coeval, and their parental melts were derived from the same mantle sources [Kramm and
Copyright 2002 by the Russian Journal of Earth Sciences.
Paper number TJE02094.
ISSN: 1681-1208 (online)
The online version of this paper was published 15 May 2002. URL: http://rjes.wdcb.ru/v04/tje02094/the02094.htm
Kogarko, 1994; Kramm et al., 1993]. The hallmark of the region’s alkaline rocks is their immense abundances of REE, Y, Sr, Zr, Hf, Nb, Ta, and Th. These are either concentrated in apatite, titanite, perovskite, and other accessories or, given their concentrations in melts were high enough, form their own discrete minerals, such as loparite, pyrochlore, and eu-dialyte, whose economic deposits provide the basis for the region’s mining industry.
Geologic observations and experimental evidence suggest that alkaline ultramafic rocks forming parts of carbon-atite complexes originated through crystal fractionation in nephelinitic melts, which resulted, at early stages, in olivine, clinopyroxene, and melilite cumulates and their complementary foidolites and nepheline syenites [Arzamastsev et al., 2001; Dawson et al., 1995; Ivanikov et al., 1998; Kukharenko et al., 1965; Nielsen, 1994; Verhulst et al., 2000]. Available data on behavior of incompatible elements during magma-genesis suggest that with advancing magma crystallization, elements such as Sr, Zr, Hf, Nb, Ta, Th, and REE are likely to become enriched in terminal melt derivatives of the
Figure 1. Location scheme for Paleozoic igneous occurrences in northeastern Baltic Shield. Intrusions: 1 - Khibiny, 2 - Lovozero, 3 - Niva, 4 - Mavraguba, 5 - Kovdor, 6 - Sokli, 7 - Sallanlatva, 8 - Vuoriyarvi, 9 - Kandaguba, 10 - Afrikanda, 11 - Ozernaya Varaka, 12 - Lesnaya Varaka, 13 - Salmagora, 14 -Ingozero, 15 - Cape Turiy, 16 - Kurga, 17 - Kontozero, 18 - Ivanovka, 19 - Seblyavr. Terrane location scheme, after [Balagansky et al., 1998].
alkaline ultramafic series. This is indeed the case in alkaline ultramafics of the Khibiny massif, at whose lower horizons large fragments of such bodies are found surrounded by agpaitic syenites [Arzamastsev et al., 1998; Galakhov, 1975]. However, in the majority of alkaline ultramafic plu-tons region-wide, terminal crystallization products (ijolites, nepheline syenites, and cancrinite syenites) are appreciably depleted in elements such as Nb, Ta, and rare earths.
This work is intended to study how the above trace elements behave in alkaline ultramafic suites and, in particular, to find out why rare earth elements follow different distribution patterns in ultramafic carbonatite intrusions and in the Khibiny massif. Our study draws on mineralogic and geochemical data on representative samples from the Kovdor, Vuoriyarvi, Cape Turiy, Salmagora, and Afrikanda massifs, the Lesnaya Varaka and Ozernaya Varaka intrusions, and the Khibiny complex. ICP-MS analyses were made on whole-rock samples and on separates of coexisting perovskite, apatite, titanite, clinopyroxene, melilite, olivine, nepheline, and magnetite. Data obtained enable us to identify those factors responsible for the diversity of REE distribution pat-
terns in alkaline ultramafic suites and, in particular, to assess the role of high-REE accessory phases-loparite, apatite, and titanite.
2. Geologic Structure of the Intrusions
In the northeastern Baltic Shield, intracratonic magma-tism that spanned some 40 to 50 m.y. can be divided into three episodes. The initial episode, from 405 to 380 Ma, coinciding with the final phase of Caledonian orogeny, involved inception of the Khibiny, Lovozero, and Kontozero calderas in the foreland of the Caledonian front, accompanied by sub-alkaline volcanism and emplacement of ultramafite and Ne-syenite intrusions. The principal period of igneous activity, between 380 and 360 Ma, gave rise to the multiphase Khibiny and Lovozero plutons and to alkaline ultramafic intrusions associated with carbonatites [Kramm and Kogarko, 1994; Kramm et al., 1993] (Figure 1). The final episode resulted in dike swarms and diatremes made up of alkaline picrites,
Figure 2. Scheme showing geologic structure of the Kovdor massif, simplified after [Ternovoi, 1977]. 1 - carbonatite, 2 -phoscorite, 3 - nepheline syenite, 4 - foidolite, 5 - olivine-diopside-phlogopite rocks, 6 - olivine-monticellite-melilite rocks, 7 - melilite rocks, 8 - pyroxenite, 9 - peridotite and dunite, 10 - Precambrian basement.
melanephelinites, melilitites, and kimberlites [Arzamastsev et al., 2001].
2.1. Alkaline Ultramafic Plutonic Suites Forming Parts of Carbonatite intrusions (Kovdor Type)
Plutonic alkaline ultramafic suites are found forming parts of multiphase intrusions. Lithologic zonation of the intrusive bodies portrays the following order of emplacement of rocks that constitute the series (i) dunite, (ii) pyroxen-ite, (iii) melilite-bearing rocks (turjaite, melilitolite, okaite), (iv) melteigite, (v) ijolite, (vi) nepheline/cancrinite syenite, and (vii) carbonatites and phoscorites. The complete set of lithologies is represented in the Kovdor, Cape Turiy, and Vuoriyarvi massifs, whereas in the rest of intrusions only particular groups of rock varieties are exposed at the present topographic surface. In most intrusions, olivine and clinopy-roxene cumulates make up their cores, melilite rocks and foidolites occurring in peripheral zones (Figure 2). Nepheline and cancrinite syenites either make up detached satellite bodies near the intrusions (e.g., the Maly Kovdor) or fill in veins in alkaline ultramafics (Ozernaya Varaka). Boss-like carbonatite bodies, surrounded by carbonatite stockworks,
usually are located centrally in the intrusions, but occasionally they are displaced from geometric centers of the ring bodies of alkaline ultramafites. The order of emplacement, based on generalized field evidence from all the intrusions of the region, is consistent with that reported for alkaline ul-tramafic intrusions worldwide [Kogarko et al., 1995; Le Bas, 1987; Nielsen, 1987; Woolley, 1987]. Alkaline ultramafic intrusions occur in spatial association with bodies of olivine melteigite porphyry and with dikes and diatremes of alkaline picrite, Ol-melanephelinite, nephelinite, and melilitite.
2.2. Alkaline Ultramafic Plutonic Suites Forming Parts of Agpaitic Syenite Complexes (Khibiny Type)
Although exposed portions of the Khibiny and Lovozero plutons are dominated by agpaitic syenites, geophysical data verified by drilling reveal alkaline ultramafic rocks [Galakhov, 1975] and carbonatites [Dudkin et al., 1984] within the Khibiny massif and ultramafic and melilite rocks [Arzamast-sev et al., 1998] within the Lovozero massif. According to our own data [Arzamastsev et al., 1998], volumetrically, alkaline ultramafic rocks make up at least 30% of the Khibiny pluton and 25% of the Lovozero pluton within the 12.5 km depth range accessible to gravity surveying. The plutons are thus shown to comprise the complete series of rocks typical of alkaline ultramafic massifs of the province: peridotites, pyroxenites, melilitolites, melteigites, ijolites, and carbon-atites. The Khibiny complex displays at least three phases of emplacement of alkaline ultramafic melts with intervening stages of Ne-syenite magma injection (Figure 3). The peridotites, pyroxenites, and melilitolites originated at the earliest formative phase of the massif (Phase I, Figure 3b), which preceded agpaitic syenite injections. The ring melteig-itesijolite intrusion (Phase II, Figure 3d) took shape after the emplacement of nepheline syenites forming the margin of the Khibiny massif, but prior to the formation of the Ne-syenites found in its core. The Khibiny alkaline ultramafic series culminated in carbonatites (Phase III, Figure 3g), which cut through the Ne-syenite core of the massif and carry pyrox-enite, ijolite, and melteigite xenoliths.
As regards the Lovozero massif, alkaline ultramafics are encountered mostly in its northeast part, where large blocks and xenoliths of peridotites and melilitic rocks occurring among nepheline syenites suggest that these rocks originated at the earliest stage of emplacement of the complex. Foidolites are not widespread in the massif, their presence being evidenced by sporadic, Ne-syenite-hosted, ijolite and melteigite xenoliths, recovered in cores from a number of drillholes.
3. Analytical Techniques and Sample Preparation
Sixty-nine representative samples, collected from drill-cores and outcrops in the Khibiny, Lovozero, Kovdor,
Figure 3. Hypothetical model for the formation of the Khibiny complex [Arzamastsev et al., 1998]. Symbols: 1 -carbonatite, 2 - pulaskite, 3 - nepheline syenite in the core of the massif (foyaite), 4 - kalsilite/nepheline syenite, juvite, and apatite rocks, 5 - ijolite and melteigite, 6 - nepheline syenite in the rim of the massif, 7 - olivine pyroxenite and melilitolite, 8 - alkaline volcanites, 9 - Precambrian basement, 10 - fault. (a)-(g) - phases of emplacement of the massif.
Afrikanda, Cape Turiy, Lesnaya Varaka, Ozernaya Varaka, Seblyavr, Salmagora, Sallanlatva, Vuoriyarvi, and Ivanovka intrusions, were selected for this study from a total of more than 500 samples. Modal-mineral compositions of the samples are listed in Table 1.
Whole-rock major element analyses were carried out
at the Geological Institute, Kola Science Center, Russian Academy of Sciences, using a routine technique of sample fusion with 2Na2 CO3+1Na-tethraborate followed by dissolution in HCl. Si, Al, Mg, Ca, Fe, Ti, Ni, Co, Cr, and V were measured by atomic absorption on a Perkin Elmer 403 instrument with an accuracy (coefficient of variation, CV) better than 3% (G. Gulyuta, analyst). Na, K, Li, Rb, and Cs were measured by flame photometry (CV ~5%); P and S, by photocolorimetry and polarography from the same solutions with an accuracy of ~5% and ~10%, respectively; and F and Cl, by the ion-selective electrodes method (CV ~15%). The Fe2+/Fe3+ ratio was measured by titration (CV ~10%). H2O and CO2 were analyzed by the gravimetric method (CV ~10%).
Trace elements were analyzed by ICP-MS at the University of Granada. Sample charges of 0.1 g were allowed to stand for 30 min in an HNO3 + HF mixture in Teflon-lined containers at T = 180°C and ~200 p.s.i., evaporated until dry, and dissolved in 100 ml of 4% HNO3. Each specimen was analyzed three times on an ELAN-5000 PE SCIEX instrument using a rhenium within-lab standard. Accuracies were ±2 rel.% and ±5 rel.% or better for concentrations of 50 and 5 ppm, respectively.
Major elements in minerals were measured at the Geological Institute, Kola Science Center, on a Cameca MS-46 ion microprobe using natural and synthetic standards. Acceleration voltage was 30 kV for Sr and Zr and 20 kV for the rest of the elements; sample current was 20-40 nA, and ion beam diameter, 1.5-3 ^m.
Mineral grains separated for trace-element analysis were inspected under an optical microscope in order to reject foreign inclusions. A number of samples were inspected under a scanning electron microscope. Minerals were separated on a magnetic separator and in heavy liquids. Finally, 8-10 mg charges were cleaned by repeated hand-picking to 99.9 vol % purity. Trace element abundances in sample charges were measured by ICP-MS as described above.
