07 buda.indd Buda et al.: Mafi c enclaves in peraluminous Variscan granitoid in the Battonya Unit from Southeast Hungary 243 � AB STRA CT Variscan granitoids occur in the southeastern part of the Tisza Mega Unit of Hungary. The presence of amphibole, calc-alkaline-type Mg-rich biotite in metaluminous basic enclaves, and muscovite and Fe-Al-biotite in peraluminous granitoids, suggests a mixed I-S-type origin. Two types of muscovite have been identifi ed: a primary euhedral to sub- hedral, Ti-Na-Al rich variety, crystallized after Fe-rich peraluminous biotite in the two-mica granite and in muscovite granite, and a secondary subhedral Si enriched and Mg-bearing, Ti-poor mica formed as a hydrothermal alteration product of feldspars, and is present in all rock types. Given the compositional continuum of “white micas”, we sug- gest that magmatic crystallization was followed by autometasomatic and hydrothermal activity, due to a water-rich liquid trapped in the rock during the fi nal stages of magmatic activity. Based on the bulk composition of the prevail- ing rock-type, the abundance of primary muscovite, the majority of the granitoid magma crystallized from a water- saturated peraluminous melt for which the pressure was 490–600 MPa, the temperatures were 650–685 °C and the depth of the intrusion was a minimum of 15 km. Keywords: basic enclave, peraluminous granitoid, Variscan, I/S-type, primary-, secondary muscovite, P, T, depth of intrusion, SE Hungary Mafi c enclaves in peraluminous Variscan granitoid in the Battonya Unit from Southeast Hungary � György Buda1, Elemér Pál-Molnár2 and Friedrich Koller3 1 Department of Mineralogy, Eötvös Loránd University, H-1117 Budapest, Pázmány P. st. 1/C, Hungary; (buda@ludens.elte.hu) 2 Department of Mineralogy, Geochemistry and Petrology, University of Szeged, H-6701 Szeged, P.O. Box 651, Hungary; (palm@geo.u-szeged.hu) 3 Department of Lithospheric Research, University of Vienna, A-1090 Vienna Althanstrasse 14, Austria; (friedrich.koller@univie.ac.at) doi: 104154/gc.2012.15 Geologia Croatica 65/2 243–253 8 Figs. 3 Tabs. Zagreb 2012 Geologia CroaticaGeologia Croatica 1. INTRODUCTION Variscan granitoids occur in the Carpathian Basin (Hun- gary). The present geology and tectonic setting of the Car- pathian or Pannonian Basin (fi g. 1/A), are the result of a multi-step evolution of geological structures (HAAS et al., 2000; KOVÁCS et al., 2000, HAAS et al., 2004; SCHMID et al., 2008 ). The complexity is due to the tectonic position of the ter- ritory. It is situated in the collision zone of the European and African continental plates. The history began with spread- ing, followed by a series of collisions. During the Alpine orogenesis, the drifting and welding of the individual frag- ments was accompanied by folding processes and nappe for- mation. At the end of the Miocene, attenuation of the crust (upward bulging of the mantle) resulted in the development of a large basin that determines the present structural setting of the area. The greatest proportion of the Pre-Neogene basement of the Pannonian Basin is composed of two megatectonic units: in the north the ALCAPA Mega Unit (the southern part of which is named the Pelso Composite Unit) and in the south Geologia Croatica 65/2Geologia Croatica 244 the Tisza Mega Unit (TMU, KOVÁCS et al. 2000) or Tisia Composite Terran (KOVÁCS et al., 2010). In the Hungarian part of the Variscan TMU (fi g. 1/B) two types of granitoids can be distinguished: an older (354 Ma, KLÖTZLI et al., 2004) deep-seated metaluminous and slightly peraluminous, K- and Mg-rich, I- and allanite-type granitod, with K-Mg-rich basic durbachitic enclaves (BUDA et al., 2004/a), occurring in the southwest part of the TMU outcropping in the Mórágy Unit (Mecsek Mts) and a slightly younger granitoid which is mostly strongly peraluminous with mafi c enclaves, I/S- and monazite-type (BUDA et al., 2009) in the southeastern part of the TMU located in the characteristic uplift of the basement of the Battonya Unit, studied only from