Garnet peridotites from Pohorje: Petrography, geothermobarometry and metamorphic evolution
Petrografija, geotermobarometrija in metamorfni razvoj granatovega peridotita
na Pohorju
Mirijam VRABEC
University of Ljubljana, Faculty of Natural Sciences and Engineering, Department of Geology, Aškerčeva 12, SI-1000 Ljubljana, Slovenia; e-mail: mirijam.vrabec@ntf.uni-lj.si
Prejeto / Received 15. 3. 2010; Sprejeto / Accepted 20. 5. 2010
Key words: ultrahigh-pressure metamorphism, garnet peridotite, geothermobarometry, collisional orogen, Pohorje, Eastern Alps, Slovenia
Ključne besede: ultravisokotlačna metamorfoza, granatov peridotit, geotermobarometrija, kolizijski orogeni, Pohorje, Vzhodne Alpe, Slovenija
Abstract
Ultrahigh-pressure (UHP) metamorphism has been recorded in Eo-Alpine garnet peridotites from the Pohorje Mts., Slovenia, belonging to the Eastern Alps. The garnet peridotite bodies are found within serpentinized meta-ultrabasites in the SE edge of Pohorje and are closely associated with UHP kyanite eclogites. These rocks belong to the Lower Central Austroalpine basement unit of the Eastern Alps, exposed in the proximity of the Periadriatic fault system.
Garnet peridotites show signs of a complex four-stage metamorphic history. The protolith stage is represented by a low-P high-T assemblage of olivine + Al-rich orthopyroxene + Al-rich clinopyroxene + Cr-spinel. Due to metamorphism, primary clinopyroxene shows exsolutions of garnet, orthopyroxene, amphibole, Cr-spinel and ilmenite. The UHP metamorphic stage is defined by the assemblage garnet + olivine + Al-poor orthopyroxene + clinopyroxene + Cr-spinel. Subsequent decompression and final retrogression stage resulted in formation of kelyphitic rims around garnet and crystallization of tremolite, chlorite, serpentine and talc.
Pressure and temperature estimates indicate that garnet peridotites reached the peak of metamorphism at 4 GPa and 900 °C, that is well within the UHP stability field. Garnet peridotites in the Pohorje Mountains experienced UHP metamorphism during the Cretaceous orogeny and thus record the highest-pressure conditions of all Eo-Al-pine metamorphism in the Alps.
Izvleček
Granatovi peridotiti na JV robu Pohorja kažejo znake metamorfoze pri ultravisokotlačnih pogojih. Nastopajo v obliki majhnih teles znotraj serpentiniziranih metaultrabazičnih kamnin in so v tesni povezavi z ultravisokotlačnimi kianitovimi eklogiti. Tako peridotiti kot eklogiti pripadajo kamninam Spodnjega srednjega avstroalpina Vzhodnih Alp.
Metamorfni razvoj granatovih peridotitov je potekal v štirih fazah. Protolitna faza obsega nizkotlačno in vi-sokotemperaturno mineralno združbo olivin + visoko-Al ortopiroksen + visoko-Al klinopiroksen + Cr-spinel. Med metamorfozo so se v primarnih klinopiroksenih formirale eksolucijske lamele granata, ortopiroksena, amfibola, Cr-spinela in ilmenita. Fazo ultravisokotlačne metamorfoze označujejo minerali granat + olivin + nizko-Al or-topiroksen + klinopiroksen + Cr-spinel. Sledili sta dekompresijska in kot zadnja retrogradna faza, ki je nastopila pri najnižjih P-T pogojih. To zaznamujejo nizkotemperaturni minerali, kot so tremolit, klorit, serpentin in lojevec.
Geotermobarometrični izračuni kažejo, da so bili granatovi peridotiti na Pohorju med viškom metamorfoze v času kredne orogeneze izpostavljeni tlaku 4 GPa in temperaturi preko 900 °C, kar ustreza polju ultravisokotlačne metamorfoze. Tako predstavljajo najvišje tlačne pogoje, dosežene med eo-alpinsko orogenezo na območju celotnega Alpskega orogen.
Introduction
Garnet peridotites are commonly associated with eclogites in UHP metamorphic terranes (Liou et al., 1998; Carswell & Compagnoni, 2003; Chopin, 2003). Peridotite massifs are important features of orogenic belts worldwide. Spinel peridotite is pre-
dominant in such bodies, but garnet peridotite is common in continental collision belts, particularly in Eurasian UHP metamorphic terranes (garnet peridotites and pyroxenites have been reported from 11 of the 15 or so HP/UHP terranes). These so-called 'orogenic' or 'Alpine-type' peridotites include several garnet-bearing rock types, such as
lherzolites, harzburgites, wehrlites, dunites and pyroxenites, generally referred to as garnet peri-dotites. These rocks mostly occur not only within metamorphosed continental crust, but also within units of oceanic affinity (e.g. Brueckner & Meda-ris, 2000 and references therein). Although volu-metrically minor, these UHP metamorphic rocks provide an opportunity to evaluate the tectono-thermal conditions related to the interaction of mantle and crust during UHP metamorphism as well as important information on orogenic processes in deep orogenic root zones and the upper mantle (e.g. Zhang et al., 1994; Dobrzhinetskaya et al., 1996; van Roermund & Drury, 1998).
Most garnet peridotites are depleted upper mantle material, variously modified by metasomatism, but some originated by low-pressure crystallization from ultramafic-mafic igneous complexes. All presently known garnet peridoti-tes in Eurasian HP/UHP terranes can be divided into two groups, one having a high P/T ratio and the other a low P/T ratio (Medaris, 2000; Figure 1). Nearly all of the peridotite occurences in the high P/T group can be related to subduction processes and are isofacial and approximately contemporaneous with associated UHP crus-tal rocks that contain coesite and diamond. The single exception is the Western Gneiss Region, Norway, where the garnet peridotites are relicts of old, cold lithosphere that formed earlier and
under different conditions than those prevailing during the overprinting Caledonian metamor-phism. Peridotites in the low P/T group are associated with HP crustal rocks that are characterized by HP granulites and strongly retrogressed eclogites, in which little evidence for the presence of coesite or diamond was found so far. The extremely high temperatures of the low P/T group would seem to require the influence of upwelling asthenosphere.
Garnet peridotites are thought to have evolved in at least four different tectonothermal settings (Medaris, 2000): (1) emplacement of peridotites (serpentinites or igneous complexes, e.g. ophiolite components or ultramafic differentiates of mafic intrusions) into the oceanic or continental crust prior to UHP metamorphism, followed by transport of peridotites and associated crust to UHP conditions (high P/T) by a subducting plate; (2) transfer of peridotites from a mantle wedge to the crust of an underlying, subducting plate (high P/T); such peridotites are initially either spinel- or garnet-bearing, depending on the depth of derivation; (3) originating from upwelling asthenosphere that passed through a high-temperature spinel peridotite stage, followed by cooling into the garnet peridotite field (low P/T); and (4) extraction of garnet peridotites from ancient subcontinental lithosphere, perhaps by deep-seated faulting within a continental plate (high P/T).