4. Petrography of the Rocks and Distribution of REE-bearing Mineral Phases
Ultramafic rocks. Kovdor-type dunites, Ol-clinopyro-xenites, and pyroxenites are adcumulates and mesocumu-lates with olivine and clinopyroxene as cumulus phases and ore minerals, phlogopite, spinel, and nepheline as intercumulus (Table 1). The only primary high-REE minerals are perovskite and apatite. In the dunites, perovskite occurs sporadically as an intercumulus phase forming small roundish grains (Figure 4a). In the pyroxenites, perovskite is present as an early cumulus phase accounting for as much as 40 vol % in Vuoriyarvi rocks, 19-31 vol % in Afrikanda, and 11-16 vol % in the Salmagora massif [Korobeinikov et al., 1998; Kukharenko et al., 1965]. In ultramafic rocks, apatite is less common, dunites containing no more than 0.2% and pyroxenites usually bearing up to 3% apatite by volume. The only exception is Vuoriyarvi and Afrikanda
ARZAMASTSEY ET AL.: RARE EARTH ELEMENTS IN ROOKS AND MINERALS Table І. Modal-mineral compositions of alkaline ultramafic rocks (vol %)
Ol Cpx Mel Ne Mic Prv Ap Ttn Mag Others
4/4GG KVD Dunite 92 <1 8 Spl 1
22Т/43 KVD Turjaite 5 5Т 5 2G 1 <1 12
252/1GG KVD Turjaite 3 5б 3 33 <1 <1 3
Т/394 KVD Foidolite б5 2G 8 <1 Т
Т/348 KVD Foidolite б5 1G 1G <1 2 3 4 Amph 5
5^4G KVD Foidolite ТТ 5 Т 3 3 5
5/бЮ KVD Foidolite 3Т 55 3 2 3
V3G KVD Foidolite 58 35 2 1 Cal 5
Т/92.8 KVD Foidolite б9 2G 1 <1 5 3 1
2Т/б5 KVD Foidolite 5 ТG 1G 5 <1 4 5
MK-1G KVD Nepheline syenite 2G 35 1G 1 3 1 Fsp 3G
AFR-1 AFR Peridotite
AFR-5 AFR Pyroxenite ТG 8 1Т 1 5
AFR-б AFR Pyroxenite ТG 14 5 3 Grt 8
25-AFR AFR Pyroxenite 9G 2 5 1 1 Cal 1
Z-б LSV Dunite 95 <1 5
SL-23 SLM Dunite 8Т 1 1 <1 1G Spl 1
SL-24 SLM Pyroxenite Т5 5 5 3 5 1 б
93/192 VUO Pyroxenite ТG 2 1G <1 18
282/224 VUO Pyroxenite 84 12 1 1G
282/251 VUO Pyroxenite бб 5 1G 1 18
25V2G8 VUO Melteigite б5 3G 2 1 1
25/15 SLN Ijolite 5G 44 1 2 2 Cal 1
2б/151 SLN Ijolite 4G 5G 1 1 9
31/2GG SLN Ijolite 45 4G 2 1 2 5 Cal 5
2б/151 SLN Ijolite 3Т 52 1 3 2 4 Cal 1
8-OV OZV Melteigite Т1 5 5 <1 8 5 5
1G1G/1G52 KHI Peridotite 6G 2G 1G <1 1 б
A-1G44 KHI Peridotite 4G 24 5 29 1 1
A-1G36 KHI Pyroxenite 5Т 3 15 <1 1 5 Amph 18
A-1087 KHI Pyroxenite бТ 5 15 б 2 5
A-1G38 KHI Pyroxenite 3 39 2 3G 1 1 1G Amph 14
1G1G/1G59 KHI Turjaite 5 5G 2G <1 2 25 Grt 1
ЮЮ/11б5 KHI Turjaite 5 45 2G <1 <1 15 Mtc 1G, Spl 3
455/345 KHI Melteigite б5 23 2 3 Т
4бб/552 KHI Melteigite 6G 18 1G 2 5 5 Fsp <1
1119/2Т9 KHI Melteigite бб 11 5 Т 8 Fsp 3
ЮЮ/118б KHI Ijolite 24 2G 3G 1 3 3 19 Fsp 3
1GТ2/53G KHI Ijolite 5G 3б 1 9 2 Fsp 2
455/4G2 KHI Ijolite 45 45 3 1 3 1 Fsp 2
1б3б/Т21 KHI Ijolite 21 55 2 3 3 2 Fsp 14
1152/83 KHI Ijolite 33 4Т 1 1 5 3 Fsp 1G
Note: Mineral composition were determined by thin-section counting on 1000 points. Hereinafter in Tables: KVD — Kovdor, LSV — Lesnaya Varaka, SLM — Salmagora, AFR — Afrikanda, VUO — Vuoriyarvi, OZV — Ozernaya Varaka, SLN — Sallanlatva, KHI — Khibiny. Ol — olivine, Cpx — clinopyroxene, Mel — melilite, Mic — mica, Ne — nepheline, Prv — perovskite, Ap — apatite, Mag — magnetite, Mtc — monticellite, Spl — spinel, Ttn — titanite, Grt — Ca-Ti-garnet, Cal — calcite, Fsp — K-Na-feldspar, Amph — amphibole.
pyroxenites, in which apatite accounts for as much as 8% of rock volume [Kukharenko et al., 1965]. Besides perovskite and apatite, the pyroxenites contain sporadic titanite that forms secondary segregations partially replacing perovskite and magnetite.
Ultramafic rocks encountered in the Khibiny and Lovozero
massifs are represented by peridotites and, chiefly, by pyroxenites, which are texturally and compositionally similar to ultramafics of the Kovdor suite. Pyroxene with characteristic cumulus features is in places partially replaced by richterite and/or phlogopite. REE-bearing accessories are represented by apatite and titanite (up to 6 and 2 vol %,
50 jim
01
(a)
Prv
|%
Cpx
Figure 4. Perovskite segregations in rocks of the alkaline ultramafic series (backscattered electrons raster photomicrographs): a - primary perovskite (Prv) in olivine (Ol) from Kovdor dunite, sample 4/400; b - secondary perovskite overgrown on magnetite (Mag) and melilitolite + phlogopite (Phl) grains, Kovdor, sample 252/100.
respectively; Table 1). An important distinction is that per-ovskite is a rare accessory in all ultramafic rocks from the Khibiny.
Melilite-bearing rocks, dominantly uncompahgrites and turjaites, form independent intrusion phases in the Kov-dor and other alkaline ultramafic massifs. In the Khibiny and Lovozero, melilite rocks are encountered as xenoliths. Melilite together with phlogopite compose large oikocrysts with clinopyroxene and nepheline inclusions. REE-bearing phases, represented by perovskite, apatite, and, less frequently, titanite, occur sporadically. Intersticial segregations of magnetite are not infrequently rimmed by secondary per-ovskite (Figure 4b), indicative of a Ti-bearing phase having been exsolved from primary titanomagnetite [Nielsen et al., 1997].
Foidolites occur widely in both the Kovdor and Khibiny alkaline ultramafic suites. The rocks are ortho- and mesocu-mulates with nepheline segregations varying in habit from anhedral to euhedral in less and more leucocratic rocks, respectively. Clinopyroxene makes up zoned segregations whose compositions are different in the Kovdor and Khibiny suites. In foidolites of the Kovdor and other alkaline ultra-mafic massifs, pyroxene is represented by diopside, which makes up grain cores, while grain rims are composed of aegirine-augite. Pyroxenes in Khibiny ijolite-melteigites are more alkaline than in the Kovdor suite and, unlike the latter, are composed of aegirine-augite rimmed by aegirine. Accordingly, late amphiboles developed after clinopyroxene have different compositions, mostly pargasitic in Kovdor foido-lites and corresponding to richterite or magnesiocataphorite in the Khibiny suite.
Distribution patterns of REE-bearing accessories are different in Kovdor and Khibiny foidolites. In Kovdor, Vuori-
yarvi, and Cape Turiy melteigites and ijolites, the early-generation perovskite, just as apatite and titanite, is a typical accessory phase. Not infrequently, the perovskite is observed to be replaced by titanite. The mean titanite abundance in ijolites is <1 vol %. Apatite abundances in foidolites attain a critical maximum of 1.2 wt % in the most melanocratic lithologies [Arzamastseva and Arzamast-sev, 1996].
Unlike the Kovdor suite, Khibiny foidolites contain apatite and titanite not only as late magmatic accessories, but also as widespread primary REE minerals. Both apatite and titanite are most abundant in melanocratic foidolite varieties, where they account for 4 and 5 vol % on average, respectively. A distinctive feature of Khibiny foidolites is that they lack primary perovskite.
Nepheline- and cancrinite syenites in Kovdor-type massifs show evidence of early crystallization of light-colored phases, nepheline and K-Na-feldspar. Just as in foidolites, pyroxene is represented by zoned grains of diopside rimmed by aegirine-augite. REE-bearing accessories are titanite and apatite.
Arzamastsev et al. [1998] showed that neither Khibiny nor Lovozero agpaitic Ne-syenites are cogenetic with rocks of the alkaline ultramafic series. This is evidenced, in particular, by the fact that the REE-bearing mineral assemblage in agpaitic syenites differs fundamentally from that in the alkaline ultramafic rocks. Lovozero lujavrites have as much as 90 vol % eudialyte and 12 vol % loparite, while in Khibiny Ne-syenites the most widespread primary magmatic phases are eudialyte and apatite. Distribution, composition, and origin of these economically important minerals were studied by Kogarko [1977, 1999] and Kravchenko et al. [1992] and are beyond the scope of this work.
5. Results
5.1. Rock Chemistry
5.1.1. Major elements. Bulk-rock analyses representative of Kovdor- and Khibiny-type alkaline ultramafic suites are listed in Tables 2 and 3. Compositional variation trends for both suites, plotted on the totality of major-element analyses amassed to date (Figure 5), show the ultramafic portion to be controlled by precipitation of olivine and clinopyrox-ene, whereas the foidolite trend is controlled by fractionation of clinopyroxene and nepheline. The decrease in Mg# through this rock sequence from 0.90 in dunites to 0.56 in Ne-syenites of the Kovdor suite is correlative with variations of Ni, Cr, Co, V, and Sc.
The following distinctions exist between the Kovdor and Khibiny suites in terms of major-element abundances. Khibiny foidolites are relatively lower in MgO and higher in SiO2 and alkalis (Figure 5). Thus, weighted mean abundances of these oxides in Khibiny foidolites are 43.62 wt % SiO2, 9.40 wt % Na2O, 3.59 wt % K2O, and in Kovdor-type foidolite intrusions, 41.64 wt % SiO2, 8.10 wt % Na2O, 2.73 wt % K2O. The high contents of silica and alkalis are manifest in modal-mineral compositions of Khibiny foidolites, such that K-Na-feldspar is a characteristic accessory mineral in ijolites, where it accounts for as much as 10 vol %. Among other distinctions between Kovdor and Khibiny rocks, one should note the higher F content of Khibiny rocks and the differences in TiO2 and P2Ob distributions. Thus, in Kovdor suite the highest TiO2 abundances are detected in pyrox-enites, which have 8-15 wt % MgO on average, whereas in Khibiny suite TiO2 is highest in the most evolved rocks, ijolites and melteigites, which have 3-7 wt % MgO.
5.1.2. Rare earth elements (REE). Chondrite-normalized plots for REE from both rock suites, listed in Tables 4 and 5, are shown in Figure 6. Along with data for specific samples, all the plots display the REE pattern for the weighted mean composition of alkaline ultramafic rocks of the Kola province [Arzamastsev et al., 2001].
All the Kovdor-type alkaline ultramafic rocks lack Eu anomaly and show depletion in the light REE relative to the heavy REE (Figure 6). The lowest total REE contents and (La/Yb)N ratios (11.7-17.4) were detected in olivine cumulates from the Kovdor, Lesnaya Varaka, and Salmagora massifs. By contrast, pyroxenites from the majority of massifs, which contain perovskite and, to a lesser extent, apatite, are sharply REE-enriched relative to the mean composition of alkaline ultramafic rocks. These rocks have steeper REE patterns with (La/Yb)N = 52-226. More evolved derivatives (melilitolites, foidolites, and Ne/cancrinite syenites) have lower REE contents compared to the mean alkaline ultramafic rock composition for the province, at 5x10 to 3x102 times the chondritic level. Therefore, with advancing differentiation of the Kovdor suite, late-stage ijolite and Ne-syenite derivatives become progressively depleted in REE.