oil prospecting drill-core samples. One of the main purposes of this study to distinguish primary mus- covite from secondary muscovite in the peraluminous gran- itoid in order to estimate the P/T of crystallization and the depth of intrusion of the Battony granitoids. For this estima- tion it was important to prove the presence of primary mus- covite in these altered rocks because the breakdown curve of primary muscovite (CLARKE et al., 2005), which inter- sects the experimentally determined watersaturated peralu- minous granite solidus (JOHANNES & HOLTZ), can give a rather good estimation for the physical parameters of crys- tallization and depth of intrusion. Due to the volatile enriched environment, subsolidus muscovite is also widespread; con- sequently we had to use different criteria to distinguish them from primary muscovite. The role of basic enclaves in the peraluminous granitoid is not clear, and requires further re- search. 2. OUTLINE OF GEOLOGICAL SETTING The TMU comprises the crystalline basement of south Hun- gary, east Croatia, north Serbia, and the western part of Transylvania (Romania, Fig.1/A). It is bordered by the Mid Hungarian Lineament, the Szá va -Mosla vima -Zombor- Bečej-Lipova line, (the Northern border of the Srem – Mureş ophiolite belt), and the Someş lineament in the Northwest, South and Northeast, respectively. As a consequence of the fact that at present, the basement is covered by 1000–6500 m of Miocene-Pliocene sediments, its structure and petrol- ogy can only be investigated by geophysical methods and borehole samples. The seismic research of the past decades has shown that during the Neogene, the Pannonian Basin underwent a complex tectonic evolution that has principally modifi ed the original Variscan structures of the area (TARI et al., 1999; CSONTOS et al., 1999). As an independent unit, the TMU existed from the Late Cretaceous, when its rotation began, until the Early Miocene (CSONTOS, 1995; MÁRTON, 2000, 2001; KOVÁCS et al., 2000). Separation from the Moldanubian Zone of Variscan Figure 1: A – Sketch map of the main tectonic units of Central Europe (CBP= Central Bohemian Pluton, SBP=South Bohemian Pluton, MHL=Mid Hunga- rian Lineament). B – Structural units of the Hungarian part of the Tisza Mega Unit. Inset: simplifi ed geological map of Békesian Composite Unit after KOVÁCS et al. (2000), modifi ed by PÁL-MOLNÁR et al. (2001). C. Location of bore-holes of the Battony Unit. Buda et al.: Mafi c enclaves in peraluminous Variscan granitoid in the Battonya Unit from Southeast Hungary Geologia Croatica 245 Europe started in the Late Triassic–Early Cretaceous, as re- corded by crystalline rocks (BUDA et al., 2004/b) and sedi- mentary sequences (HAAS et al., 2004; CSONTOS et al., 2004; SCHMID et al., 2008). The Hungarian part of the TMU is called the Kunságia Composite Unit and the Béké- sia Composite Unit (BCU). The BCU can be divided into four units: Kelebia, Csongrád, Battonya, and Sarkadkeresz- túr (fi g. 1/B). The areas of interest are located in the BCU, which is part of the Békés-Codru Alpine Zone (HAAS et al., 2004). The Battonya Unit is a 15–25 km long and 10–15 km wide body forming a fl at anticline covered by 1000–1500 m of Miocene and Pannonian sediments. The present study fi rst of all deals with the genesis of “white micas” of mostly two-mica and muscovite granitoids, occurring in the uplifted basement of the Battonya Unit. These plutonic rocks are surrounded by regional metamor- phic and migmatitic rocks and are partly covered by Alpine sequences. The rocks were metamorphosed at about 6–700 MPa and 500–570°C (350–330 Ma) and are locally affected by dynamo- and retrograde metamorphism (330–315 Ma) according to SZEDERKÉNYI (2001). 