Figure 1. P-T estimates for Pohorje garnet peridotites in comparison with well established UHP terranes:
(1)	Asian UHP terranes (dark grey color);
(2)	Scandinavian Caledonides (black color);
(3)	European Variscan terranes (white color); and
(4)	Alpine terranes (pale grey color; after Medaris, 2000).
Shown for reference are equilibria for diamond-graphite (Bundy, 1980), coesite-quartz (Bohlen & Boettcher, 1982), and spinel-garnet peridotite (O'Hara et al., 1971). Also shown are steady-state conductive geotherms for 200 km and 100 km thick lithosphere, a dry lherzolite solidus (Takahashi, 1986), and a stability field for majoritic garnet containing 3 to 5 vol% pyroxene.
Garnet peridotite bodies in the Alps are known from two main regions. Alpe Arami, Monte Duria and Cima di Gagnone garnet peridotites belong to the Adula-Cima Lunga unit (Ernst, 1978; Nimis & Trommsdorff, 2001; Paquin & Altherr, 2001), and are of Tertiary age (Becker, 1993; Gebauer, 1996), whereas garnet peridotites from Nonsberg area in the Ulten zone (Obata & Morten, 1987; Nimis & Morten, 2000) are of Variscan age (Tumiati et al., 2003). Metamorphic processes related to the Cretaceous (so-called Eo-Alpine) events in the Alps have been recognized mainly in the Austroalpine units (e.g. Thoni & Jagoutz, 1992; Hoinkes et al., 1999; Schmid et al., 2004; Schuster et al., 2004). In the Eastern Alps, the metamorphic grade of Cretaceous metamorphism reached UHP facies in the south-easternmost parts, in the Pohorje Mountains of Slovenia, belonging to the Lower Central Au-stroalpine unit (Janak et al., 2004; Vrabec, 2010).
In kyanite eclogites from Pohorje Mountains UHP metamorphism have been recently documented (Janak et al., 2004; Vrabec, 2010). The eclogites are closely associated with serpentinized metaultrabasites in which investigated garnet peridotite remnants are preserved (Janak et al., 2006). Early estimates of the P-T conditions experienced by the Pohorje garnet peridotites were in the range of 750-1050 °C and 2.4-3.6 GPa (Hinter-lechner-Ravnik et al., 1991; Visona et al., 1991).
This paper presents the evidence for UHP meta-morphism of garnet-bearing ultramafic rocks in the Austroalpine units of the Eastern Alps, exposed in the Pohorje Mountains of Slovenia. Described here are the mineralogical, petrological and geothermobarometrical features of garnet peridotites constraining their multi-stage meta-morphic evolution. The obtained results offer additional evidence for UHP metamorphism in the Eastern Alps.
Geological Background
The Pohorje massif is built up of three Eo-Alpine Cretaceous nappes (Mioc & Znidarcic, 1977; Fodor et al., 2003) that belong to pre-Neogene metamorphic sequences of the Austroalpine units of the Eastern Alps (Figure 2). The lowest nappe that is termed the Pohorje nappe (Janâk et al., 2006) represents the Lower Central Austroalpine (Janâk et al., 2004) and consists of medium- to high-grade metamorphic rocks, predominantly micaschists, gneisses and amphibolites with marble and quarzite lenses. It also contains several ec-logite lenses and a body of metaultrabasic rocks. The Pohorje nappe is overlain by a nappe composed of weakly metamorphosed Paleozoic rocks, mainly low-grade metamorphic slates and phyl-lites. The uppermost nappe is built up of Permo-Triasic clastic sedimentary rocks, mainly sandstones and conglomerates. The two latter nappes represent the Upper Central Austroalpine. The entire nappe stack is overlain by Early Miocene sediments which belong to the syn-rift basin fill of the Pannonian Basin (Fodor et al., 2003).
The magmatic intrusion in the central part of Pohorje is of Miocene age (18-19 Ma; Trajanova et al., 2008; Fodor et al., 2007). It is of granodioritic to tonalitic composition (Zupancic, 1994), with a very small gabbroic enclave in its SE part. The main intrusion was followed by the formation of aplite and pegmatite veins, and lamprophyric dykes. In the western part of Pohorje, shallow dacite bodies and dykes intrude both the granodiorite body and the country rocks, suggesting that the dacite intrusion is somewhat younger than the grano-diorite one. The Pohorje nappe is folded into an ESE-WNW-striking antiform, the core of which is occupied by the intrusion. Therefore, neither the original basal contact of the Pohorje nappe nor
48°-
47°-
46°
-48°
-47° N
J Hallstatt nappes i | i | Upper Central Austroalpine cover and Tirollc nappes ^ Upper Central Austroalpine basement
Figure 3
i | i | Lower Central Austroalpine cover and Bajuvaric nappes [ ^ J Lower Central Austroalpine basement ]] Lower Austroalpine (basement & cover)
Penninic and Helvetic nappes
Figure 2. Tectonic map of the Eastern Alps. B-Bajuvaric, GN-Gurktal nappe, GP-Graz Paleozoic, K-Koralpe, NGZ-Northern Grauwacke zone, Ö-Southern Ötztal nappe, P-Pohorje, S-Saualpe, T-Tirolic. Modified after Neubauer & Höck (2000) and Schmid et al. (2004).
any deeper tectonic units are exposed in the Pohorje area.
North and south of the granodiorite intrusion, eclogite bodies, lenses and bands of different sizes are found within country rocks. Numerous lenses, boudins and bands of eclogites also occur within the metaultrabasite body, located in the south-easternmost part of Pohorje Mountains near Slovenska Bistrica. Metaultrabasites form a body of ca. 5 x 1 km size, which is termed the Slovenska Bistrica ultramafic complex (SBUC; Janak et al., 2006; Figure 3). Some outcrops of garnet peridoti-tes also occur away from this body, further to the west. The main protoliths of the Slovenska Bistrica ultramafic complex are harzburgites and dunites (cf. Hinterlechner-Ravnik, 1987; Hinterlechner-Ravnik et al., 1991). Because of extensive serpen-tinization, only a few less-altered bodies of garnet peridotites, garnet pyroxenites and coronitic me-tatroctolites are preserved (Hinterlechner-Ravnik, 1987; Hinterlechner-Ravnik et al., 1991). The country rocks of the eclogites and the Slovenska Bistrica ultramafic complexareamphibolites,orthogneis-ses, paragneisses and micaschists. These rocks form a strongly foliated matrix around elongated lenses and boudins of eclogites and ultrabasites, including the Slovenska Bistrica ultramafic complex.