Khibiny alkaline ultramafic rocks have a REE distribution pattern which is sharply dissimilar to the Kovdor suite (Figure 6). By and large, REE abundances of perovskite-
free peridotites and pyroxenites are close to the estimated mean values for the alkaline ultramafic series. Due to low (La/Yb)N ratios, ranging 31.4-53.4, the light REE contents are G.5-G^ times the mean values for the alkaline ultramafic series, whereas the medium and heavy REE contents are 2 times higher than the mean values. Just as in pyroxenites, REE abundances in Khibiny melilite rocks are within the range of mean values established for the alkaline ultramafic rocks. On the other hand, the latest derivatives in the suite, ijolites and melteigites, are markedly REE-enriched relative to the mean composition of alkaline ultramafic rocks of the province. In particular, melteigites from the Khibiny layered complex, which have up to 8 vol % titanite and 5 vol % apatite, show 2x1G3 times the chondritic REE concentrations. To sum up, the Khibiny alkaline ultramafic suite is characterized by a progressive REE enrichment of its late derivatives.
5.2. REE distribution in minerals
5.2.1. REE-bearing phases. Perovskite. Two generations of perovskite have been reported from alkaline ultra-mafic rocks of the province. Generation I perovskites originate from the early igneous stage of alkaline ultramafite crystallization, as evidenced by the fact that melt inclusions in these perovskites match trapped portions of the primary melt compositionally [Kogarko et al., 1991; Veksler et al., 1998b]. Generation II perovskite, found mainly in melilitolites and foidolites, makes up rims around per-ovskite I and around magnetite. According to [Mitchell, 1996b], the early-generation perovskites are compositionally close to the ideal formula CaTiO3, whereas late perovskite segregations follow a loparite trend associated with enrichment in Na, LREE, Nb, and Th. Established are appreciable compositional distinctions between the early and late generations of the perovskites extracted for analysis. Generation I perovskites (Table 6) have the lowest REE, Nb, Ta, Y, U, Th, and Sr abundances, which have been detected in Vuoriyarvi pyroxenites. On the other hand, in Generation II perovskites, as represented by samples from Kovdor melilitolites and Ozernaya Varaka ijolites, the listed elements have 2 to 10 times the concentrations of the early magmatic perovskites. Overall, all the perovskites are sharply LREE enriched ((La/Yb)N = 207-518) (Figure 7). Compared to perovskites from other carbonatite assemblages worldwide, the varieties under study are closely similar to those from the Oldoinyo Lengai foidolites [Dawson et al., 1995] and kimber-lites [Mitchell and Reed, 1988] in terms of REE contents, but the latter have higher (La/Yb)N ratios.
Apatite. Besides Ca, P, and F, apatites from all the rocks under study have appreciable abundances of Sr, Y, and REE (Table 6), the late apatite generation having highest values. Apatites from pyroxenites and foidolites of the Kovdor, Afrikanda, Sallanlatva, and Khibiny plutons have very narrow ranges of both total REE contents and (La/Yb)N, 57278. Chondrite-normalized REE spectra (Figure 7) for apatites are nearly parallel and broadly correlative to the REE abundances of host rocks. The earlier report on Eu anomaly
Figure 5. Major oxides (wt %) vs. MgO in alkaline ultramafic rocks of the Kovdor (empty circles) and Khibiny (solid circles) type.
Table 2. Whole-rock major element analyses (wt %) for carbonatite-bearing alkaline ultramafic massifs of the Kola province
Rock DUN DUN DUN PRD PRX PRX PRX PRX PRX PRX MELT MELT MLG MLG MLG
Massif KVD LSV SLM AFR AFR AFR VUO VUO VUO SLM KVD KVD KVD KVD KVD
Sample 4/400 Z-6 SL-23 AFR-1 AFR-5 AFR-6 93/192 2S2/224 2S2/251 SL-24 22T/43 252/100 7/394 T/34S 5/T40
SiO2 3T.S1 3S.T4 3S.5S 13.SS 37.6S 32.17 43.21 34.24 26.97 39.33 41.25 41.10 44.10 4S.24 3S.35
TiO2 0.24 0.35 0.52 22.30 1.69 7.19 4.14 12.2S S.63 3.S6 0.79 0.47 1.26 0.22 1.29
Al2O3 1.20 0.3S 0.96 0.41 3.36 7.41 3.SS 3.63 4.02 7.05 10.90 S.02 10.15 1.24 4.01
Fe2 O3 1.4S 3.74 4.90 1S.59 4.4S 10.95 7.15 S.S5 19.09 6.90 3.74 2.6S 4.37 2.46 S.TS
FeO 9.01 11.22 6.07 11.10 4.S1 9.41 4.36 5.76 12.71 9.12 4.3S 3.22 6.19 3.43 12.36
MnO 0.20 0.23 0.24 0.23 0.13 0.22 0.14 0.1S 0.34 0.21 0.10 0.09 0.15 0.17 0.21
MgO 44.05 43.30 39.67 15.72 S.S1 9.1S 12.60 11.07 9.69 S.41 10.10 9.90 10.27 14.76 14.41
CaO 4.17 0.69 3.3S 14.1S 2S.S7 15.95 22.4S 21.56 15.70 20.9S 19.60 26.40 14.47 22.50 14.6S
Na2 O 0.10 0.03 0.0S 0.09 0.S2 1.55 0.50 0.43 0.37 1.6S 4.65 3.7S 4.56 1.43 0.46
K2O 0.05 0.03 0.51 0.06 0.06 1.29 0.21 0.52 0.52 0.37 2.10 1.35 2.54 0.77 2.02
P2O5 0.03 0.04 0.04 0.01 S.05 1.01 0.19 0.19 0.16 0.3S 0.05 0.07 0.12 1.76 0.0S
CO2 0.24 0.16 0.10 0.79 0.20 0.27 0.36 0.26 0.2S 0.30 0.2S 0.40 0.21 1.73 0.6S
Stot. 0.0S 0.02 0.05 n.a. 0.21 0.25 n.a. n.a. 0.02 n.a. n.a. n.a. n.a. n.a. 0.01
F 0.01 0.01 0.01 n.a. 0.40 0.07 0.03 0.04 0.03 0.02 0.06 0.05 0.07 0.1S 0.07
H2O 0.72 0.50 3.96 1.S2 0.47 3.07 0.44 0.56 0.55 1.33 1.42 1.S6 0.SS 0.S9 2.1S
Total 99.39 99.44 99.07 99.1S 100.04 99.99 99.69 99.57 99.0S 99.94 99.42 99.39 99.34 99.7S 99.59
mg# 0.90 0.S7 0.92 0.37 0.77 0.64 0.S4 0.59 0.36 0.62 0.S0 0.S5 0.75 0.SS 0.6S
Rock MLG IJL IJL IJL IJL IJL IJL IJL NFS NFS AVER*
Massif OZV SLN SLN SLN SLN KVD KVD KVD OZV KVD
Sample S-OV 31/200 25/110 25/15 26/151 5/610 7/30 27/65 Z-12 MK-10
SiO2 45.40 41.49 35.93 41.93 41.25 44.56 44.44 42.92 55.79 51.S3 37.20
TiO2 0.S5 1.29 0.43 0.73 0.7S 0.13 0.34 1.92 0.44 0.S2 2.6S
Al2O3 3.S7 14.31 19.03 15.94 16.20 19.56 12.50 7.20 19.07 16.52 7.20
Fe2O3 3.55 5.96 1.42 4.4S 6.57 1.17 0.22 4.56 1.66 2.1S S.96
FeO 6.76 4.51 2.47 6.71 4.67 2.01 7.43 7.92 1.72 4.70 6.1S
MnO 0.24 0.16 0.06 0.17 0.13 0.10 0.1S 0.14 0.05 0.12 0.25
MgO S.97 5.34 4.77 5.35 5.62 5.66 5.26 11.S6 0.61 3.3S 12.62
CaO 22.67 12.93 13.44 11.16 11.30 9.52 14.74 17.40 2.39 4.44 17.11
Na2O 2.52 7.SS 11.44 S.53 S.77 9.94 7.29 2.67 11.35 S.5S 2.97
K2O 0.34 2.S2 3.04 2.S4 2.99 4.04 2.69 0.64 2.43 3.64 1.S7
P2O5 3.41 1.S9 5.36 0.76 0.67 0.79 1.00 0.20 0.21 0.54 1.20
CO2 0.26 0.43 1.19 n.a. 0.59 0.S1 1.10 0.S0 1.S9 0.44 1.76
Stot. 0.01 0.10 0.30 0.04 0.05 0.01 n.a. n.a. n.a. 0.10 -
F 0.20 0.06 0.27 0.04 0.03 0.06 0.05 0.06 0.03 0.10 —
LOI 0.62 0.66 1.34 0.S5 0.41 1.15 0.S1 1.29 1.65 1.S6 —
Total 99.67 99.S3 100.49 99.53 100.03 99.51 9S.05 99.5S 99.29 99.25 100.00
mg# 0.70 0.49 0.69 0.59 0.6S 0.S3 0.56 0.73 0.25 0.56 0.61
Note: Hereinafter in Tables: n.a. — not analyzed, n.d. — not detected, mg# = Mg/(Mg+Fe2+). Rock symbols: DUN — dunite, PRD - peridotite, PRX - pyroxenite, MEL - melilitolite, MELT - turjaite, MLG - melteigite, IJL - ijolite, NFS - nepheline syenite. AVER* - weighted mean composition of the alkaline ultramafic series of the Kola province, after Arzamastsev et al. [2001].
[Kravchenko et al., 1979] has not been confirmed by any single measurement. Comparison with other provinces in terms of REE contents and patterns shows that apatite compositions under study resemble those from carbonatites of the Alno, Sokli, and Fen massifs [Hornig-Kjarsgaard, 1998].
Titanite. We have analyzed late titanites, which replace
perovskite in Afrikanda pyroxenites (sample 25-AFR), and groundmass titanites from Ozernaya Varaka and Khibiny ijo-lites. Comparison shows that Khibiny varieties are appreciably enriched in Sr, whereas Ozernaya Varaka and Afrikanda titanites have elevated concentrations of Zr, Hf, U, and Th (Table 7). All the varieties have narrow ranges of REE con-
Table 3. Whole-rock major element analyses (wt %) for the Khibiny alkaline ultramafic series
Rock PRD PRD PRX PRX PRX MEL MEL MLG MLG MLG MLG IJL IJL IJL IJL
Sample A-1044 1010/ A-1036 A-1087 A-1038 1052 1010/ 1010/ 1119/ 1059 1165 279 455/ 345 466/ 1010/ 552 1186 1072/ 530 455/ 1636/ 1152/ 402 721 83
SiO2 43.62 38.26 41.60 37.53 41.37 28.01 29.98 41.24 37.56 44.00 39.52 43.48 44.81 43.67 46.07
TiO2 3.41 3.51 4.91 2.90 4.18 6.01 2.84 6.42 7.73 4.60 7.25 2.67 1.97 1.61 2.28
Al2O3 5.21 4.29 5.92 11.09 7.37 6.12 3.58 4.87 3.38 3.64 9.17 18.85 17.44 21.03 17.84
Fe2 O3 5.41 10.31 4.33 5.90 8.90 15.57 10.51 9.23 11.60 11.72 8.00 4.88 5.31 4.53 5.17
FeO 7.06 5.25 11.25 4.04 5.22 5.83 5.18 8.22 11.81 7.70 7.00 3.17 3.19 3.95 2.90
MnO 0.19 0.28 0.23 0.17 0.23 0.26 0.29 0.48 0.61 0.33 0.28 0.16 0.21 0.22 0.29
MgO 17.85 19.93 11.67 6.49 13.38 9.20 16.58 5.74 7.17 8.32 7.01 3.35 3.94 1.54 1.79
CaO 9.36 12.60 11.20 18.40 9.09 23.43 28.46 13.61 14.68 13.41 11.74 7.70 7.91 4.63 3.94
Na2 O 2.26 0.65 3.47 5.69 3.18 1.35 0.67 4.93 3.30 4.02 4.56 10.58 10.74 13.21 11.58
K2O 2.91 2.06 2.11 1.78 3.60 0.86 0.04 1.73 0.81 1.46 2.36 4.45 3.78 3.42 5.20
P2O5 0.36 0.42 0.38 2.97 0.36 0.77 0.37 1.88 0.99 0.27 1.25 0.65 0.22 1.00 0.37
CO2 0.14 0.38 0.23 0.96 0.32 0.49 0.35 n.a. 0.05 0.05 0.32 0.31 0.07 0.15 0.08
Stot. 0.03 0.16 0.12 0.40 0.04 0.04 0.02 0.30 n.a. n.a. 0.19 n.a. n.a. 0.04 n.a.