3. SAMPLING AND ANALYTICAL METHODS The studied samples were obtained from boreholes of the Battonya Unit around the Battonya and Mezőhegyes (Fig. 1/C/I., II.) settlements. The rocks were acquired from the rock collection of the Department of Mineralogy, Geochem- istry and Petrology of the University of Szeged. The samples are drill-cores and consequently their numbers are limited. The major and trace element analyses of the rocks were carried out using ICP-AES methods at the University of Stockholm and at ALS Chemex in Canada (Vancouver). Most of the analyses were published by PÁL-MOLNÁR et al. (2001). Detection limits for major components are 0.01Wt %, FeO content was determined by titrimetric and H2O– and H2O+ by gravimetric methods. Major element com- positions of minerals were determined by a CAMECA SX- 100 electron probe X-ray microanalyser at the Department of Lithospheric Research of the University of Vienna. Dur- ing the measurements an accelerating voltage of 15 kV and a beam current of 10 nA were used. A beam size of 1–2 μm was used for amphiboles, micas and other minerals, for feld- spar minerals a beam size of 5 µm was used. The counting time was for each element ranged from 20–40 sec. For cali- bration, well defi ned mineral standards were used (quartz for Si, rutile for Ti, almandine for Al and Fe, a chromite for Cr, spessartine for Mn, olivine for Mg, wollastonite for Ca, al- bite for Na and an orthoclase for K). Afterwards, standard ZAF corrections were applied. Approximately 500 spot anal- yses were carried out. We analyzed 3 to 5 points in each min- eral grain, but in the case of zoned crystals, as many as 20– 30 points were analyzed, depending on the number of distinguishable zones. 4. PETROGRAPHY The Battonya granitoid has light greenish grey, grey and pinkish grey colours. It is generally medium-grained, equi- granular, sometimes with pinkish microcline megacrysts. The majority contains biotite and/or muscovite. Three rock types have been distinguished: Type I.: quartzmonzodiorite (Fig. 2/A, I.) is the green- ish grey variety containing amphibole and biotite but no pri- mary muscovite. The chemical composition is mostly meta- luminous or slightly peraluminous (Fig. 2/B, I.).They are most probably basic enclaves in the prevailing two mica and muscovite granitoid pluton . Amphiboles form large euhedral and subhedral crystals or aggregates. The large amphibole is zoned; the core is Mg- Figure 2: A – Rock classifi cation: I. Quartzmonzodiorite; II. Granodiorite; III. Granite; (DEBON et al., 1983). B – A/CNK v. A/NK of Battonya granitoids (I. Quartz- monzodiorite; II. Granodiorite III.Granite; after SHAND, 1947). Geologia Croatica 65/2Geologia Croatica 246 Biotite is subhedral, Mg-rich (Fe/ (Fe + Mg) = 0.31, Ta- ble II.) and Al poor (Al = 2.84 pfu) with phlogopitic (Fig. 3/B, I.) composition, having a calc-alkaline (ABDEL-RAH- MAN, 1994; BUDA et al., 2004/c) chemical character (Fig. 3/C, I.). Sometimes biotites occur as anhedral patches in amphi- bole showing replacement texture. Alteration of biotite to chlorite is common. Primary muscovite is absent but a sec- ondary variety (sericite) is common in plagioclase. The pla- gioclases have oscillatory zoning between andesine (An43–40, Fig. 3/D) and oligoclase (An17–13) with secondary albitization and sericitization. Sometimes unzoned oligoclase (An17–10) can also be observed. A cross-hatched microcline is present but not common; it shows replacement texture without perthitic exsolution and has a low Na content (Or94, Fig. 3/D, insert). Quartz is de- formed with wavy extinction, and secondary calcite is ob- served. Accessory minerals are acicular apatite, zircon and rare monazite. Type II and type III: granodiorite and granite (Fig. 2/A, II, III.). These granitoids are the most common. Differences between the granodiorite and granite are not well defi ned because autometasomatism, and hydrothermal processe s ob- scure the primary rock and mineral compositions (e.g., the K-feldspar/plagioclase ratio). Granodiorite-granite is grey with either biotite and muscovite or with muscovite alone, and sometimes contains microcline megacrysts. These rocks are strongly peraluminous (Fig. 2/B II., III., A/CNK = 1.1– 1.7, CIPWavg corundum = 4). In the two mica granitoid the biotite is Fe-rich (Fe/ (Fe + Mg) = 