The timing of HP/UHP metamorphism in the Pohorje nappe is Cretaceous, as documented by dating of eclogites with garnet Sm-Nd and zircon U-Pb ages of 91 Ma (Miller et al., 2005). Almost identical ages have been obtained from dating of garnet (93-87 Ma; Thoni, 2002) and zircon (92 Ma; Janak et al., 2009) of gneisses and micaschists. This age is similar to that of Koralpe and Saualpe eclogite facies metamorphism (Thoni & Jagoutz, 1992; Thoni & Miller, 1996; Miller & Thoni, 1997; Thoni, 2002). Tertiary K-Ar mica ages (19-13 Ma)
as well as apatite and zircon fission track ages (19-10 Ma) were obtained from the country rocks of eclogites and metaultrabasites in the Pohorje nappe (Fodor et al., 2002). This suggests that the peak of metamorphism was attained during the Cretaceous, and final cooling occurred in the Early to Midd Miocene. Upper Cretaceous (7570 Ma) cooling ages were determined in the Koralpe area, the north-westward extension of the Pohorje nappe (Schuster et al., 2004), indicating that the Koralpe rocks were exhumed during the Upper Cretaceous. Also the major exhumation of the Pohorje nappe, from UHP depth to crus-tal depth, most probably occurred already during the Upper Cretaceous. The final stage of exhumation to the surface was achieved in the Miocene by east- to north-east-directed low-angle exten-sional shearing, associated with the main opening phase of the Pannonian basin and leading to the core complex structure of the Pohorje Mountains (Fodor et al., 2003). The Miocene shearing event reactivated and overprinted the nappe boundaries in the Pohorje area (Janak et al., 2006). Therefore, direct structural evidence for the kinematics of Cretaceous exhumation has not yet been found.
Methods
Electron Probe Micro-Analysis
Microchemical analyses of the main constituent minerals were determined by Electron Probe Micro-Analysis (EPMA) technique using a CAME-CA SX-100 electron microprobe at Dionyz Stur Institute of Geology in Bratislava. Bombarding of micro-volumes of sample with a focused electron beam (5-30 keV) induced emission of X-ray photons. The wavelengths of collected X-rays
Figure 3. Simplified geological map of Pohorje and adjacent areas (modified from Mioc & Znidarcic, 1977) showing locations of the investigated garnet peridotites. Locality VI01/04 is outcroping within the SBUC near Visole while the other one, locality 119, is exposed farther west, near Prihovca.
were identified by recording their WDS spectra (Wavelength Dispersive Spectroscopy). Analytical conditions were 15 keV accelerating voltage and 20 nA beam current, with a peak counting time of
20 s and a beam diameter of 2-10 |im. Raw counts were corrected using a PAP routine.
Representative analyses of mineral phases are given in Table 1.
Table 1. Representative microprobe analyses of mineral compositions. I -III - decompression stage, IV - retrogression stage.
protolith stage, II - metamorphic stage,
Sample	119	119	119	119	119	119	119	119	119	119	119
Mineral	Ol II	Grt II	Grt IIexs	Cpx I, II	Opx IIexs	Opx II	Opx III	Spl I, II	Spl III	Amp III	Amp IV
SiO2	40.70	41.40	41.95	54.02	58.26	57.73	56.50	0.01	0.04	45.23	56.16
TiO2	0.00	0.01	0.04	0.03	0.01	0.05	0.01	0.14	0.00	0.35	0.11
Al2O3	0.03	23.20	22.70	0.93	0.85	0.74	1.97	27.78	69.64	12.49	2.26
&2O3	0.01	0.12	1.05	0.16	0.17	0.11	0.03	35.43	0.00	0.77	0.30
FeO	10.69	10.02	12.13	1.78	6.93	6.55	6.32	25.50	7.79	5.18	3.73
MnO	0.10	0.24	0.46	0.02	0.10	0.10	0.08	0.29	0.00	0.02	0.08
MgO	49.90	18.80	16.56	17.52	34.81	35.64	34.70	10.30	23.20	18.41	21.89
CaO	0.02	5.46	5.81	24.90	0.56	0.20	0.21	0.00	0.06	12.14	12.93
Na2O	0.00	0.00	0.00	0.42	0.00	0.00	0.01	0.00	0.00	2.70	0.30
K2O	0.00	0.00	0.00	0.02	0.00	0.00	0.01	0.00	0.00	0.07	0.02
Total	101.44	99.25	100.70	99.80	101.69	101.12	99.84	99.45	100.73	97.36	97.79
Si	0.986	2.983	3.018	1.968	1.979	1.963	1.950	0.000	0.001	6.390	7.743
Ti	0.000	0.001	0.002	0.001	0.000	0.001	0.000	0.003	0.000	0.037	0.012
Al	0.001	1.971	1.925	0.040	0.034	0.030	0.080	1.004	1.994	2.080	0.367
Cr	0.000	0.007	0.060	0.005	0.005	0.003	0.001	0.858	0.000	0.086	0.032
Fe2+	0.217	0.602	0.730	0.054	0.197	0.186	0.183	0.640	0.157	0.574	0.430
Mn	0.002	0.015	0.028	0.001	0.003	0.003	0.002	0.008	0.000	0.002	0.010
Mg	1.802	2.019	1.776	0.951	1.762	1.806	1.785	0.471	0.840	3.876	4.499
Ca	0.000	0.422	0.448	0.972	0.020	0.007	0.008	0.000	0.002	1.838	1.910
Na	0.000	0.000	0.000	0.030	0.000	0.000	0.000	0.000	0.000	0.740	0.082
K	0.000	0.000	0.000	0.001	0.000	0.000	0.000	0.000	0.000	0.013	0.004
Total	3.008	8.020	7.987	4.022	4.000	3.999	4.009	2.984	2.994	15.636	15.088
XMg	0.89	0.78	0.71	0.95	0.90	0.92	0.91	0.42	0.84	0.94	0.91
Cr*								0.46	0.00		
Sample	VI01/04	VI01/04	VI01/04	VI01/04	VI01/04	VI01/04	VI01/04	VI01/04	VI01/04	VI01/04	VI01/04
Mineral	Ol II	Grt II	Cpx I	Cpx II, III	Opx I	Opx II	Opx III	Spl I, II	Spl III	Amp III	Amp IV
SiO2	40.62	41.73	52.95	55.28	56.73	57.33	55.65	0.04	0.09	44.70	56.89
TiO2	0.00	0.00	0.00	0.00	0.00	0.00	0.00	0.10	0.00	0.13	0.03
Al2O3	0.00	22.99	4.87	1.05	2.19	0.81	1.82	26.68	65.96	13.85	1.20
Cr2O3	0.000	0.48	0.16	0.21	0.00	0.00	0.03	37.29	0.85	1.23	0.21
FeO	12.239	10.94	3.36	1.66	8.05	7.55	9.71	22.97	11.71	3.77	2.25