F 0.45 1.06 0.60 0.14 0.91 0.58 0.16 0.43 0.20 0.36 0.32 0.09 0.07 0.21 0.26
H2O 1.01 0.68 1.52 1.27 1.32 1.53 0.46 0.72 0.33 1.08 0.48 0.20 0.48 0.70 1.23
Total 99.27 99.84 99.54 99.73 99.47 100.05 99.49 99.80 100.22 100.96 99.45 100.54 100.14 99.91 99.00
mg# 0.82 0.87 0.65 0.74 0.82 0.74 0.85 0.38 0.52 0.66 0.64 0.65 0.69 0.25 0.29
tents and relatively low (La/Yb)N ratios (40-53), which results in gently sloping, straight chondrite-normalized patterns (Figure 7).
5.2.2. Rock-forming minerals. Olivine. To analyze trace element contents, we selected the purest olivine grains of Fo82-9i composition from Kovdor and Lesnaya Varaka dunites. This, however, did not ensure the absence of magnetite microinclusions, which are distributed evenly within olivine crystals. Scanning electron microscopy detects extremely thin perovskite rims around primary chromite inclusions in olivine. On the one hand, positive correlation of Nb and Ta with REE in olivine (Table 8) implies the presence of perovskite microinclusions. On the other hand, all the olivine specimens analyzed show negative Eu anomaly, also observable in magnetite that coexists with olivine (Figure 8). The highest Eu oxidation degree (Eu/Eu* < 0.08) was established in Lesnaya Varaka dunites, which contain significant amounts of magnetite. Based on this evidence, we assume that a considerable fraction of REE contained in olivine grains is concentrated not in this mineral proper, but in perovskite and magnetite microinclusions.
Clinopyroxene. In early cumulates of the alkaline ul-tramafic series, clinopyroxene is represented by diopside Di8oHd1BAcB, with foidolites and nepheline syenites containing zoned segregations that range in composition from augite DiBBHd40AcB to aegirine-augite DiB0Hd30Ac20 [Arzamastsev and Arzamastseva, 1993; Kukharenko et al., 1965]. A study of zoned pyroxene grains using the laser ablation technique [Arzamastsev et al., 2001b] shows that zone-to-zone variations of major elements within crystals are not accompanied by any marked variations in the contents of trace elements, in particular, REE. This is further supported by analyses of pyroxene separates from pyroxenites, melilitolites, and ijo-
lites from carbonatite massifs of the province, which reveal a narrow range of REE variations in all the groups of rocks (Table 8). The higher REE contents are observed in rock varieties from Khibiny ijolites, although all the rocks have the same REE distribution pattern. Plots shown in Figure 8 demonstrate all the clinopyroxenes to be enriched in Yb and Lu relative to Dy, Ho, and Er.
Melilite. Microprobe measurements on melilites from rocks of the Kovdor massif yield the following composition (mol %): Mg-akermanite, 49-70; Fe-akermanite, 5-11; Na-melilite, 36-40. Compared with previously published data on melilite compositions in the rocks of the province [Bell et al., 1996], the analyzed melilites have higher Mg/Fe ratios, a feature typical of Ne-free alkaline ultramafites [Mitchell, 1996a; Rass, 1986]. Overall, the melilite is high in Sr due to the isomorphous replacement Sr2+ ^ Ca2+. Unlike Khibiny melilites, Kovdor ones display no appreciable enrichment in Sr (Table 8). Compared with the scanty reported REE measurements on melilites from various provinces [Mitchell, 2001; Onuma et al., 1981], Kovdor specimens have somewhat lowered total REE contents and straight patterns with relatively high (La/Yb)N ratios of 178-203 (Figure 8).
Nepheline. Nepheline compositions in rocks of the Kovdor-type alkaline ultramafic intrusions range from Ne77.8-82.5Ks9.6-18.9 Qz 1.4-3.2 to Ne78.6-81.6KsiB.2-20.1
Qz1.4-3.2 in foidolites and Ne-syenites, respectively. Nephelines from Khibiny foidolites are higher in the kalsilite end-member and silica (Ne68.4-72.8Ks21.B-26.1Qz4.8-7.4). Because of high Fe2O3 contents in the matrix of nepheline, all the nepheline grains are replete with aegirine microlites representing exsolution products. REE contents in all the nepheline varieties range from low to very low (Table 8). Chondrite-normalized REE patterns are straight (Figure 8), nephelines from Khibiny ijolites having negative Eu anomaly
Table 4. Whole-rock trace element analyses (ppm) for carbonatite-bearing alkaline ultramafic massifs of the Kola province
Rock DUN DUN DUN PRD PRX PRX PRX PRX PRX PRX MELT MELT MLG MLG MLG
Massif KVD LSV SLM AFR AFR AFR VUO VUO VUO SLM KVD KVD KVD KVD KVD
Sample 4/400 Z-6 SL-23 AFR-1 AFR-5 AFR-6 93/192 282/224 282/251 SL-24 227/43 252/100 7/394 7/348 5/740
Li n.d. 2.58 3.32 2.11 n.d. 4.80 n.d. 0.81 1.86 6.22 n.d. n.d. n.d. n.d. n.d.
Rb 4.53 0.94 18.7 1.54 5.05 25.0 10.4 18.9 11.69 11.7 47.3 35.8 69.6 23.4 63.0
Cs n.d. 0.08 0.29 0.05 n.d. 0.11 n.d. 0.24 0.19 0.14 0.36 0.20 0.61 0.12 0.75
Be 0.18 0.26 0.86 0.47 2.37 6.20 1.73 1.29 1.12 7.03 8.42 9.19 1.81 2.62 1.90
Sr 74.5 7.67 160 766 1525 1313 399 677 369 1103 1998 3050 358 563 298
Ba 21.1 12.3 152 30.7 20.6 25.7 151 297 222 801 1011 951 401 103 937
Sc 7.82 7.09 8.80 31.3 14.9 14.4 79.0 89.5 43.0 46.2 12.6 2.34 28.5 97.5 13.5
V 20.8 20.8 58.3 190 177 210 142 202 375 355 73.1 41.6 171 191 190
Cr 1462 2124 2725 27.3 23.2 10.2 30.3 116 171 38.6 3.96 5.07 1083 51.1 30.4
Co 112 168 93.9 96.4 35.8 69.0 35.8 46.1 85.1 52.4 36.7 35.1 49.6 12.9 69.1
Ni 1480 1432 1961 54.5 40.6 29.7 59.8 75.3 148 54.5 145 85.4 321 21.5 231
Cu 18.1 7.58 25.8 49.9 314 216 34.5 58.1 33.8 415 17.6 26.1 162 12.3 28.2
Zn 70.0 79.9 85.9 201 34.2 108 48.3 144 208 148 183 219 79.8 44.1 194
Ga 3.84 1.91 2.68 27.5 12.9 28.1 16.9 26.5 31.7 18.3 15.9 15.9 14.8 5.27 16.5
Y 1.49 0.69 2.38 49.3 66.9 25.9 27.9 78.5 36.3 29.4 3.18 3.76 6.20 10.3 3.51
Nb 8.64 3.00 10.3 1412 31.6 379 208 818 561 238.3 12.7 10.8 18.8 18.5 32.4
Ta 0.41 0.38 0.44 132 1.89 41.7 20.4 42.2 48.5 13.7 0.86 0.73 0.46 0.93 2.80
Zr 21.0 6.31 80.9 111 419 472 456 450 482 425 98.5 25.8 113 190 210
Hf 0.55 n.d. 1.93 4.75 12.9 5.72 18.0 15.9 17.3 11.9 2.88 0.68 2.99 4.78 2.59
Sn 2.18 0.78 n.d. 7.38 4.96 5.21 6.37 7.79 11.0 7.37 2.71 1.83 3.43 3.93 4.99
Pb 0.98 0.71 0.48 5.43 13.0 5.93 1.65 3.16 1.48 4.15 2.50 3.53 5.05 2.14 1.73
U 0.29 n.d. 0.43 16.2 1.53 6.19 3.28 14.5 6.54 5.38 0.22 0.24 0.45 0.50 0.83
Th 0.95 0.29 0.48 201 7.36 72.7 15.9 87.3 43.0 12.2 0.81 0.88 1.07 3.80 2.30
La 5.16 0.95 5.39 1724 354 475 224 1046 513 172 28.5 42.6 21.2 42.5 8.25
Ce 11.1 1.66 10.1 4827 551 1037 502 2800 1343 368 52.9 76.2 50.0 99.6 18.5
Pr 1.24 0.17 1.13 359 53.0 111 57.5 256 144 43.2 5.71 8.08 6.09 12.2 2.32
Nd 3.37 0.55 4.08 1131 189 386 222 888 516 142 19.9 27.4 22.1 47.7 8.14
Sm 0.60 0.11 0.70 124 31.1 44.2 35.5 125 70.0 20.2 2.69 3.74 3.57 7.30 1.58
Eu 0.23 0.02 0.21 29.4 9.23 10.1 9.26 33.1 17.7 5.36 0.52 0.84 0.95 1.99 0.36
Gd 0.32 0.08 0.65 78.9 24.8 23.2 24.1 86.9 47.3 13.8 1.62 2.06 2.28 5.15 1.02
Tb 0.05 0.02 0.09 8.57 3.18 2.31 2.70 10.1 5.35 1.74 0.16 0.22 0.28 0.59 0.14
Dy 0.32 0.09 0.47 24.3 16.0 8.19 10.9 32.1 17.6 7.64 0.71 0.90 1.42 2.59 0.77
Ho 0.06 0.02 0.10 2.96 2.74 1.10 1.52 4.52 2.26 1.23 0.13 0.14 0.26 0.41 0.14
Er 0.19 0.05 0.26 4.72 5.92 2.14 2.65 7.55 3.76 2.70 0.28 0.32 0.63 0.90 0.40
Tm 0.03 0.01 0.04 0.43 0.67 0.25 0.31 0.75 0.36 0.36 0.04 0.04 0.10 0.13 0.07
Yb 0.21 0.06 0.24 2.23 3.50 1.48 1.67 3.65 1.80 2.03 0.25 0.23 0.67 0.93 0.42
Lu 0.03 0.01 0.04 0.23 0.49 0.21 0.23 0.41 0.21 0.27 0.04 0.03 0.12 0.14 0.08
(La/Yb)N 17.4 11.7 15.7 521 71.1 226 94.2 193 192 59.6 81.9 128 22.3 32.0 13.9
(Eu/Eu* = 0.13), evidently due to the presence of magnetite microinclusions, rather than aegirine ones only. On the other hand, in nephelines from Kovdor ijolites, which are least abundant in aegirine microlites, Eu anomaly is expressed poorly (Eu/Eu* = 0.69).
5.2.3. REE distribution in coexisting mineral phases. Data on REE distribution in principal REE- bearing phases—perovskite, apatite, and titanite (Tables 6, 7)— enable us to calculate partition coefficients for these phases.