0.58, Table II, Fig. 3/B, II.) and strongly pleochroic (γ, = dark brown α, = yellowish brown) with peraluminous (Al = 3.02 pfu) compositions (Fig. 3/C, II.) and sometimes entirely altered to chlorite. Euhedral or subhedral large primary muscovite is common. Sometimes muscovite grew across the biotite (Fig. 4/1, 2) indicating later crystallization from an Al-rich water-satu- rated melt . According to MILLER et al. (1981), Al-rich biotite (>3.00 Al pfu) coexists with quartz, K-feldspar, and Na-pla- gioclase in peraluminous granite. The plagioclase is sometimes oscillatory zoned. The co- res are mostly oligoclase (An25–18, fi g. 5/A) and the rims are albite (An2–0) in the two mica granitoid and the muscovite granitoid, the plagioclases are richer in Na (An18–0, fi g. 5/B ). The plagioclase cores are strongly sericitized or altered to clay minerals, partly replaced by cross-hatched microcline and albite. Albite and microcline with low Na (Or95–97) is widespread, occurring in replacement textures. Secondary albite also forms vein fi llings. Sometimes large primary al- bite (An3–4) is replaced partly by microcline (e.g. two-mica granite). Maximum or nearly maximum microcline (Δ = 0.74, BUDA, 1975) occurs as megacrysts with low Na con- tent (Or95–98) indicating a low crystallization temperature and slow rate of cooling. Quartz is ubiquitous and displays wavy extinction; it also occurs as myrmekite in plagioclase. Stubby apatite, zircon, and monazite crystals are common accessory minerals. Table I: Representative compositions of amphiboles from Battonya Unit determined by electron microprobe. Battonya N-2   1 2 3 4 5 6 7 SiO2 46.55 50.61 51.93 51.69 51.02 50.93 52.83 TiO2 0.66 0.30 0.27 0.16 0.25 0.22 0.25 Al2O3 9.42 5.87 4.85 4.97 5.52 5.90 4.27 FeO 11.15 9.23 8.69 8.48 8.90 9.30 8.43 Cr2O3 0.20 0.10 0.02 0.07 0.08 0.16 0.00 MnO 0.46 0.38 0.35 0.33 0.33 0.37 0.27 MgO 14.56 16.75 17.39 17.38 16.96 16.65 17.31 CaO 12.05 12.47 12.67 12.61 12.75 12.59 12.53 Na2O 1.34 0.76 0.59 0.73 0.76 0.78 0.54 K2O 0.45 0.33 0.22 0.18 0.21 0.25 0.17 Total 96.84 96.80 96.97 96.60 96.77 97.13 96.60 Structural formulae calculated on an anhydrous basis of 23 (O) TSi 6.823 7.299 7.434 7.426 7.343 7.316 7.559 TAl 1.177 0.701 0.566 0.574 0.657 0.684 0.441 Sum_T 8 8 8 8 8 8 8 CAl 0.450 0.295 0.254 0.266 0.279 0.314 0.280 CCr 0.024 0.011 0.002 0.008 0.009 0.018 0 CTi 0.073 0.033 0.029 0.018 0.027 0.024 0.028 CMg 3.181 3.600 3.711 3.722 3.639 3.565 3.691 CFe2 1.273 1.061 1.005 0.987 1.046 1.079 0.997 CMn 0 0 0 0 0 0 0.005 Sum_C 5 5 5 5 5 5 5 BFe2 0.094 0.053 0.036 0.032 0.025 0.038 0.012 BMn 0.057 0.046 0.042 0.040 0.041 0.045 0.028 BCa 1.849 1.901 1.922 1.928 1.934 1.918 1.921 BNa 0 0 0 0 0 0 0.039 Sum_B 2 2 2 2 2 2 2 ACa 0.043 0.026 0.022 0.013 0.032 0.019 0 ANa 0.381 0.213 0.165 0.203 0.211 0.216 0.111 AK 0.084 0.061 0.041 0.034 0.038 0.045 0.032 Sum_A 0.509 0.300 0.229 0.250 0.281 0.281 0.143 Sum_cat 15.509 15.300 15.229 15.250 15.281 15.281 15.143 1. Core of the large grain. 2. Outer zone of a large grain. 3. Larger crystal. 4–6. Small acicular grains. 7. Small acicular grain. hornblende with a low Si (6.823 pfu) and high Al (1.627 pfu, A/CNK = 0.70), Ti (TiO2 = 0.66 Wt %), and Cr (Cr2O3 = 0.2 Wt %) content (table I.). According to HOLLAND & BLUNDY’s (1994) amphibole-plagioclase thermometer, it formed about 700°C and at 440 MPa pressure (ANDERSON et al., 1996). The rim is actinolite (Fig. 3/A) which addition- ally forms small aggregates (A/CNK=0.31–0.45). It probably formed at similar P/T conditions to secondary muscovite . Buda et al.: Mafi c enclaves in peraluminous Variscan granitoid in the Battonya Unit from Southeast Hungary Geologia Croatica 247 Table II: Representative compositions of biotites from Battonya Unit determined by electron microprobe.   