MnO	0.210	0.45	0.09	0.02	0.08	0.18	0.14	0.34	0.15	0.04	0.05
MgO	47.510	17.64	17.65	17.42	33.69	34.13	32.80	10.28	20.73	18.58	23.33
CaO	0.029	6.16	21.320	24.680	0.130	0.110	0.189	0.00	0.04	12.57	13.27
Na2O	0.000	0.00	0.290	0.500	0.000	0.000	0.093	0.00	0.00	2.36	0.13
K2O	0.000	0.00	0.010	0.010	0.000	0.000	0.027	0.00	0.00	0.07	0.02
Total	100.61	100.39	100.699	100.834	100.865	100.105	100.468	97.70	99.53	97.30	97.38
Si	1.000	2.993	1.901	1.984	1.949	1.982	1.941	0.001	0.002	6.287	7.823
Ti	0.000	0.000	0.000	0.000	0.000	0.000	0.000	0.002	0.000	0.014	0.003
Al	0.000	1.943	0.206	0.044	0.089	0.033	0.075	0.983	1.952	2.296	0.195
Cr	0.000	0.027	0.005	0.006	0.000	0.000	0.001	0.921	0.017	0.137	0.023
Fe2+	0.252	0.653	0.099	0.048	0.231	0.218	0.283	0.591	0.243	0.406	0.258
Mn	0.004	0.027	0.003	0.001	0.002	0.005	0.004	0.009	0.003	0.005	0.005
Mg	1.74	1.886	0.944	0.932	1.725	1.758	1.706	0.479	0.775	3.894	4.783
Ca	0.00	0.474	0.820	0.949	0.005	0.004	0.007	0.000	0.001	1.894	1.956
Na	0.00	0.000	0.020	0.035	0.000	0.000	0.006	0.000	0.000	0.644	0.036
K	0.00	0.000	0.000	0.000	0.000	0.000	0.001	0.000	0.000	0.013	0.004
Total	3.000	8.003	3.998	3.999	4.001	4.000	4.025	2.986	2.993	15.590	15.085
XMg	0.87	0.75	0.90	0.95	0.89	0.89	0.86	0.45	0.76	0.98	0.95
Cr*								0.48	0.86		
Analyses (in wt%) of olivine (Ol), garnet (Grt), clinopyroxene (Cpx), orthopyroxene (Opx), spinel (Spl) and amphibole (Amp). Olivine is normalized to 4, garnet to 12, clinopyroxene to 6, orthopyroxene to 6, spinel to 4 and amphibole to 23 oxygens. Exs - exsolution in clinopyroxene.
Garnet-olivine Fe2+-Mg exchange geothermometery
Garnet-olivine Fe2+-Mg exchange thermometer is based on the partitioning of iron and magnesium between the coexisting garnet and olivine and may be represented by the exchange reaction:
2 pyrope + 3 fayalite —» 2 almandine + 3 forsterite
The distribution coefficient KD is defined as:
yol ygrt „ Mg' Fe D ~-
yol ygrt ^ Fe ' Mg
where XJ&g is the mole fraction of Mg in olivine, Xf£ is the mole fraction of Fe2+ in the garnet, etc.
Garnet-olivine Fe2+-Mg exchange thermometer has been successfully calibrated by O'Neill & Wood (1979) and later corrected by O'Neill (1980) yielding the following equation:
Tow-80 ( O =
_ 902 + DV + (X\^ - X°Je) ■ (498 + 1.51(P - 30))
In Kd +0.357
| -98-(*g-*g) + 1347-*g 2?3
\nKD +0.357
DV term is incorporating thermal expansion and compressibilities for all four phases and is given by:
DV = 462.5 ■ (1.0191+(T-1073)) • (2.87 • 10"5) • (P- 2.63■ 10"1 • P2 - 29.76) +
+ 262.4 • (1.0292+(T -1073)) • (4.5 • 10"5) • (P - 3.9 • 10"4 • ?2 - 29.65) -
-	454 ■ (1.020+(T-1073)) ■ (2.84 • 10"5) • (? - 2.36 ■ 10"4 ■ P2 - 29.79) -
-	278.3 • (1.0234+(T-1073)) • (2.3 • 10~5 HP - 4.5 • 10"4 • P2 - 29.6)
where P is in kbars. The four parts of the DV term are volume expressions for almandine, forsterite, pyrope and fayalite, respectively. Since the DV term involves temperature, upper equation for Tow-80 is best solved iteratively by estimating initial value of T (°C) at pressure P (kbar). Since the DV term is small, this method converges rapidly. At P equal to the experimental pressure of 30 kbar, the DV term is zero.
This geothermometer is most sensitive in the temperature and composition regions where KD is substantially greater than 1. It serves as a reliable geothermometer for magnesium-rich garnet-oli-vine assemblages equilibrated close to, or within, the temperature range 900-1400 °C and pressures up to about 60 kbar. For a fixed KD, the influence of pressure is to increase the calculated temperature by between 3 and 6 °C per kbar (O'Neill & Wood, 1979).
In garnet-olivine mineral combination only the garnet is a problematic member because it can incorporate significant amounts of Fe3+ in its structure. The presence of a Fe3+ component has a considerable influence on the calculated temperatures. The comparison of estimated temperatures for several garnet-olivine pairs with temperatures obtained from two-pyroxene thermometers has shown, that in the case of garnet-olivine thermo-
meter the Fe3+ content in garnets can be ignored and all Fe treated as Fe2+ (Canil & O'Neill, 1996).
Garnet-orthopyroxene Fe2+-Mg exchange geothermometery
The garnet-orthopyroxene Fe2+-Mg exchange thermometer is based on the distribution of Fe2+ and Mg between garnet and orthopyroxene according to the reaction:
2 pyrope + 3 ferrosilite ^ 2 almandine + 3 enstatite
One of the reliable calibrations of this geother-mometer which is applicable to garnet peridotites and granulites was made by Harley (1984):
T	3740 +140022.86-P ^
R- In ^+1.96
where P is pressure in kbars and R is the universal gas constant (8.3143 J/K mol). The distribution coefficient is given by:
X o ' y\	I H ' / /l/Trr
K,
_Xfe _(Fe2+/Mg)& X?: (Fe^/Mg)"
and
Ca
Xgrt =_
C° Ca + Mn + Fe2+ +Mg
The distribution of Fe2+ and Mg between garnet and orthopyroxene produces a good geothermo-meter with required high dP/dT slope and a range in Kd of 4 to 1.5 over geologically attainable P-T conditions. At low temperatures the precision of the geothermometer is limited by analytical uncertainties. An error in KD of only ±0.1 is equivalent to ±40-60 °C error in temperature estimation (Harley, 1984).