Comparison of coefficients obtained for the coexisting pairs perovskite/apatite (Dprv/Ap), perovskite/titanite (DPrv/Tit), and apatite/titanite (DAp/Tit) (Table 9) shows that in early pyroxene-perovskite cumulates, REE partition preferentially into the perovskite. Overall, during magmatic crystallization, REE enter the above minerals in the following order: perovskite > apatite > titanite. According to our calculations, the early-generation perovskite (sample AFR-5) extracts medium- and heavy REE most strongly (DPrv/Ap for Tb-Lu > 3), whereas in perovskite Ilsapatite pairs (sam-
Table 4. Continued
Rock MLG IJL IJL IJL IJL IJL IJL IJL SFN SFN AVER*
Massif OZV SLN SLN SLN SLN KVD KVD KVD OZV KVD
Sample 8-OV 31/200 25/110 25/15 26/151 5/610 Т/30 2Т/65 Z-12 MK-10
Li 4.20 3.Т1 2.92 n.d. n.d. n.d. n.d. 5.21 4.36 43.4 13.5
Rb Т.91 46.Т 42.Т 50.1 52.9 54.6 63.Т 15.5 20.0 131 49.3
Cs 0.12 0.30 0.24 0.04 n.d. 0.04 0.01 n.d. 2.91 0.94 0.64
Be 2.56 2.90 2.40 1.Т8 1.Т2 6.52 10.0 1.29 4.53 4.2Т —
Sr 1106 561 8Т9 359 388 281 Т30 429 96Т 1039 2094
Ba 31.6 88.6 8Т.9 Т6.2 6Т.1 129 163 210 956 1101 1116
Sc 11.9 4.Т5 2.89 8.01 13.5 22.3 11.6 49.Т 1.11 10.Т 24.8
V 200 1Т5 46.Т 101 94.9 85.4 1Т5 294 66.6 124 104
Cr 59.1 46.0 15.3 13.3 19.6 5.16 Т6.0 409 12.4 55.4 293
Co 32.5 31.6 11.8 31.6 33.1 Т.55 23.0 53.Т 3.38 18.9 42.5
Ni 24.4 16.Т Т.Т3 19.4 18.2 Т.55 30.8 130 1.99 31.9 243
Cu 12.0 135 65.0 62.6 118 9.05 23.4 205 4.60 58.4 —
Zn Т5.1 Т0.Т 10.4 59.4 58.5 22.Т 96.0 61.9 18.0 102 —
Ga 10.6 21.Т 18.0 18.3 19.5 20.1 30.Т 13.1 1Т.4 20.8 —
Y 20.5 19.3 26.Т 6.25 6.33 4.66 Т.21 10.6 1.96 12.5 33.6
Nb 29.0 48.0 18.6 16.3 16.3 20.4 65.3 16.1 135 52.8 95.8
Ta 2.05 5.53 1.52 0.54 0.81 2.16 3.99 0.Т3 10.2 2.8Т 5.50
Zr 164 182 Т4.4 58.2 55.4 264 283 82.8 146 155 34Т
Hf 3.55 4.36 2.0Т 1.Т1 1.80 5.41 4.Т9 3.24 2.53 3.Т3 Т.65
Sn 2.42 3.Т0 3.91 2.43 2.69 3.12 3.19 3.54 4.8Т 3.30 —
Pb 1.59 1.9Т 10.6 2.69 3.39 1.2Т 2.53 4.13 1.53 13.3 —
U 0.83 0.40 1.03 0.49 0.44 0.50 1.54 0.38 0.Т2 1.68 2.15
Th 12.2 4.36 10.3 1.86 2.33 Т.02 1Т.2 1.31 0.Т5 8.56 8.51
La 169 38.6 113 21.6 22.6 32.0 55.4 18.5 12.8 52.1 131
Ce 315 83.1 216 40.0 44.1 Т0.2 118 36.2 30.0 88.Т 249
Pr 34.1 9.86 23.Т 4.42 4.99 Т.93 13.1 4.19 3.66 8.40 2Т.4
Nd 116 38.2 86.3 15.5 18.3 28.Т 46.0 16.1 12.8 2Т.3 96.9
Sm 15.1 6.65 12.Т 2.55 3.12 4.22 5.94 2.92 1.ТТ 3.99 14.4
Eu 3.60 2.01 3.63 0.80 0.91 1.12 1.45 0.9Т 0.49 0.Т8 3.60
Gd 11.1 6.02 10.9 2.06 2.33 2.69 3.4Т 2.52 1.34 2.84 10.2
Tb 1.28 0.8Т 1.39 0.25 0.28 0.30 0.3Т 0.3Т 0.1Т 0.39 1.26
Dy 5.26 4.84 6.01 1.31 1.38 1.32 1.48 2.0Т 0.68 2.16 6.02
Ho 0.82 0.84 1.11 0.25 0.25 0.20 0.2Т 0.40 0.10 0.44 1.05
Er 1.8Т 2.03 2.50 0.58 0.5Т 0.42 0.Т1 0.99 0.20 1.26 2.42
Tm 0.25 0.30 0.32 0.09 0.08 0.06 0.10 0.15 0.03 0.19 0.32
Yb 1.50 1.ТТ 1.Т1 0.60 0.54 0.50 0.Т2 0.93 0.1Т 1.22 1.83
Lu 0.25 0.30 0.23 0.11 0.10 0.08 0.12 0.14 0.03 0.18 0.26
(La/Yb)N Т6.2 14.Т 44.6 25.4 29.5 45.0 54.3 14.0 51.2 30.0 48.4
ple 8-OV) the bulk of the heavy REE partition into the apatite. The results obtained are consistent with microprobe measurements on minerals from Ugandan clinopyroxenites and kamafugite lavas [Lloyd et al., 1996] and from the plutonic Oldoinyo Lengai alkaline ultramafic rocks [Dawson et al., 1994, 1995], which reveal a relative constancy of REE distribution in the perovskite-apatite pair (DPrv/Ap: La 9, Ce 16, Nd 9.5). DPrv/Ap values similar to those obtained by us for the late perovskite II-apatite pairs were established for Kaiserstuhl calcite carbonatites [Hornig-Kjarsgaard, 1998], DPrv/Ap in these rocks decreasing from 6.8-4.9 for the LREE
to 3.0-1.5 for the MREE through to 0.5 for Yb.
5.2.4. Estimating REE distribution between minerals and rocks. In view of the fact that alkaline ul-tramafic rocks under study are differentiates, and their chemistries do not necessarily correspond to compositions of those melts that precipitated the mineral phases contained in these rocks, estimates of mineral/melt partition coefficients (Dminerai) may be very tentative. Hence, when calculating D REE for early phases from pyroxene and olivine
ARZAMASTSEV ET AL.: RARE EARTH ELEMENTS IN ROOKS AND MINERALS Table 5. Whole-rock major element analyses (wt %) for the Khibiny alkaline ultramafic massif
Rock PRD PRD PRX PRX PRX MEL MEL MLG MLG MLG MLG IJL IJL IJL IJL
Sample A-1044 1010/1052 A-1036 A-1087 A-1038 1010/ 1010/ 1119/ 1059 1165 279 455/ 345 466/ 1010/ 1072/ 455/ 1636/ 1152/ 552 1186 530 402 721 83
Li 36.6 8.0 46.1 2.6 84.3 6.00 7.50 32.4 12.2 28.4 22.3 28.5 7.90 14.5 44.2
Rb 115.4 138.4 112.7 23.9 207.8 58.5 1.10 51.8 15.9 37.7 86.0 23.4 34.4 71.3 97.6
Cs 1.30 2.60 1.52 0.32 2.20 0.79 0.03 0.55 0.32 0.22 0.60 3.62 0.19 0.78 0.95
Be 0.99 2.54 7.39 4.68 5.46 5.61 3.17 7.36 3.02 3.34 4.25 6.53 5.73 5.70 15.3
Sr 893 1126 995 748 1485 5933 539 6168 2544 3237 2194 31.3 1352 4974 3280
Ba 558 1364 432 187 521 1063 49.4 1166 168 1114 852 357 335 49.2 2609
Sc 21.4 23.9 28.2 19.0 21.1 42.0 24.0 23.3 26.5 22.3 20.0 2.50 19.5 2.67 5.50
V 213 506 251 242 265 298 83.1 547 673 739 428 1.80 276 322 208
Cr 1131 1277 800 22.7 724 158 1061 92.7 112 39.1 135 72.8 51.4 38.9 83.4
Co 80.7 98.0 66.1 27.7 62.5 83.8 102 49.8 65.1 75.6 45.9 2.6 16.0 10.9 14.8
Ni 915 1018 428 37.8 568 278 994 77.2 104 61.9 134 37.4 29.1 5.61 64.3
Cu 65.2 963 39.4 237 26.1 194 34 285 534 628 455 10.3 18.0 21.0 83.2
Zn 157 190 305 131 226 277 159 247 429 143 325 80.8 105 102 200
Ga 12.2 12.4 28.2 21.1 24.2 33.4 9.2 20.0 14.3 12.8 24.6 32.3 32.9 37.0 38.2
Y 19.7 27.7 30.4 45.9 33.6 30.5 18.3 76.8 63.0 36.0 86.6 41.8 24.1 21.4 56.7
Nb 39.0 73.4 104 154 94.8 312 157 304 261 169 371 215 110 101 387
Ta 2.55 5.41 7.64 6.83 5.75 23.3 15.1 17.8 31.2 16.4 28.0 15.8 7.98 5.59 11.2
Zr 220 345 481 429 453 480 173 1168 812 814 744 929 565 564 2131
Hf 5.94 8.74 10.3 12.2 11.1 12.5 4.59 23.4 19.8 24.8 18.0 25.3 12.9 11.5 32.3
Sn 0.34 1.96 2.73 3.10 2.01 5.92 1.40 7.53 5.00 4.19 5.40 8.12 2.17 11.5 6.31
Pb n.a. n.a. n.a. n.a. n.a. n.a. n.a. 6.42 n.a. 0.78 n.a. 8.21 n.a. 5.79 11.9
U 0.41 1.56 1.76 3.05 1.86 4.45 2.97 4.44 0.85 0.20 1.57 3.68 1.08 1.45 8.51
Th 2.67 5.04 9.09 6.10 7.22 27.9 19.2 16.9 3.99 0.85 23.4 23.2 3.19 5.30 19.6
La 62.0 85.6 102 143 102 251 128 330 222 108 380 119 69.4 204 116
Ce 138 176 223 255 216 465 270 652 441 250 747 238 150 332 200
Pr 16.5 20.3 26.4 28.1 24.8 49.2 28.9 66.8 50.8 30.7 88.9 27.3 16.6 30.3 19.7
Nd 68.4 79.9 105 112 99.0 173 103 235 190 116 323 97.6 62.2 96.1 67.3
Sm 11.6 13.7 18.0 22.0 16.7 23.3 13.3 35.0 30.4 19.9 49.5 16.8 10.4 12.0 11.1
Eu 3.29 3.92 5.08 7.11 4.70 6.18 3.47 10.2 8.97 5.77 14.3 1.68 3.04 3.24 3.40
Gd 8.47 10.8 13.2 20.6 12.0 13.8 7.50 29.4 22.8 13.8 33.1 11.2 7.63 9.36 10.5
Tb 1.03 1.39 1.65 2.82 1.64 1.66 0.90 3.98 3.08 1.93 4.37 1.73 1.05 1.20 1.68
Dy 4.99 6.42 7.57 12.23 7.71 7.85 4.20 17.9 14.6 9.08 21.0 9.44 5.26 4.88 9.23
Ho 0.81 1.04 1.22 1.88 1.34 1.18 0.69 3.09 2.46 1.61 3.42 1.97 0.93 0.86 2.01
Er 1.85 2.45 2.63 4.03 3.04 2.67 1.64 6.94 5.61 3.62 7.83 5.31 2.37 1.97 5.63
Tm 0.21 0.28 0.31 0.44 0.37 0.29 0.20 0.93 0.66 0.49 0.86 0.81 0.32 0.29 0.86
Yb 1.21 1.54 1.82 2.40 2.19 1.66 1.20 5.17 4.06 3.23 4.80 4.71 2.20 1.95 5.05
Lu 0.17 0.21 0.27 0.32 0.30 0.22 0.18 0.74 0.59 0.55 0.60 0.70 0.34 0.34 0.71
(La/Yb)N 36.0 39.1 39.3 42.0 32.8 106.8 75.2 48.1 38.5 23.6 55.7 17.8 22.2 70.4 15.4
cumulates, REE contents were correlated not with their host rocks, but with the mean composition for alkaline ultramafic rocks (Table 4), which best approximates composition of the melt parental to the series. Coefficients thus obtained are listed in Table 10 and are compared to published experimental values. In the plot showing Dprv/meit for the entire REE spectrum (Figure 9), partition coefficients for Kola perovskites, while plotting somewhat lower, stay nonetheless with the same trend as does DPrv/melt in melilite-olivine basalts, as determined by Onuma et al. [1981].