biotite coexists with amphibole biotite coexists with muscovite   Battonya N-2 aver- age Mezőhegyes-5 aver- age   1 2 3 4 5 6 7 8   9 10 11 12 13 14   SiO2 38.99 39.17 38.79 37.51 37.90 38.02 38.00 38.21 38.32 34.88 35.49 34.64 34.89 35.09 35.16 35.02 TiO2 1.45 1.89 2.16 1.84 1,64 1.98 2.03 2.19 1.90 3.33 3.18 3.51 3.36 3.62 3.56 3.42 Al2O3 16.16 16.34 16.12 16.30 16.23 16.33 16.39 16.27 16.27 16.59 16.21 16.70 16.60 16.46 16.22 16.46 Cr2O3 0.00 0.00 0.00 0.12 0.14 0.06 0.06 0.04 0.05 0.02 0.01 0.01 0.02 0.00 0.02 0.01 FeO 13.44 12.15 12.63 13.41 13.07 12.02 12.19 11.78 12.59 21.46 21.08 21.67 21.32 21.24 21.58 21.39 MnO 0.21 0.19 0.16 0.23 0.23 0.22 0.20 0.21 0.21 0.32 0.31 0.35 0.33 0.34 0.29 0.32 MgO 14.68 14.93 14.88 15.20 15.40 15.63 15.74 15.94 15.30 8.64 8.67 8.45 8.52 8.36 8.27 8.49 BaO 0.00 0.00 0.00 0.12 0.08 0.15 0.23 0.18 0.09 0.29 0.16 0.23 0.30 0.35 0.31 0.27 CaO 0.00 0.04 0.02 0.03 0.01 0.02 0.01 0.01 0.02 0.00 0.03 0.01 0.02 0.00 0.02 0.01 Na2O 0.11 0.13 0.09 0.07 0.10 0.09 0.10 0.09 0.10 0.14 0.11 0.14 0.11 0.10 0.09 0.11 K2O 9.90 9.94 9.98 9.24 9.50 9.70 9.79 9.69 9.72 9.57 9.14 9.43 9.52 9.44 9.50 9.43 Total 95.94 94.78 94.80 94.08 94.30 94.20 94.74 94.63 94.56 95.23 94.37 95.12 94.98 95.00 95.01 94.95   Structural formulae calculated on an anhydrous basis of 22 (O) Si 5.778 5.777 5.740 5.619 5.657 5.658 5.634 5.653 5.689 5.420 5.528 5.392 5.431 5.456 5.475 5.450 AlIV 2.222 2.223 2.260 2.381 2.343 2.342 2.366 2.347 2.311 2.580 2.473 2.609 2.569 2.544 2.525 2.550 AlVI 0.598 0.615 0.550 0.493 0.509 0.519 0.495 0.488 0.533 0.456 0.500 0.452 0.474 0.470 0.449 0.467 Ti 0.162 0.210 0.240 0.208 0.184 0.222 0.226 0.244 0.212 0.389 0.372 0.411 0.393 0.424 0.417 0.401 Fe2 1.666 1.499 1.563 1.680 1.632 1.495 1.512 1.458 1.563 2.789 2.746 2.820 2.775 2.762 2.810 2.784 Cr 0.000 0.000 0.000 0.015 0.016 0.007 0.008 0.005 0.006 0.003 0.001 0.002 0.002 0.000 0.002 0.001 Mn 0.026 0.024 0.020 0.029 0.029 0.027 0.025 0.027 0.026 0.042 0.040 0.046 0.043 0.045 0.038 0.042 Mg 3.243 3.283 3.282 3.395 3.425 3.467 3.480 3.517 3.387 2.002 2.012 1.960 1.978 1.938 1.920 1.968 Ba 0.000 0.000 0.000 0.007 0.005 0.008 0.014 0.011 0.006 0.017 0.010 0.014 0.018 0.022 0.019 0.017 Ca 0.000 0.006 0.003 0.005 0.001 0.004 0.001 0.001 0.003 0.000 0.005 0.002 0.003 0.000 0.003 0.002 Na 0.032 0.037 0.025 0.021 0.030 0.025 0.028 0.027 0.028 0.042 0.034 0.041 0.034 0.030 0.027 0.035 K 1.872 1.870 1.885 1.766 1.809 1.841 1.852 1.830 1.840 1.898 1.816 1.873 1.890 1.873 1.887 1.873 Cations 15.599 15.544 15.565 15.619 15.640 15.615 15.641 15.607 15.604 15.638 15.534 15.619 15.611 15.561 15.572 15.589 Fe/ FeMg 0.340 0.310 0.320 0.330 0.324 0.300 0.302 0.293 0.315 0.580 0.580 0.590 0.583 0.585 0.590 0.585 1. – Small crystal with amphiboles. 2–6. –Small crystals near to amphiboles. 7–8. – Large crystals with amphiboles. 9–14. – Large crystals with musco- vite sometimes transecting by muscovite. 5. WHITE MICA PETROGRAPHY AND CHEMISTRY We distinguished the primary (magmatic) muscovite from secondary muscovite in order to obtain information of the P/T conditions of crystallization and depth of the intrusion of a mainly peraluminous granitoid melt in the Battonya area, where knowledge is limited as these rocks are only studied in drill-cores from 1000–1500 m depth. There are textural and chemical criteria for distinguish- ing primary (magmatic) muscovite from secondary musco- vite (SPEER, 1984): 1) Textural criteria: the grains of pri- mary muscovite are subhedral to euhedral with sharp grain boundaries; grain sizes are similar to those of other, coexist- ing magmatic minerals. Often the textural evidence is uncer- tain, and chemical criteria are also needed. 