The effects of Fe3+ calculations are very important when using garnet-orthopyroxene Fe2+-Mg exchange thermometer. Normally, in natural assemblages Fe3+ preferentially enters garnet rather than orthopyroxene. KD values calculated by simply assuming Fetot = Fe2+ will therefore be greater than those calculated by estimating Fe3+ with some consistent charge- and mass-balance algorithm. Even a small decrease of KD, resulting from Fe3+ calculation, may raise estimated temperatures by 20-100 °C, which is a significant amount (Harley, 1984). In natural systems, TH-84 temperatures calculated with upper equation by ignoring Fe3+ should be regarded as minimum temperatures.
Al-in-orthopyroxene geobarometry
Reliable geobarometers suitable for HP/UHP rocks are mostly based on net-transfer reactions involving transfer of Al from tetrahedral to octahedral coordination sites. The Al-in-orthopyrox-ene barometer has been widely used. The content of Al3+ in octahedral sites in orthopyroxene coexisting with garnet is particularly pressure de-
pendent and hence serves as an adequate indicator of the pressure conditions at which the rock has been equilibrated. Several calibrations of this barometer have been performed, as summarized by Krogh Ravna & Paquin (2003). To date, the Brey & Köhler (1990) calibration seems to be the most reliable for pressure calculations over a wide pressure range. Pressure is calculated according to the equation:
Y&1 —
Cr
Cr
Al+Cr

P(kbctr) =-with
2 1000
2-C,
C1 =-ÄT-ln^:D-5510 + 88.91T-19T12 +
Like in the Fe2+-Mg geothermometry, the oxidation state of present iron has significant influence. Fe3+ is replacing Al3+ in octahedral places in orthopyroxene structure. Consequently, equal amounts of Al3+ in tetrahedral sites are required to retain charge balance. This results in a limited amount of Al3+ available for the substitution, therefore calculated activity of the MgAl2SiO6 component in orthopyroxene is considerably underestimated.
Results
+ 3 ■ (Xg)2 • 82458 + ■ XpJ • (80942-46.7 • T) - Petrography and mineral chemistry
-	3 • Xfl • Xg • 17793 - Xg • Xg • (1.164 • 106 -
-	420.4 • T)-Xfe ■ Xg ■ (-1.25 • 106 + 565 • T)
C2 = -832 - 8.78 • 10"5 • (T - 298) + 3 • (Xfa)2 • 3305 -
- Xg ■ Xg • 13.45 + Xg ■ Xg ■ 10.5 C3 =16.6-10"4
Kn =
R is the universal gas constant (8.3143 J/K mol) and the distribution coefficient is calculated as:
(1 -x%?-x%
D y Ml ( yM2)2 y Ml
-A-MF'^MF) 'aAI,TS
Site occupancies for pyroxenes are taken from Nickel & Green (1985) and Carswell & Gibb (1987) and are defined as:
y ML _
-X-Al —
\rjy A A
y ft A A
AI +Na —Cr -Fe -2-Ti
Al +Na-Cr -Fe —2-Ti
Al-Na +Cr +Fei+ +2-Ti
(forJd< 0)
{ for Jd >0)
%-Mg ~XMF 'Xmt (i -1,2)
yMl _ y Ml /■i _ y \
AFe ~AMF'\i AMF)
=(1 -Xf -Cr-Fe3+ -Ti)
=(1 -Ca-Na-Mn) _ Mg " Mg +Fe2+
Site occupancies for garnet are as follows:
Ca

Ca +Mg +Fe2+ +Mn
ygrt _
Fe
2 +
xri

Ca +Mg +Fez+ +Mn Mg
Ca +Mg +Fe2+ +Mn
Al Al+Cr
Several samples of relatively well-preserved garnet peridotites from two known localities were investigated: one locality is outcroping within the SBUC near Visole; the other one is exposed farther west, near Prihovca (Figure 3). In Visole the garnet-bearing peridotites occur as very small lenses within the extensively serpentinized ultra-basites while in Prihovca area garnet peridotite bodies of up to several metres in size are exposed within the rocks of continental crustal origin, mainly micaschists and gneisses. Garnet peridotites exhibit rather massive and relatively homogeneous textures without any distinct compositional layering visible in the outcrop, hand-specimen and thin-section scale. In well preserved garnet peridotites big pinkish-red colored garnet grains are surrounded by a black matrix whereas more serpentinized varieties contain completely white colored garnets.
Garnet peridotites consist of garnet, olivine, orthopyroxene, clinopyroxene and brown spinel, which are to a variable extent replaced by amphibole, green spinel, serpentine, talc and chlorite. They show higher modal amounts of garnet and clinopyroxene relative to olivine, therefore they are mainly classified as pyroxenites (garnet-oli-vine websterites), some of the samples even as garnet orthopyroxenites. However, because of intensive retrogression of these rocks, the abundance of primary minerals is largely obscured.
Garnet mostly forms big porphyroblastic grains with irregular boundaries (Figure 4a). Only rarely it is found in idiomorphic forms with well developed crystal faces. Garnet is also found as exsolution lamellas from clinopyroxene, in form of irregular, bleb-resembling inclusions in orthopyroxene and in coronas around Cr-spinel. All garnets are pyrope-rich, belonging to alman-dine-pyrope-grossular series. End member compositions are ranging from 53-68 mol% of pyrope, 18-33 mol% of almandine and spessartine, and 8-20 mol% of grossular and andradite. Garnets in samples from Prihovca contain slightly higher pyrope content (56-68 mol%) than garnets from Visole (54-66 mol%).
Figure 4. Garnets from garnet peridotites in photomicrographs - backscattered electron images (BSE).
(a)	Inhomogeneous garnet porphyroblasts are mainly found in shape of xenomorphic grains with irregular boundaries.
(b)	Patchy garnet grains surrounded by secondary symplectites of spinel, amphibole and orthopyroxene. Difference between high-Mg dark parts and low-Mg bright parts within same garnet grain is well displayed.
(c)	Big garnet grain with irregular boundaries comprises clinopyroxene and orthopyroxene inclusions. Garnet is surrounded by amphibole and appears homogeneous due to relatively small magnification.
(d)	Corundum and spinel inclusions in inhomogeneous garnet display semi-parallel orientation. Spinel inclusions in this case might be interpreted as remnants of primary low-pressure stage or as secondary minerals. It is also not clear whether corundum minerals are real inclusions or maybe exsolutions from garnet.
(e)	Cr-Spinel inclusion in garnet represents primary spinel overgrown by garnet during subduction.
(f)	Garnet rims are replaced by symplectitic intergrowth of Al-orthopyroxene, Al-spinel, diopside and Prg-amphibole. As a result of retrogression, garnet shows a decrease in Mg (darker parts) and increase in Fe (brighter parts). Amp-amphibole, Cpx-clinopy-roxene, Crn-corundum, Grt-garnet, Ol-olivine, Opx-orthopyroxene, Spl-spinel.