In calculations of D REE for minerals from the more
evolved members of the alkaline ultramafic series (ijolites), we assumed their constituent phases (clinopyroxene, melilite, apatite, and titanite) to have been in equilibrium with the host rocks. The obtained Dcpx/rock and DAp/rock values, listed in Table 11, broadly compare to those for minerals in alkaline volcanites from other regions [Caroff et al., 1993; Foley et al., 1996; Irving and Price, 1981; Larsen, 1979; Onuma et al., 1981]. On the other hand, partition coefficients for titanites from Khibiny and Ozernaya Varaka ijolites are lower than those for phonolite-hosted titanites [Worner et al., 1983].
Figure б. Chondrite-normalized REE patterns for alkaline ultramafic rocks of the Kovdor and Khibiny types. In all the plots, heavy line shows REE pattern for the weighted mean composition of the alkaline ultramafic series. Normalizing values, after [Anders and Grevesse, 1989].
6. Discussion
Petrologic evidence, supported by experimental data [Edgar, 1987; Le Bas, 1987; Onuma and Yamamoto, 1976; Pan and Longhi, 1989, 1990; Veksler et al., 1998a; Wilkinson and Stolz, 1983], indicate that the main process responsible for the genesis of alkaline ultramafic suites of various provinces worldwide was fractional crystallization of primary olivine melanephelinitic magma. Coherence of the rock formation sequence from early olivine- and clinopyroxene cumulates to melilitolite, foidolite, and Ne-syenite, is corroborated by geologic and petrographic observations. Estimates of magma compositions for the Kola alkaline province [Arzamastsev et al., 2001a] allow the inference that alka-
line ultramafics of the Kovdor and Khibiny types originated from the same primary magma. This is further supported by isotope studies, indicative of a single mantle source for Khibiny and Kovdor alkaline rocks [Kramm and Kogarko, 1994]. Variation trends in major-element plots for both suites reflect sequential precipitation of olivine, clinopyrox-ene, and melilite. Foidolites are produced through a reaction that involves resorption of melilite and formation of diopside and nepheline:
3CaMgSi2O6 + 2NaAlSiO4 = Mg2SiO4
diopside nepheline olivine
+ Ca2MgSi2O7 + NaCaAlSi2O7 + NaAlSi3Os . melilite (solid solution) liquid
100000
10000
1000
100
10
100000
10000
1000
100
10
100000
10000
1000
100
10
Perovskite
—i—232(224
282*251
k 205297
. —H—25-AFR
: —o—AFR-1
: —«—252/100
—±— sew
La Ce Pr Nd sm Eu Gd Tb Dy Ho Er TmYb Lu
Apatite
—•—1636/874
. ——31/200
25/110
—B—25-£FR
: —b—J&FR-5 '
—♦— 7/92.8
-4-8-OV
1 1 1 1 La Ce Pr Nd i i i i i i i i i —i Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
Titan ite
: -S— 25-£FR
. —*—8-OV
i —•—301 /900
-©—1636/874
1636/721
T 1----1---1--1---1--1---1--1--1---1--1---1--1 r
La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er TmYb Lu
Figure 7. Chondrite-normalized REE patterns for per-ovskite, apatite, and titanite from alkaline ultramafic rocks. Normalizing values, from [Anders and Grevesse, 1989].
Published data concerning distribution of trace elements in the above principal mineral phases of the alkaline ultra-mafic series are indicative of REE, Sr, Y, Zr, Hf, Nb, and Ta enrichment of final derivatives. Indeed, taking into account that partition coefficients for these elements in the first phases to crystallize, olivine and diopside, and considerably lower than 1, incompatible elements should be concentrated in late ijolite and Ne-syenite melts. Such distribution is exemplified by Khibiny-type alkaline ultramafics, in which, as follows from the plot in Figure 5, late ijolites are abnormally high in REE, Sr, and Y. On the other hand, as appears from the diagram in Figure 5, within the Kovdor-type alkaline ultramafic series, late ijolites and nepheline syenites of the Maly Kovdor, Vuoriyarvi, and Ozernaya Varaka massifs are more strongly depleted in REE than early differentiates. A similar pattern is found in alkaline ultramafic suites of the Maimechas-Kotui province in Siberia [Egorov, 1991], the Gardiner complex in East Greenland [Nielsen et al., 1997],
Figure 8. Chondrite-normalized REE patterns for rock-forming minerals of alkaline ultramafic rocks. Normalizing values, from [Anders and Grevesse, 1989].
and Tanzanian plutonic alkaline suites [Dawson et al., 1995].
Let us consider the main factors responsible for the differences in REE enrichment patterns between Kovdor- and Khibiny-type alkaline ultramafic rocks, which should include (i) conditions at which the primary alkaline ultramafic magma precipitates the principal REE phases (perovskite, apatite, and titanite), and (ii) changes in the composition of the primary magma and, accordingly, in the crystallization
Table 6. Trace element abundances (ppm) in perovskite and apatite from rocks of the alkaline ultramafic series of the Kola province
Mineral Perovskite I Perovskite II Apatite
Rock PRX PRD PRX MELT IJL PRX IJL
Massif AFR AFR VUO KVD OZV AFR KVD OZV SLN KHI
Sample 25-AFR AFR-1 205/ 282/ 282/ 252/ 8-OV 25-AFR AFR-5 7/92.8 8-OV 31/ 25/ 1636/
297 224 251 100 200 110 874
Sr 894 1796 392 907 545 2168 3545 5846 1274 5005 9358 1997 3202 27612
Ba 4.02 12.5 2.64 2.33 2.58 75.2 8.30 17.5 3.36 21.3 49.7 13.7 22.7 289
Sc 0.28 9.12 4.48 0.04 4.59 n.d. n.d. n.d. 4.04 n.d. n.d. 4.14 4.09 3.97
V 52.1 91.1 34.7 57.7 37.7 173 173 137 39.3 46.8 64.0 26.5 39.7 20.2
Cr n.d. 12.6 9.82 11.9 13.2 16.1 6.50 n.d. 9.20 n.d. n.d. 10.3 13.8 9.72
Co 0.66 4.67 0.81 1.15 0.89 n.d. n.d. n.d. 0.70 n.d. n.d. 0.77 0.89 0.75
Ni 1.45 8.67 4.15 5.36 3.56 1.36 0.33 5.01 4.10 4.94 3.27 5.47 8.75 5.63
Cu 80.8 96.4 61.5 72.1 35.1 164 1027 132 23.7 8.17 6.15 17.4 17.3 18.0
Ga 11.2 40.8 14.5 25.6 23.5 78.5 111 9.75 3.22 17.2 22.1 3.24 6.66 14.9
Y 60.0 111 64.4 142 98.6 350 203 131 50.0 149 178 54.9 86.1 134
Nb 991 2915 159 1382 560 4060 8569 3.47 1.34 2.39 13.8 4.42 4.62 9.27
Ta 52.4 234 25.5 91.0 53.7 190 551 0.56 0.06 0.33 3.86 0.12 0.16 0.24
Zr 68.6 213 69.7 186 122 573 142 5.37 0.92 3.11 8.06 0.78 0.47 4.12
Hf 2.25 8.98 2.18 6.40 4.19 16.7 4.54 0.42 0.12 0.38 0.70 0.13 0.15 0.22
Pb 4.64 12.37 4.51 7.12 4.72 30.1 63.8 3.38 1.73 10.4 10.1 2.33 2.83 1.55
U 27.5 34.7 10.3 26.3 19.2 41.5 137 5.61 0.88 22.0 11.3 0.83 3.26 0.74
Th 63.1 456 130 140 129 961 2557 32.5 3.23 339 199 9.24 26.2 4.32
La 1246 3510 880 1962 1629 6587 10700 1573 320 1417 2625 221 515 1798
Ce 3081 9255 2301 4582 4274 14822 22177 2023 499 3068 4423 438 984 2740
Pr 216 803 277 486 460 1645 2210 175 49.1 350 425 49.9 108 239
Nd 683 2570 1039 1716 1621 5644 6719 554 169 1247 1315 184 379 755
Sm 98.1 277 137 236 211 672 677 84.6 25.6 158 151 26.5 51.9 85.5
Eu 25.2 66.9 35.0 63.6 54.6 162 159 25.8 7.86 38.3 40.2 7.74 14.3 23.2
Gd 64.1 178.2 91.7 164 142 328 299 63.9 24.3 89.6 95.9 23.7 42.9 71.4
Tb 7.36 18.8 9.55 18.0 15.4 35.9 31.1 7.93 2.91 9.30 10.8 2.81 4.89 8.22
Dy 25.5 53.2 28.8 66.9 46.2 140 111 32.9 12.0 39.8 45.4 12.0 19.8 32.7
Ho 3.63 6.52 3.92 8.24 6.17 21.1 14.3 5.17 2.02 6.18 7.23 2.19 3.38 5.00
Er 5.91 10.5 6.11 13.7 10.0 36.2 24.0 9.53 4.18 12.0 15.3 4.78 7.12 9.66
Tm 0.64 0.99 0.61 1.33 0.90 3.89 2.60 0.97 0.47 1.49 1.76 0.60 0.81 0.99
Yb 2.80 4.89 2.73 6.38 4.40 19.83 13.92 4.83 1.81 7.16 9.80 2.61 3.80 4.35
Lu 0.28 0.52 0.31 0.69 0.45 2.49 1.88 0.60 0.24 0.78 1.17 0.35 0.46 0.44
(La/Yb)N 300.3 483.3 217.3 207.3 249.6 223.8 517.9 219.3 119.1 133.4 180.5 57.0 91.4 278.5
order of principal and accessory mineral phases as a result of mixing with batches of phonolitic melt supplied from independent source.
According to experimental data [Kogarko, 1990; Veksler and Teptelev, 1990] and to studies on melt inclusions [Kogarko et al., 1991; Veksler et al., 1998b], perovskite and apatite crystallized at early stages. This is evidenced by the fact that euhedral perovskite and apatite crystals contain inclusions that were homogenized at temperatures of >970°C and 1000-700°C, respectively [Kogarko, 1977; Nielsen et al., 1997]. Hence, crystallization paths of the alkaline ultra-mafic series must be considered with due account of REE-bearing phases, in the context of the six-component sys-
tems SiO2-TiO2-Al2O3-CaO-MgO-Na2O and SiO2-P2Os-Al2 O3-CaO-MgO-Na2 O.