2) Chemical cri- teria: the magmatic muscovite is enriched in Ti, Na, and Al and contains lower amounts of Si and Mg compared to sec- ondary muscovite. Primary and secondary muscovites can be distinguished in the granite-granodiorite of the Battonya Unit based on these criteria. The primary muscovite grains are large, up to a few mil- limetres in size, with euhedral and subhedral outlines. In the two-mica granitoids they usually grew across biotite (Fig. 4./1,2) , and in the muscovite granite they also form large euhedral and subhedral grains with sharp boundaries that clearly separate them from the grain boundaries of neighbor- ing minerals, such as feldspars and quartz (Fig. 4./3). The secondary muscovites are smaller than the primary grains Geologia Croatica 65/2Geologia Croatica 248 Figure 3: A – Amphibole composition of quartzmonzodiorite. B-C – Plot of biotite composition coexisting with amphibole (I) and muscovite (II). B – Pla- gioclase and microcline composition of quartzmonzodiorite. (100–250 μm or less), and have subhedral shapes and, in most cases, they occur in plagioclases or microcline as al- teration products (Fig. 4./4–7), usually together with second- ary anhedral albite and microcline . Chemically, the primary muscovite (Fig. 6) has more Ti (Table III, avg.: 0.12 pfu), Na (avg.: 0.14 pfu), and Al (avg.: 5.21 pfu) and less Mg (avg.: 0.20 pfu) and Si (avg.: 6.16 pfu) than the secondary muscovite, which has avg.: Ti 0.05 pfu, Na 0.07 pfu, Al 5.06 pfu, Mg 0.28 pfu, Si 6.28 pfu. A high Ti content is a good indicator of primary muscovite because it is not affected by secondary processes such as subsolidus oxidation or exchange of cations (ZEN, 1988). The Mg, Fe, Na, Al, and Si contents of the two types of muscovite can overlap according to SPEER (1984). A very slight enrich- ment in Fe can be observed in the secondary muscovite (Fe in secondary: 0.46 pfu; Fe in primary: 0.43 pfu). According to MONIER et al. (1984), the ratio of Na/ (Na+K) is also a good indicator for distinguishing the origin of muscovite (primary: Na/(Na+K) = 0.06–0.12; post- and late-magmatic: 0.01–0.07; hydrothermal: < 0.04). In the case of the Battonya granitoids, primary muscovite has a higher Na/(Na+K) ratio (0.07) compared to secondary muscovite (0.04, Table III). Therefore the primary muscovites can be distinguished from secondary muscovite both texturally and compositionally. Textures show that primary muscovite crystallized from the melt after biotite. The secondary muscovite originated by low-temperature hydrothermal processes compared with late- to post-magmatic muscovites. The primary (magmatic) muscovite crystallization was followed by secondary (sub- solidus) mica formation as a continuous postmagmatic pro- cess during the Variscan orogeny. This is also supported by K/Ar, Sr/Rb ages (average white mica age 350–330 Ma) published by SZEDERKÉNYI (2001). 6. DISCUSSION AND CONCLUSION The relationhip of quartzmonzodiorite to the two mica and muscovite granitoid is not clear but it is most probably a ba- sic enclave showing I-type characters e.g. low initial 87Sr/86Sr330Ma ratio (0.7005) and the presence of amphibole. Similar enclaves are known in the other variscan granitoids in Hungary (Mórágy Unit) or in the other granitoids of Moldanubian zone of the Variscan orogenic belt. The average composition of the Battonya granite-grano- diorite generally corresponds to the composition of the water- saturated peraluminous near eutectic granite melt called “gran- ite low” (Fig. 7/A, WINKLER et al., 1974, CLARKE, 1992). Magmatic cordierite, andalusite was not present due to the water-saturated high pressure melt. The two-mica gran- ite could crystallize according to the following equation: biotite + muscovite + quartz = cordierite (andalusite) + K-feldspar + H2O Buda et al.: Mafi c enclaves in peraluminous Variscan granitoid in the Battonya Unit from Southeast Hungary Geologia Croatica 249 Figure 4: 1, 2 – Backscattered electron images of coarse, subhedral, clearly terminated primary muscovite [Mu(p)] grown across slightly chloritized Al- rich biotite (Bi). 3 – Coarse grained euhedral primary muscovite. 4,5,6 – Subhedral small grains of secondary muscovite [(Mu(s)] in plagioclase (Pl). 