The most pronounced feature of garnets from the studied garnet peridotites is their patchy appearance (Figure 4b) caused by chemical inhomogene-ity. Patchy garnets were found in samples from both localities, although garnets from Prihovca are slightly more homogeneous than those from Visole. Dark parts of garnets are Mg-rich with 60 to 68 mol% of pyrope and are corresponding to peak pressure compositions. Bright parts are Ca-
and Fe-rich, but Mg-poor with much lower pyrope content (54 to 56 mol%). During decompression, Mg is moving out of garnet which results in enrichment of Ca and Fe. Compositional change between the dark and bright parts in garnets can be well expressed with magnesium number (Mg#):
Mg#= 100 • Xf^ = 100
Mg
Mg +Fe
2 +
Figure 5. Chromian-rich spinel occurring in matrix (BSE). Matrix minerals in (b) are mostly olivine and amphibole. Both grains show weak zonation indicating an increase of Cr content from core to rim. Amp-amphibole, Cpx-clinopyroxene, Ilm-ilmenite, Ol-olivine, Opx-orthopyroxene, Spl-spinel.
In the dark parts Mg# is reaching 0.78, whereas it never exceeds 0.68 in the bright parts. Relatively slow diffusion processes caused an irregular distribution of composition that resulted in patchy texture of garnet.
Inclusions in garnets are typically clinopyrox-ene, orthopyroxene (Figure 4c), corundum (Figure 4d) and spinel (Figure 4e). Mg# of garnet close to the interface with clinopyroxene inclusion (0.74) is slightly lower than Mg# of garnet next to orthopyroxene inclusion (0.76) indicating that compositional modification of garnet is higher next to clinopyroxene than next to orthopyroxene. Cr-spinel inclusions are remnants of the primary low-pressure stage that was overgrown by garnet during subduction. Pressure increase and possibly cooling governed formation of garnet on expense of spinel, clinopyroxene and orthopyroxene.
Garnets are replaced by kelyphitic rims consisting of symplectitic intergrowth of high-Al orthopyroxene, Al-rich spinel, diopside and par-gasitic amphibole (Figure 4f). Chromium number (Cr*) in Al-spinel is ranging from 0.6-0.9 and is calculated from:
Cr =100-
Cr
Cr+Al
Kelyphitic assemblage around garnets formed during the exhumation-related decompression of these rocks. Decompressional breakdown of garnet caused the diffusion of Mg and Al in spinel and Ca in clinopyroxene. As a result of retrogression, garnet shows a decrease in Mg and increase in Fe.
Spinel group minerals form two generations, the brown chromian-rich spinel and the green aluminum-rich spinel. Cr-spinel occurs in the matrix (Figure 5a) and as inclusions in garnet (Figure 4d, e). Cr-spinel inclusions are remnants of the primary low-pressure stage that was overgrown by garnet (Figure 4e) during subduction due to pressure increase and possibly cooling.
The composition of Cr-spinel ranges from Al2O3 = 24.3-53.5 wt%, Cr2O3 = 13.9-38.7 wt% and Mg# = 40.7-68.2. Cr-spinel shows a weak zoning with
mainly lighter rims and darker cores (Figure 5b). The lighter spinel has a higher chromium number (Cr* = 47-52) than the darker spinel (Cr* = 22-43). During the growth, garnet takes up the Al from the spinel, which consecutively becomes more Cr-rich at the rim and thus lighter in color. Al-spinel represents a second generation that may be found in symplectites, mostly with Al-orthopy-roxene replacing garnet (Figure 4f). The composition of Al-spinel ranges from Al2O3 = 57.7-69.6 wt%, Cr2O3 = 0-2.8 wt%, Mg# = 76.3-85.5 and Cr* = 0-3.1.
Olivine grains are unzoned and nearly homogeneous in composition (Figure 6a). The chemical homogeneity of olivine may be explained by the fact that olivine is a mineral with fastest diffusion of elements. Fe-Mg diffusion in olivine is about two orders of magnitude faster than in pyroxene and garnet (Brenker & Brey, 1997). Olivine mainly occurs as matrix mineral sometimes containing clinopyroxene (Figure 6a) and orthopyroxene inclusions. Forsterite content of the studied olivine is ranging in very wide range from 77.0 to 91.0. Olivine contains 0.02-0.28 wt% MnO, <0.07 wt% CaO, <0.02 wt% TiO2 and <0.15 wt% Cr2O3. NiO content is rather variable and is reaching up to 0.38 wt%.
Olivine is intensively fractured and broken down into smaller grains due to retrogression (Figure 6b). Cracks are filled with secondary opaque minerals. In the contact zones between olivine and garnet extensive kelyphitic coronas have been developed (Figure 6b). They consist of diopsidic clinopyroxene, orthopyroxene, Al-spinel and par-gasitic amphibole. Kelyphitisation results from a metamorphic reaction between olivine and garnet during retrogression. The relative abundance of amphibole and clinopyroxene in kelyphitic rims probably reflects local fluctuations of PH2O during kelyphite growth (Godard & Martin, 2000).
Orthopyroxenes occur as four different types of grains: (1) small inclusions in garnet (Figure 4c); (2) symplectitic intergrowth with Al-spinel replacing garnet (Figure 4f); (3) oriented lamellar exsolutions from clinopyroxene; and (2) individu-
Figure 6. Olivine grains in BSE.
(a)	Homogeneous olivine with small clinopyroxene inclusion.
(b)	Kelyphitic corona in contact between garnet and olivine. Olivine grains are broken down into numerous individual particles due to retrogression and weathering. Cracks are often filled with opaque secondary minerals. Amp-amphibole, Cpx clinopyroxene, Grt-garnet, Ol-olivine, Opx-orthopyroxene, Spl-spinel.
al matrix grains (Figure 7). Regardless of their occurrence, grain size and textural origin, the analyzed orthopyroxene grains are very similar in composition. All orthopyroxenes are enstatites (En = 83.7-92.1) with Mg-numbers varying from 83.9 to 92.4. Al2O3 and Cr2O3 concentrations range form 0.73-2.98 wt% and 0-0.20 wt%, respectively. CaO and TiO2 contents in all measured orthopyroxenes are low with <0.56 wt% for CaO and <0.05 wt% for TiO2. MgO (31.67-35.70 wt%) and MnO contents are typical for worldwide orthopyroxene compositions with MnO in some cases extended to slightly higher values (up to 0.26 wt%).