In the pseudo-ternary nephelines-diopsides-titanite melting diagram (Figure 10), perovskite and the five remaining phases correspond to the mineral assemblage constituting rocks of the alkaline ultramafic series. According to [Veksler and Teptelev, 1990], perovskite forms a large crystallization field contiguous to the fields of all the phases except olivine. The primary alkaline ultramafic melt of composition A, which contains 2-3 wt % TiO2, plots in the diop-side crystallization field, so that resultant melts evolve toward the cotectic lines Di-Prv (points B and C) to produce olivine and pyroxene-perovskite cumulates and melil-
Table 7. Trace element abundances (ppm) in titanite and magnetite from rocks of the alkaline ultramafic series of the Kola province
Mineral Titanite Magnetite
Rock PRX IJL DUN MELT
Massif AFR OZV KHI KVD LSV KVD
Sample 25-AFR 8-OV 301/500 1636/874 1636/721 4/400 Z-6 252/100
Sr 801 987 4266 4386 2220 n.d. 4.08 56.2
Ba 2.89 16.7 9.69 9.13 6.92 2.38 5.11 13.3
Sc n.d. n.d. n.d. 5.00 4.66 22.7 15.05 n.d.
V 465 273 407 317 127 146 302 735
Cr 0.29 0.86 3.27 17.7 13.7 20300 47780 118
Co n.d. n.d. n.d. 1.11 0.80 238 288 182
Ni 2.34 2.21 2.21 5.51 3.64 3045 1962 796
Cu 227 107 115 61.2 37.0 13.1 31.5 58.6
Ga 7.86 21.3 16.0 11.9 6.92 44.1 35.9 30.8
Y 229 270 334 231 123 1.88 0.22 7.09
Nb 2299 6265 2659 2045 507 5.12 1.64 22.1
Ta 101 593 250 92.5 35.7 0.74 0.23 1.90
Zr 3351 2826 2356 1206 716 46.8 18.3 76.1
Hf 113 73.0 69.0 36.4 17.5 1.54 0.74 2.02
Pb 10.2 10.7 0.15 1.55 24.2 n.d. 0.17 n.d.
U 13.2 13.2 3.12 1.48 1.17 0.01 n.d. 0.01
Th 26.9 100 17.8 9.37 7.71 0.79 0.72 1.50
La 693 1260 961 678 382 8.12 1.22 24.0
Ce 1416 3323 2463 1813 989 12.8 2.25 53.7
Pr 154 407 309 228 123 1.43 0.23 5.69
Nd 556 1423 1148 840 442 4.28 0.57 20.3
Sm 109 209 194 137 70.0 0.60 0.15 2.87
Eu 36.3 59.6 58.7 41.4 20.7 0.01 n.d. 0.84
Gd 98.0 135 143 109 54.7 0.35 0.05 1.93
Tb 13.2 16.9 18.9 14.3 7.29 0.06 0.01 0.27
Dy 62.5 78.6 90.3 63.1 32.2 0.34 n.d. 1.09
Ho 10.2 12.8 14.8 10.3 5.33 0.05 n.d. 0.18
Er 20.9 25.7 29.7 20.3 11.1 0.09 n.d. 0.39
Tm 2.40 3.11 3.36 2.25 1.24 0.01 n.d. 0.04
Yb 11.6 16.0 15.4 9.80 5.11 0.03 n.d. 0.18
Lu 1.26 1.87 1.66 0.86 0.49 0.00 n.d. 0.02
(La/Yb)N 40.1 53.2 42.1 46.6 50.4 173.0 — 95.8
itolites. One factor controlling perovskite stability in melts is silica activity, described by the reactions CaTiO3 + SiO2 = CaTiSiO5 and 2CaTiO3 + NaAlSi3O8 = NaAlSiO4 + 2CaTiSiO5 [Carmichael et al., 1970; Veksler and Teptelev, 1990]. Hence, even small amounts of a more silicic material, when added to silica-undersaturated olivine melanephelinitic melt (the melt evolution course A1 — B1 — C1), prevent early crystallization of perovskite. As a result, Ti-silicates will crystallize not in initial melt derivatives in the form of per-ovskite, but in more evolved products (ijolites and nepheline syenites) in the form of titanite.
The behavior of apatite during evolution of the alkaline ultramafic series can be approximated by the section NaAlSiO4-CaMgSi2O6-Ca5(PO4)3F (Figure 11), as
discussed by Kogarko [1990], where the primary olivine melanephelinitic melt falls in the diopside crystallization field. Since the P2O5 content of the initial melt is 1.26 wt % (Table 2), apatite is unlikely to precipitate at early stages of rock crystallization. The fact that P2O5 distribution in all the members of the series points to the existence of a maximum of 2.8 wt % in melanocratic members of the foido-lite trend [Arzamastseva and Arzamastsev, 1996] suggests that apatite appears on the liquidus during crystallization of nepheline-pyroxene assemblages. Based on the above experimental models for crystallization of REE-bearing titanium minerals and phosphates, the following evolution paths for alkaline ultramafic suites of the Kola province can be considered.
Table 8. Trace element abundances (ppm) in rock-forming minerals of the alkaline ultramafic series of the Kola province
Mineral Olivine Pyroxene Melilite Nepheline
Rock DUN PRX MELT IJL MLG MELT IJL
Massif KVD LSV AFR KVD OZV KHI KVD KVD KHI
Sample 4/400 4/898 Z-6 25-AFR 252/100 7/30 8-OV 301/500 227/43 252/100 7/30 455/402
Rb 4.62 n.d. n.d. 0.62 0.38 1.27 0.67 2.52 7.03 7.14 117 56.6
Sr 92.5 5.32 1.22 474 301 260 553 2289 3689 3652 64.5 48.7
Ba 4.11 3.55 n.d. 6.25 5.70 5.02 34.9 6.31 7.22 16.5 39.5 57.8
Sc n.d. n.d. n.d. 39.5 51.7 5.57 n.d. 6.17 n.d. n.d. 9.23 14.2
V 1.40 0.42 0.57 169 41.8 290 131 651 0.76 1.04 0.68 1.60
Cr 3.00 4.55 17.6 4.19 n.d. 138 12.1 0.42 n.d. n.d. n.d. n.d.
Co 77.1 102 151 36.3 13.0 35.4 40.5 34.5 21.3 24.9 n.d. n.d.
Ni 917 1439 1267 17.9 74.1 42.8 15.2 9.75 4.47 6.55 n.d. 0.70
Cu 3.91 5.15 1.24 216 8.92 6.39 71.0 10.8 3.20 3.23 4.77 2.80
Ga n.d. n.d. n.d. 8.61 2.43 11.44 8.82 6.58 15.8 16.3 45.3 39.4
Y 7.05 1.73 0.51 4.63 5.67 4.19 7.45 17.6 3.54 4.33 2.02 1.68
Nb 7.77 8.27 3.42 8.33 4.50 12.32 10.1 5.44 0.13 0.46 13.0 9.15
Ta 0.80 0.79 0.52 0.51 0.98 0.44 0.95 0.34 0.01 0.08 1.06 0.71
Zr 1.69 2.70 0.50 215 459 452 281 958 0.93 1.17 2.82 7.54
Hf 0.12 0.06 0.06 9.10 12.6 7.18 8.29 24.9 0.03 0.09 0.11 0.20
Pb 1.17 n.d. 0.14 3.65 n.d. 4.65 0.21 1.03 2.66 4.48 0.43 n.d.
Th 3.08 4.32 0.95 0.54 1.69 1.88 1.55 0.75 0.29 0.79 3.92 0.28
La 19.9 17.3 2.29 16.1 14.8 9.17 23.3 36.6 39.2 38.3 22.40 4.81
Ce 33.0 29.8 3.85 29.1 32.4 22.6 52.5 84.9 70.2 66.2 40.3 9.42
Pr 3.34 3.21 0.42 3.09 3.87 3.19 6.04 10.0 7.48 7.01 3.68 1.00
Nd 11.5 9.44 1.31 11.1 15.4 12.1 22.4 38.0 25.2 25.2 12.6 3.35
Sm 1.87 1.20 0.07 1.85 2.73 1.94 3.46 6.45 3.48 3.40 1.72 0.64
Eu 0.33 0.19 0.002 0.53 0.68 0.35 0.94 1.95 0.67 0.78 0.30 0.03
Gd 1.19 0.73 0.10 1.76 1.82 1.39 2.51 4.88 1.82 1.81 1.04 0.57
Tb 0.18 0.08 0.02 0.25 0.23 0.14 0.34 0.66 0.19 0.20 0.12 0.07
Dy 0.98 0.31 0.06 1.15 1.15 0.74 1.81 3.67 0.95 0.93 0.45 0.34
Ho 0.19 0.02 0.01 0.16 0.19 0.14 0.30 0.71 0.15 0.13 0.05 0.05
Er 0.48 0.02 n.d. 0.38 0.46 0.36 0.83 1.99 0.24 0.25 0.08 0.10
Tm 0.07 0.001 n.d. 0.06 0.07 0.07 0.13 0.36 0.03 0.03 0.01 0.01
Yb 0.51 n.d. n.d. 0.58 0.52 0.95 1.00 3.39 0.16 0.13 0.03 0.07
Lu 0.09 n.d. n.d. 0.10 0.09 0.19 0.18 0.66 0.02 0.02 0.00 0.01
(La/Yb)N 27.7 — — 19.7 20.2 6.8 16.4 7.6 177.8 202.8 463.3 47.7
6.1. Evolution of the Kovdor-type alkaline ultramafic series
According to the first scenario, which is apparently materialized in the Kovdor-type rock sequence, the olivine melanephelinitic melt A of Figure 10, after having precipitated olivine, will evolve toward the diopside-perovskite cotectic, where perovskite-clinopyroxene cumulates are formed. Early crystallization of a phase that has Dree ^1 will result in a dramatic depletion of residual melt, which will sequentially produce the series of REE-depleted derivatives (ijolites and nepheline syenites). The central role in early extraction of REE from melt was thus played by perovskite, although apatite may also have played a subordinate role at this stage, because it could, in principle, have reached the
liquidus as well. With respect to the Kovdor-type alkaline ultramafic series, evidence for the model just proposed is as follows:
(1) The Afrikanda, Vuoriyarvi, Salmagora, and Cape Turiy massifs contain clinopyroxene-perovskite cumulates composed of primary magmatic perovskite. In some intrusions (Kovdor, Afrikanda, Ozernaya Varaka, Vuoriyarvi), local clinopyroxenite zones with up to 3% primary magmatic apatite have been found.
(2) The latest derivatives of the Kovdor series are sharply depleted in REE, Nb, Ta, and Sr relative to both the mean parental magma composition and to earlier cumulates.
(3) Primary REE-bearing accessories in late differentiates of the Kovdor series are relatively low in REE and Sr due to the melts being depleted in these elements. Thus, apatites from Ozernaya Varaka cancrinite syenites have as little
Table 9. Partition coefficients between the coexisting perovskite, apatite, and titanite in the rocks of the alkaline ultramafic series
DPer/Ap DPer/Ap DPer/Ap DPer/Tit DPer/Tit DAp/Tit DAp/Tit DAp/Tit
Rock PRD PRX MLG PRX IJL PRX MLG IJL
Sample AFR-5 25-AFR 8-OV 25-AFR 8-OV 25-AFR 8-OV 1636/874
La 1.43 0.79 4.08 1.80 8.49 2.27 2.08 2.65
Ce 1.79 1.52 5.01 2.18 6.67 1.43 1.33 1.51
Pr 1.86 1.23 5.20 1.40 5.42 1.14 1.04 1.05
Nd 1.89 1.23 5.11 1.23 4.72 1.00 0.92 0.90
Sm 2.30 1.16 4.49 0.90 3.24 0.78 0.72 0.63
Eu 2.73 0.98 3.94 0.69 2.66 0.71 0.67 0.56
Gd 2.61 1.00 3.12 0.65 2.21 0.65 0.71 0.66
Tb 3.32 0.93 2.87 0.56 1.84 0.60 0.64 0.57
Dy 4.38 0.77 2.43 0.41 1.41 0.53 0.58 0.52
Ho 4.99 0.70 1.97 0.35 1.11 0.51 0.57 0.49
Er 5.67 0.62 1.57 0.28 0.93 0.46 0.59 0.48
Tm 6.58 0.66 1.48 0.27 0.84 0.40 0.57 0.44
Yb 8.77 0.58 1.42 0.24 0.87 0.42 0.61 0.44
Lu 7.69 0.46 1.61 0.22 1.01 0.48 0.63 0.51
as 0.67-0.71 LREE2O3 and 0.60-0.68 wt % SrO, and those from Maly Kovdor nepheline syenites, as little as 0.33-1.31 LREE2O3 and 0.59-1.07 wt % SrO [Arzamastseva and Arza-mastsev, 1996].