7 – Coarse grained secondary muscovite in plagioclase. Geologia Croatica 65/2Geologia Croatica 250 Figure 5: Plot of plagioclase and microcline composition in two mica (A) and in muscovite granitoid (B). Figure 6: Composition of muscovite in two mica (A) and muscovite grani- toids (B). I, II. fi elds according to MONIER et al. 1986. Figure 7: A – Plot of Battonya granitoid in "granite low" system (I. Isotherm at 685oC projected on a cotectic surface, PH2O = 500 MPa, An0–14, WINKLER, 1975). II. The same system after CLARKE, 1992. B – Possible P/T conditions of crystallization of peraluminous granitoids of the Battony Unit. Experimental phase equilibrium diagram of watersaturated peraluminous granite solidus (I). (JOHANNES & HOLTZ, 1996) and stoichiometric muscovite breakdown curve (II.), andalusite = sillimanite reaction (R69, RICHARDSON, et al. 1969). The possible isobaric cooling path of Battonya peraluminous granitoids is shown between the two arrows, (after CLARKE, et al.,2005). The increasing ƒH2O and high aKAlSi3O8 increases the sta- bility of muscovite (CLEMENS et al., 1988). Muscovite is stable if the An content of coexisting plagioclase is low (al- bite-oligoclase). At higher An content, the solidus tempera- ture of the granitoid melt is higher, and primary muscovite cannot crystallize as in the case of quartzmonzodiorite. The bulk composition of the two mica and muscovite granitoid and the presence of primary muscovite indicates a low temperature water-saturated “minimum” peraluminous granite melt (Fig. 7/A, B). The pressure of crystallization of magmatic muscovite without magmatic andalusite could be 490–600 MPa according to CLARKE et al. (2005), because below this pressure, magmatic cordierite or andalusite can crystallize instead of or in addition to the muscovite. The P/T conditions correspond to a minimum 15 km depth of crys- tallization of the intrusion not far from source rocks. In Bat- tonya, the temperature of melts were probably higher be- cause of the presence of metaluminous amphibole-biotite quartzmonzodiorite, but the majority of the rock such as the Buda et al.: Mafi c enclaves in peraluminous Variscan granitoid in the Battonya Unit from Southeast Hungary Geologia Croatica 251 Ta bl e III : R ep re se nt at iv e co m po si tio ns o f p rim ar y (m ag m at ic ) a nd se co nd ar y (h yd ro th er m al ) m us co vi te s f ro m th e Ba tt on ya U ni t d et er m in ed b y el ec tr on m ic ro pr ob e.   pr im ar y m us co vi te se co nd ar y m us co vi te Ba tt .-3 7 M h. -5 Ba tt .-6 3   Ba tt .-1 2 av er - ag e Ba tt .-6 3 Ba tt .-1 2 M h- 8 av er - ag e Si O 2 45 .4 0 45 .3 0 45 .2 2 45 .4 0 45 .1 7 45 .0 2 44 .9 4 45 .1 5 45 .4 8 45 .0 0 45 .1 6 46 .0 1 45 .2 5 45 .1 6 45 .1 6 45 .2 5 45 .9 9 46 .1 1 45 .7 0 46 .6 2 45 .5 9 46 ,1 9 46 .0 3 Ti O 2 0, 79 0. 90 1. 11 1. 79 1. 75 1. 77 1. 03 1. 08 0. 88 1. 09 1, 03 1. 16 1. 01 1. 23 1, 15 1. 18 0. 64 0. 65 0. 71 0. 04 0. 80 0. 29 0. 52 Al 2O 3 35 .9 3 36 .0 3 31 .9 5 31 .8 0 31 .3 9 31 .5 7 32 .7 4 32 .7 3 31 .3 6 32 .0 3 32 .3 9 29 .6 9 32 .8 4 32 .6 0 32 .2 7 32 .4 9 31 .7 1 32 .4 6 31 .2 7 31 .7 8 31 .2 4 30 .4 7 31 .4 9 Cr 2O 3 0. 01 0. 00 0. 01 0. 01 0. 02 0. 02 0. 02 0. 02 0. 01 0. 03 0. 01 0. 03 0. 00 0. 02 0. 00 0. 01 0. 00 0. 01 0. 00 0. 01 0. 01 0. 00 0. 00 Fe O 1. 29 1. 12 4. 18 4. 24 4. 16 3. 99 4. 14 3. 95 4. 41 4. 24 4. 06 4. 58 3. 95 4. 06 4. 04 3. 76 3. 62 3. 37 4. 37 3. 31 4. 72 4. 69 4. 01 M nO 0. 02 0. 01 0. 01 0. 03 0. 01 0. 01 0. 05 0, 04 0. 06 0. 04 0. 06 0, 10 0. 06 0. 05 0. 05 0. 04 0. 06 0. 05 0. 11 0. 07 0. 02 0. 03 0. 06 M gO 0. 53 0. 54 1. 02 1. 03 1. 04 0. 97 0. 95 0. 92 1. 25 1. 00 1. 01 1. 77 0. 97 1. 02 1. 07 1. 01 1. 38 1. 24 1. 41 1. 35 1. 26 1. 49 1. 35 Ca O 0. 01 0. 00 0. 00 0. 00 0. 00 0. 01 0. 00 0. 01 0. 01 0. 01 0. 00 0. 01 0. 00 0. 00 0. 01 0. 00 0. 00 0. 01 0. 01 0. 02 0. 02 0. 00 0. 01 N a 2 O 1. 21 1. 18 0. 39 0. 38 0. 38 0. 36 0. 49 0. 52 0. 39 0. 38 0. 50 0. 24 0. 47 0. 42 0. 55 0. 52 0. 25 0. 31 0. 29 0. 17 0. 37 0. 24 0. 27 K 2 O 9. 49 9. 54 10 .8 5 10 .6 2 10 .7 4 10 .8 0 10 .4 1 10 .5 9 10 ,8 5 10 .9 9 10 .5 9 10 .8 0 10 .7 2 10 .8 3 10 .4 1 10 .5 5 11 .1 7 11 .0 2 10 .8 0 10 .5 6 10 .8 0 11 .2 5 10 .9 3 To ta l 94 .6 7 94 .6 3 94 .7 4 95 .2 9 94 .6 7 94 .5 2 94 .7 6 95 .0 0 94 .6 9 94 .8 2 94 .8 2 94 .3 9 95 .2 8 95 .3 9 94 .7 0 94 .8 2 94 .8 1 95 .2 3 94 .6 8 93 .9 3 94 .8 1 94 .6 5 94 .6 8   St ru ct ur al fo rm ul ae c al cu la te d on a n an hy dr ou s b as is o f 2 2 (O ) Si 6. 