Matrix orthopyroxenes are found in the form of small rounded grains (Figure 7a) or as large an-hedral minerals (Figure 7b). The latter commonly reveal intracrystalline exsolution microstructures, consisting of numerous oriented ilmenite and clinopyroxene lamellas, which precipitated from a suprasaturated high-T orthopyroxene host (van Roermund et al., 2002). Exsolution lamellas exhibit parallel orientation and are concentrated in the central parts of the orthopyroxene grains. The rims of orthopyroxenes are free of exsolutions due to re-crystallization. Some of the orthopyroxenes
reveal internally folded exsolution lamellas (Figure 7b), suggesting that exsolution process was either accompanied or postdated by deformation. Some matrix orthopyroxenes also contain small exsolutions of pargasitic amphibole and garnet. Interstitial garnet exsolutions show very distinct bleb-like shapes (Figure 7b) and are mostly present along the orthopyroxene exsolution-free grain boundary. They show similar microstructures to those reported from garnet websterites in Norway (van Roermund et al., 2002).
Large matrix orthopyroxene grains are often very low in Al2O3 content (down to 0.73 wt%), which reflects high-pressure conditions during their formation. Al content in orthopyroxene is a good diagnostic criteria for revealing pressure variations during the metamorphic evolution. In general, Al decrease can be due to increase in pressure or decrease in temperature (cooling). Inversely, increase in Al content is caused by decompression or heating. High-temperature orthopyroxenes are thus characterized by low Al and high Ca contents. In the analyzed orthopyroxenes the distribution of Al shows lowest Al and highest Ca content in the core. This indicates a decrease in
Figure 7. Matrix orthopyroxenes (BSE).
(a)	Small rounded orthopyroxene grains in contact with clinopyroxenes and amphiboles.
(b)	Bended exsolutions occupying the central part of orthopyroxene grain with re-crystallized, exsolution-free rim. Garnet blebs are arranged along the orthopyroxene grain boundary. Amp-amphibole, Cpx-clinopyroxene, Grt-garnet, Ilm-ilmenite, Opx-ortho-pyroxene.
Figure 8. Matrix clinopyroxene grains (BSE).
(a)	Individual matrix clinopyroxene grain is rimmed by amphibole and is representing the relict phase of primary material; clinopyroxene inclusions in olivine are also observable.
(b)	Garnet, ilmenite and clinopyroxene exsolutions within orthopyroxene host exhibit a clearly visible parallel orientation; in some cases the exsolutions occur in two perpendicular sets. Amp-amphibole, Cpx-clinopyroxene, Grt-garnet, Ilm-ilmenite, Opx-orthopyroxene, Prg-pargasite, Tr-tremolite.
pressure and temperature from core to rim, consistent with exhumation and decompression of the rocks.
Clinopyroxene occurs in form of matrix grains (Figure 8a), inclusions in garnet (Figure 4c), olivine (Figure 6a) and orthopyroxene, exsolutions from orthopyroxene (Figure 7b) and in complex coronas in contact zone between olivine and garnet (Figure 6b). All analyzed clinopyroxenes are diopsides (En = 46.6-57.8, Fs = 0.1-6.1, Wo = 36.151.0) with Mg-numbers ranging from 90.0-99.8. They have low Na2O and Cr2O3 content varying from 0.19-0.82 wt% and 0-0.67 wt%, respectively. The Al2O3 content is ranging from 0.73-4.87 wt% but TiO2 content is mostly below 0.13 wt%. No significant compositional differences between clinopyroxene minerals with different occurrence and textural type can be observed. This is taken as good evidence for equilibrium conditions.
Coarse-grained matrix clinopyroxene minerals often contain numerous exsolution lamellas of garnet, low-Al orthopyroxene, ilmenite and par-gasitic amphibole (Figure 8b). The size of lamellas is very varied and is ranging from very tiny rods (<10 |im) of ilmenite and orthopyroxene to larger elongated exsolutions (up to several 100 |im in length) of garnet and orthopyroxene. Amphibole and some orthopyroxene exsolutions are remarkably thicker and relatively short. The obvious intergrowth of different exsolution lamellas and the lack of a clear-cut relationship might suggest a nearly simultaneous generation (Xu et al., 2004). All garnet exsolutions lie in a direction parallel to the c axis. Some ilmenite lamellas occur in two orientations with nearly perpendicular intersections (Figure 8b), suggesting a topotactical inter-growth due to exsolution rather than being a primary intergrowth or epitaxial replacement (Zhang & Liou, 2003).
Matrix clinopyroxene grains are in most cases rimmed by amphiboles of pargasitic and tremo-litic composition (Figure 8a).
Other minerals present in the analyzed garnet peridotites and pyroxenites were formed after peak pressure conditions and are related to retrogression due to the exhumation of these rocks. These are typically amphibole, chlorite, serpentine and talc. With decreasing temperature, par-gasitic amphibole that is replacing clinopyroxene and which might be stable at pressure conditions up to 25 kbar, is successfully transformed to tremo-lite, chlorite and serpentine minerals.
Amphibole occurs in 3 different generations: (1) pargasite; (2) tremolite; and (3) gedrite. Bright Na-rich amphibole belongs to pargasite compositions with Mg-number ranging from 89.9-98.1. Parga-sitic amphiboles occur around matrix clinopyro-xene grains in form of retrogressive rims (Figure 8a), as exsolutions in clinopyroxene (Figure 8) and in kelyphitic intergrowth replacing the contact zone between garnet and olivine (Figure 6b). A common retrogression product of ultramafic rocks is also orthoamphibole of gedritic composition. It is known to be forming in lower amphibolite facies conditions, possibly by reactions involving chlorite. The amphibolitization process postdated the formation of symplectitic replacement rims around major mineral phases. In some cases amphibole grains resemble inclusions or have idio-morphic forms, but they are always connected to the periphery with fluid channels and are thus indisputably of secondary origin.
Chlorite, serpentine and talc formed under lowest P-T conditions as late retrogressive stages partly replacing olivine and pyroxene minerals.
Geothermobarometry
Metamorphic conditions for the formation of garnet peridotites have been calculated from a combination of the garnet-olivine (O'Neill & Wood, 1979; O'Neill, 1980) and garnet-orthopy-roxene (Harley, 1984) Fe2+-Mg exchange thermometers, and Al-in-orthopyroxene barometer (Brey & Köhler, 1990).
Figure 9. Estimated pressure and temperature conditions with suggested metamorphic P-T path for Pohorje garnet perido-tites. A combination of garnet-olivine Fe2+-Mg exchange ther-mobarometer (OW-80; O'Neill & Wood, 1979), garnet-ortho-pyroxene Fe2+-Mg exchange thermobarometer (H-84; Harley, 1984), and Al-in-orthopyroxene barometer (BK-90; Brey & Köhler, 1990). Shown for reference are equilibria for diamondgraphite (Bundy, 1980), coesite-quartz (Bohlen & Boettcher, 1982), and spinel-garnet peridotite (O'Hara et al. 1971).