Data on REE distribution in alkaline intrusions of various provinces indicate that early fractionation of REE-bearing phases is a characteristic feature of alkaline ultramafic suites. Thus, the Oldoinyo Lengai plutonic suite has been reported to comprise clinopyroxenite (jacupirangite) cumulates with up to 28% perovskite [Dawson et al., 1995]. The character of REE distribution in the Oldoinyo Lengai rocks corresponds exactly to that in the Kovdor series: REE are enriched in early cumulates and sharply depleted in terminal members
Figure 9. Whole rock/perovskite partition coefficients for alkaline ultramafic rocks, using data from Table 10. Coefficients for perovskite in alkaline volcanites from other regions (analysis 1, heavy line), from [Onuma et al., 1981].
of the series (ijolites and eucolite-bearing Ne-syenites). Another example is provided by the Maimecha-Kotui province, where the Kugda, Guli, and Odikhincha massifs are reported to contain olivine and clinopyroxene cumulates rich
Figure 10. Melting diagram for the system nephelines-diopsides-titanite, after [Veksler and Teptelev, 1990]. Di -diopside, Prv - perovskite, Ttn - titanite, Mel - melilite, Cg - carnegieite, Ne - nepheline, Ol - olivine, L1 + L2 -immiscibility region. Point A signifies the weighted mean composition for the Kovdor-type primary alkaline ultra-mafic magma. Point A1 represents the hypothetical primary magma of the Khibiny-type alkaline ultramafic series, whose composition has been changed by mixing with phonolitic melt.
Table 10. Mineral/rock partition coefficients in pyroxene and olivine cumulates of the alkaline ultramafic series
Perovskite Apatite
Rock PRX PRD PRX PRX PRX PRX PRX
Sample 25-AFR AFR-1 282/224 205/297.5 282/251 25-AFR AFR-5
La 9.5 26.7 14.9 6.7 12.4 12.0 2.4
Ce 12.4 37.1 18.4 9.2 17.1 8.1 2.0
Pr 7.9 29.3 17.7 10.1 16.8 6.4 1.8
Nd 7.0 26.5 17.7 10.7 16.7 5.7 1.7
Sm 6.8 19.3 16.4 9.5 14.7 5.9 1.8
Eu 7.0 18.6 17.6 9.7 15.1 7.2 2.2
Gd 6.3 17.4 16.0 9.0 13.9 6.2 2.4
Tb 5.8 14.9 14.3 7.6 12.2 6.3 2.3
Dy 4.2 8.8 11.1 4.8 7.7 5.5 2.0
Ho 3.5 6.2 7.9 3.7 5.9 4.9 1.9
Er 2.4 4.3 5.7 2.5 4.1 3.9 1.7
Tm 2.0 3.1 4.2 1.9 2.8 3.1 1.5
Yb 1.5 2.7 3.5 1.5 2.4 2.6 1.0
Lu 1.1 2.0 2.7 1.2 1.7 2.3 0.9
Notes. DPrv/Rock and D^p/Rock were calculated with respect to the weighted mean composition of the alkaline ultramafic series (see AVER* in Table 4).
full spectrum of alkaline ultramafites, including clinopyrox-ene cumulates with as much as 15% perovskite [Chernysheva et al., 1990].
6.2. Evolution of the Khibiny-type alkaline-ultramafic series
The set of rock varieties that make up fragments of the alkaline ultramafic suite in the Khibiny massif, the order of their formation, and overall major-element characteristics were formerly believed to suggest similar courses of REE evolution and distribution for the Khibiny and Kovdor suites. However, according to geologic observations and geochemical data for the Khibiny alkaline ultramafic suite, generation of early olivine and clinopyroxene cumulates was not accompanied by massive precipitation of perovskite. This is the reason why REE remained in residual melt until final stages of crystallization, and REE enrichment did not occur until late ijolite derivatives started to form. Two factors preventing early crystallization of perovskite can be considered, both of them being apparently related to a drastic increase in silica activity in the melt. Firstly, the change in SiO2 activity may result from interaction of the primary olivine melanephelinitic magma with surrounding Precam-brian basement rocks. This, however, is at variance with Sr and Nd isotope data, which suggest that crustal material was not involved in alkaline magmagenesis in the Kola province [Kramm and Kogarko, 1994]. Secondly, the change in SiO2 activity may have been caused by mixing of the olivine melanephelinitic magma with a more silicic melt. A likely candidate for such a melt might be the phonolitic magma that gave rise to the Khibiny agpaitic plutonic suite. This suite, according to isotope geochemical and petrologic
in primary magmatic perovskite [Egorov, 1991]. The Nizh-nesayansky carbonatite massif (southern Siberia) has also been reported to incorporate a rock suite encompassing the
Figure 11. Melting diagram for the system nephelines-diopsides-apatite, after [Kogarko, 1990]. Di - diopside, Ap - apatite, Pho - Ca-phosphate, Mel - melilite, Cg -carnegieite, Ne - nepheline, Ol - olivine, L1 + L2 - immis-cibility region. Point A signifies the weighted mean composition for the Kovdor-type primary alkaline ultramafic magma, and point A1 , the hypothetical composition for the primary magma of the Khibiny-type alkaline ultramafic se-
ARZAMASTSEV ET AL.: RARE EARTH ELEMENTS IN ROOKS AND MINERALS Table 11. Mineral/rock partition coefficients in melilitic rocks and ijolites of the alkaline ultramafic series
Apatite Titanite Clinopyroxene Melilite
Massif SLN SLN KVD OZV KHI OZV KHI KHI OZV KVD KVD KHI KVD KVD
Rock IJL IJL IJL MLG IJL MLG IJL IJL MLG IJL MELT IJL MELT MELT
Sample 25/110 31/200 7/30 8-OV 1636/721 8-OV 301/500 1636/721 8-OV 7/30 252/100 301/500 252/100 227/43
La 4.56 5.72 25.57 15.54 8.81 7.46 8.83 1.87 0.14 0.17 0.35 0.34 0.90 1.37
Ce 4.55 5.27 25.96 14.04 8.26 10.55 10.70 2.98 0.17 0.19 0.43 0.37 0.87 1.33
Pr 4.55 5.06 26.64 12.45 7.90 11.94 12.32 4.06 0.18 0.24 0.48 0.40 0.87 1.31
Nd 4.39 4.81 27.11 11.34 7.86 12.27 12.85 4.60 0.19 0.26 0.56 0.43 0.92 1.26
Sm 4.08 3.99 26.51 9.97 7.13 13.83 13.64 5.82 0.23 0.33 0.73 0.45 0.91 1.29
Eu 3.94 3.86 26.39 11.18 7.16 16.56 14.83 6.39 0.26 0.24 0.82 0.49 0.93 1.28
Gd 3.94 3.94 25.81 8.64 7.62 12.21 12.70 5.84 0.23 0.40 0.88 0.43 0.88 1.12
Tb 3.52 3.24 25.27 8.47 6.85 13.22 12.80 6.08 0.26 0.38 1.06 0.45 0.91 1.15
Dy 3.28 2.48 26.89 8.64 6.69 14.94 13.82 6.59 0.34 0.50 1.27 0.56 1.03 1.34
Ho 3.04 2.61 23.32 8.82 5.82 15.61 12.96 6.20 0.36 0.53 1.39 0.63 0.97 1.21
Er 2.84 2.35 16.89 8.18 4.91 13.77 12.20 5.64 0.44 0.51 1.44 0.82 0.80 0.88
Tm 2.50 2.03 14.50 7.04 3.44 12.43 11.68 4.32 0.51 0.67 1.67 1.23 0.65 0.76
Yb 2.22 1.47 9.97 6.53 2.23 10.64 10.07 2.62 0.66 1.32 2.22 2.22 0.57 0.63
Lu 2.02 1.18 6.29 4.67 1.28 7.47 9.61 1.44 0.72 1.56 3.38 3.80 0.69 0.53
Notes. D^p/Rock, DTtn/Rock, Dgpx/Rock and DjMel/Rock were calculated from the ratios of REE abundances in rocks and mineral phases contained in them.
data [Arzamastsev et al., 1998; Kramm et al., 1993], evolved independently, and its origin is related to a mantle source other than that of alkaline ultramafic melts. The main feature of agpaitic melts is their relatively higher SiO2 (52-56 wt %), alkali (Na2O + K2O > 16 wt %), and F contents. However, REE contents in agpaitic syenites, according to our data [Arzamastsev et al., 2001a], are only a little higher than in alkaline ultramafites. Hence, addition to the primary silica-undersaturated melanephelinitic magma of even minor batches of phonolitic melt would increase silica and alkali contents of the magma while changing its REE content only slightly. Indeed, in comparison to Vuoriyarvi, Ozernaya Varaka, Sallanlatva, and Kovdor ijolites, their Khibiny counterparts are much higher in SiO2, Na2O, and K2O (Tables 2, 3), and feldspar-bearing varieties are widespread among them. In the nepheline-diopside-titanite melting diagram (Figure 10), the change in the composition of crystallizing melt will be expressed in that the initial liquid of composition A shifts away from the perovskite cotectic surface A1 to produce perovskite-free olivine-diopside, diopside-melilite, and diopside-nepheline rocks (option A1 -B1-C1). Accordingly, REE will be enriched progressively in these differentiates, and extraction of REE from melt will not occur until the melt has reached the apatite and/or titanite liquidus surface at the final stages of alkaline ultramafic petrogenesis. Therefore, evolution of the alkaline ultramafic series in the Khibiny massif was disturbed by mixing of minor portions of phono-litic melt with the primary olivine melanephelinitic magma, which led to a change in crystallization order of REE-bearing titanates and Ti-silicates and enrichment of late batches of melt in the majority of incompatible elements.
7. Conclusions
Our study of REE distribution in rocks and minerals of Paleozoic alkaline ultramafic rocks of the Kola province affords the following conclusions:
(1) REE patterns in rocks of the Kovdor, Afrikanda, Vuoriyarvi, and Salmagora massifs indicate a systematic depletion from earlier to later (ijolite and nepheline syenite) melt derivatives. Analysis of rock suites to be found in alkaline intrusions of other provinces (Maimecha-Kotui province of southern Siberia and East African province) shows that the above trend has a general character, inherent in many alkaline ultramafic suites.
(2) REE distribution in Kovdor-type alkaline ultramafic suites is controlled by crystallization of perovskite and, to a lesser extent, apatite. Primary olivine melanephelinitic melts of this series experienced crystallization of perovskite, the main REE-bearing mineral. Perovskite coprecipitating with the first phases to crystallize from melt, olivine and clinopyroxene, leads to a dramatic REE depletion of the residual melt and to formation of REE-depleted derivatives, ijolite and nepheline syenite.
(3) Petrogenesis of the alkaline ultramafic suite of the Khibiny massif was upset by mixing of minor batches of phonolitic melt with the primary olivine melanephelinitic magma, with an ensuing change in the crystallization order of REE-bearing titanates and Ti-silicates and enrichment of late batches of melt in the majority of incompatible elements. As a result, Khibiny ijolites, which are late and the most evolved derivatives of the alkaline ultramafic
magma, have the highest REE concentrations, accommodated by high-REE apatite and titanite.
Acknowledgments. This work would have been impossible without the painstaking and crucial procedure of mineral separation, which was performed by Lyuda Koval, and microprobe analyses of accessory mineral grains, carried out by Yakov Pakho-movsky. The study was supported by the Russian Foundation for Basic Research (project no. 00-05-64229).
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(Received 6 May 2002)