06 6 6. 05 3 6. 18 1 6. 16 6 6. 18 2 6, 16 7 6. 12 6 6. 13 9 6. 22 8 6. 15 8 6. 15 8 6. 32 7 6. 13 8 6. 12 9 6. 15 9 6. 15 8 6. 26 5 6. 23 7 6. 25 3 6. 36 0 6. 24 0 6. 34 0 6. 28 3 Al IV 1. 93 4 1. 94 7 1. 81 9 1. 83 4 1. 81 8 1. 83 3 1. 87 4 1. 86 1 1. 77 2 1. 84 2 1. 84 2 1. 67 3 1. 86 2 1. 87 1 1. 84 1 1. 84 2 1. 73 5 1. 76 3 1. 74 7 1. 64 0 1. 76 0 1. 66 0 1. 71 8 Su m _T   Al VI 3. 72 0 3. 72 3 3. 32 4 3. 25 2 3. 24 1 3. 26 0 3. 38 2 3. 38 0 3. 28 5 3. 32 0 3. 35 9 3. 13 5 3. 38 4 3. 33 9 3. 34 2 3. 36 3 3. 35 2 3. 40 7 3. 29 2 3. 46 5 3. 27 5 3. 26 6 3. 34 3 Ti 0. 07 9 0. 09 0 0. 11 4 0. 18 3 0. 18 0 0. 18 2 0. 10 6 0. 11 0 0. 09 1 0. 11 2 0. 10 6 0. 12 0 0. 10 3 0. 12 6 0. 11 8 0. 12 1 0. 06 6 0. 06 6 0. 07 3 0. 00 4 0. 08 2 0. 03 0 0. 05 4 Fe 2 0. 14 4 0. 12 5 0. 47 8 0. 48 2 0, 47 6 0. 45 7 0, 47 2 0. 44 9 0. 50 5 0. 48 5 0. 46 3 0. 52 7 0. 44 8 0. 46 1 0. 46 1 0. 42 9 0. 41 2 0. 38 1 0. 50 0 0. 37 8 0. 54 0 0. 53 8 0. 45 8 Cr 0, 00 1 0. 00 0 0. 00 1 0. 00 1 0. 00 2 0. 00 2 0. 00 2 0. 00 2 0. 00 1 0. 00 3 0. 00 1 0. 00 3 0. 00 0 0. 00 2 0. 00 0 0. 00 1 0. 00 0 0. 00 1 0. 00 0 0. 00 1 0. 00 1 0. 00 0 0. 00 1 M n 0. 00 2 0. 00 1 0. 00 1 0. 00 3 0. 00 1 0. 00 1 0. 00 6 0. 00 5 0. 00 7 0. 00 5 0. 00 7 0. 01 2 0. 00 7 0. 00 6 0. 00 6 0. 00 5 0. 00 7 0. 00 5 0. 01 3 0. 00 9 0. 00 2 0. 00 4 0. 00 7 M g 0. 10 6 0. 10 8 0. 20 8 0. 20 9 0. 21 2 0. 19 8 0. 19 3 0. 18 6 0. 25 5 0. 20 4 0. 20 5 0. 36 3 0. 19 6 0. 20 6 0. 21 8 0. 20 4 0. 27 9 0. 25 0 0. 28 7 0. 27 5 0. 25 7 0. 30 4 0. 27 5 Ca 0. 00 1 0. 00 0 0. 00 0 0. 00 0 0. 00 0 0. 00 1 0. 00 0 0. 00 1 0. 00 1 0. 00 1 0. 00 0 0. 00 1 0. 00 0 0. 00 0 0. 00 1 0. 00 0 0. 00 0 0. 00 1 0. 00 2 0. 00 2 0. 00 2 0. 00 0 0. 00 1 N a 0. 31 3 0. 30 6 0. 10 3 0. 10 0 0. 10 1 0. 09 6 0. 13 0 0. 13 7 0. 10 4 0. 10 1 0. 13 2 0. 06 4 0. 12 4 0. 11 1 0. 14 5 0. 13 8 0. 06 5 0. 08 1 0. 07 6 0. 04 4 0. 09 7 0. 06 5 0. 07 1 K 1. 61 8 1. 62 6 1. 89 2 1. 84 0 1. 87 5 1. 88 8 1. 81 0 1. 83 7 1. 89 5 1. 91 9 1. 84 2 1. 89 5 1. 85 5 1. 87 5 1. 81 1 1. 83 2 1. 94 0 1. 90 1 1. 88 5 1. 83 7 1. 88 6 1. 96 9 1. 90 3 Ca tio ns 13 .9 84 13 .9 79 14 .1 21 14 .0 70 14 .0 88 14 .0 85 14 .1 01 14 .1 07 14 .1 44 14 .1 50 14 .1 15 14 .1 20 14 .1 17 14 .1 26 14 .1 02 14 .0 94 14 .1 21 14 .0 93 14 .1 28 14 .0 15 14 .1 42 14 .1 76 14 .1 13 N a/ N a+ K 0. 16 2 0. 15 8 0. 05 2 0. 05 2 0. 05 1 0. 04 8 0. 06 7 0. 06 9 0. 05 2 0. 05 0 0. 06 7 0. 03 3 0. 06 3 0. 05 6 0. 07 4 0. 07 0 0. 03 2 0. 04 1 0. 03 9 0. 02 3 0. 04 9 0. 03 2 0. 03 6 M g/ Fe M g 0. 42 0 0. 46 0 0. 30 0 0. 30 0 0. 31 0 0. 30 0 0. 29 0 0. 29 0 0. 34 0 0. 30 0 0. 31 0 0. 41 0 0. 30 0 0. 31 0 0. 32 0 0. 33 1 0. 40 0 0. 40 0 0. 36 0 0. 42 0 0. 32 0 0. 36 0 0. 37 7 * Ba tt = B at to ny a co re sa m pl es ; M h = M ez őh eg ye s c or e sa m pl e Re m ar ks : T w o m ic a gr an ito id s. Ba tt -3 7, M h- 5. M us co vi te g ra ni to id s. Ba t- 63 , B at t- 12 , M h- 8. Geologia Croatica 65/2Geologia Croatica 252 Figure 8: A, B, C – Plot of muscovite compositions in the Battonya granitoids (arrows show the changing of composition from primary to secondary mus- covites). two-mica and muscovite granitoids, crystallized at about 650–6850C and above 490 MPa pressure. Afterwards, the granitoids were affected by alkali metasomatism, indicated by the replacement of microcline and albite, and by hydro- thermal alteration evidenced by widespread secondary mica and chloritization of biotite. Magmatic crystallization, meta- somatism, and hydrothermal processes were continuous events in the plutonic rocks as suggested by the continual decrease in Ti and Na, and the increase in Si and Mg con- tents of white micas (Fig. 8/A, B, C). The hydrothermal ac- tivity increased the A/CNK indices of the granitoids in some parts of the intrusion due to the leaching of alkalis. 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Rev. Earth Planet. Sci., 16, 21–51. Manuscript received January 23, 2012 Revised manuscript accepted May 25, 2012 Available online June 29, 2012