The initial (pre-peak) metamorphic conditions have been calculated with the application of Fe2+-Mg garnet-orthopyroxene exchange thermometer together with the Al-in orthopyroxene barometer to the garnet and orthopyroxene exsolutions in primary clinopyroxene. Estimated P-T values are 730 °C at pressure of 2.6 GPa.
Porphyroblastic garnet with the highest pyrope content and orthopyroxene with the lowest Al content together with relatively homogeneous olivine have been chosen to calculate peak P-T conditions, as it is generally recommended (e.g. Brey & Köhler, 1990; Brenker & Brey, 1997; Krogh Ravna & Paquin, 2003). The results indicate that the peak of metamorphism occurred at temperatures of 887-962 °C and pressures of 3.4-4.0 GPa (Figure 9). The equilibrium P-T conditions for the sample 119 cluster in a narrow range, close to values of 900 °C and 4 GPa. There is a very good consistency between the garnet-olivine and garnet-orthopyroxene Fe2+-Mg exchange thermometers for this sample. The P-T conditions for sample VI01/04, obtained from the garnet-olivine thermometer and the Al-in-orthopyroxene barometer, are 887 °C and 3.4 GPa, whereas the intersection between the garnet-orthopyroxene thermometer and the Al-in-orthopyroxene barometer yields
962 °C and 3.9 GPa. This discrepancy may result from partial disequilibrium between garnet, olivine and orthopyroxene during post-peak decompression. Additionally, since all Fe has been treated as Fe2+ in the calculations, the temperature obtained by garnet-orthopyroxene thermometer should only be regarded as minimum peak temperature (Harley, 1984).
The post-peak metamorphic conditions have been deduced from the composition of orthopy-roxene in symplectites with Al-rich spinel that form kelyphitic rims around garnet. The garnet-orthopyroxene Fe2+-Mg exchange thermometer in combination with the Al-in-orthopyroxene barometer yields P-T conditions of ~800 °C and 2 GPa.
Discussion and Conclusions
The geothermobarometrical data obtained from garnet peridotites, with peak P-T conditions of 887-962 °C and 3.4-4.0 GPa, clearly confirm the existence of UHP metamorphism in the Pohorje area. Recorded peak metamorphic conditions are in the same range as peak conditions determined for the associated kyanite eclogites (Janak et al., 2004; Vrabec, 2010). This confirms that the south-easternmost parts of the Austroalpine nappes in the Alps reached UHP metamorphic conditions during the Cretaceous orogeny at ca. 91-92 Ma. Garnet peridotites were most probably introduced to the subducting plate from the overlying mantle wedge and later on subducted further to the depths of at least 120 km.
From observed mineral assemblages and estimated P-T conditions a metamorphic P-T path can be deduced (Figure 9). The reaction textures, mineral compositions and thermobarometric evidence indicates that garnet-bearing peridotites have undergone a complex history, including at least four stages of recrystallization: protolith stage, metamorphic stage, decompression stage, and retrogression stage.
Stage I: the protolith stage, is garnet-free and is defined by assemblage of olivine + Al-orthopy-roxene + Al-clinopyroxene + Cr-spinel. Al-orthopy-roxene occurs as inclusions in garnet, whereas Cr-spinel is additionaly preserved in the matrix. The initial composition of the investigated peri-dotite most probably corresponded to spinel lher-zolite. The occurrence of Cr-spinel as inclusions in garnet indicates that garnet peridotites evolved from spinel-bearing protolith, which could therefore represent pieces of intermediate to shallow-level lithospheric mantle.
Stage II: the metamorphic stage, is defined by the matrix assemblage of garnet + clinopyrox-ene + orthopyroxene + olivine + Cr-spinel. Garnet occurs as coronas around Cr-spinel, as exsolutions from clinopyroxene, and as large porphyroblasts in the matrix. Primary, coarse-grained clinopy-roxene contains exsolution rods of garnet, low-Al
orthopyroxene, pargasitic amphibole, Cr-spinel and ilmenite.
Formation of garnet exsolutions from clinopy-roxene could have started at P-T conditions of about 700-750 °C and 2.5 GPa, as deduced from geothermobarometry. The exsolution process may correspond to the incorporation of peridotite from the overlying mantle wedge into subducting crust. The interaction between the hot mantle and the relatively colder subducting crust probably caused nearly isobaric cooling from spinel to garnet stability field. Similar exsolutions have been observed in other HP and UHP ultra-mafic rocks, e.g. garnet peridotite and pyroxenite from Nonsberg area, Eastern Alps (Godard et al., 1996), garnet clinopyroxenite from Sulu, eastern China (Zhang & Liou, 2003) and garnet websterite from Bardane, western Norway (Carswell & van Roermund, 2005). The formation of exsolutions in clinopyroxene is undoubtedly caused by reactions driven by changes in temperature and pressure, but the accurate conditions are difficult to estimate. The parent phase of such intergrowths of clinopyroxene + garnet + ilmenite could have been the primary clinopyroxene (Zhang & Liou, 2003). Formation of garnet lamellas in clinopyroxene has generally been interpreted as a result of exsolution from primary clinopyroxene (Dawson & Reid, 1970; Harte & Gurney, 1975; Sautter & Harte, 1988). According to experimental work of Harte & Gurney (1975) a single clinopyroxene is stable in a wedge shaped P-T stability field below the solidus (~3.4-3.8 GPa at 1380-1400 °C; 2.6 GPa at 1370 °C). With decreasing temperature, garnet first appears at ~1400 °C and 3.4-3.6 GPa, joining the clinopyroxene and forming a clinopyroxene + garnet assemblage. Hence, the exsolution of garnet from clinopyroxene has been suggested to be related mainly to cooling from near-solidus conditions toward normal mantle lithosphere temperatures. Although the effect of Ti was not evaluated in Harte & Gurney (1975) experiments, a similar clinopyroxene precursor of the garnet + ilmenite + clinopyroxene intergrowth is suggested, as the solubility of clinopyroxene (CaMgSi2O6) in garnet is limited except for majorite formed at very high pressures (see Fig. 6 in Zhang & Liou, 2003).
During the peak of metamorphism large por-phyroblastic garnet was formed from primary, Al-bearing phases such as spinel, clinopyroxene and orthopyroxene. The increased chromium content in the rims implies that Cr-rich spinel (Cr* = c. 50) remained stable at peak metamorphic conditions, since chromium moves the spinel-garnet transition boundary towards higher pressures (Webb & Wood, 1986; Klemme, 2004). P-T conditions of the peak metamorphic stage calculated from geo-thermobarometry are 887-962 °C and 3.4-4.0 GPa, that is well within the stability field of coesite.
Stage III: the decompression stage, occurred after peak pressure conditions and is manifested by formation of kelyphitic rims of high-Al orthopy-roxene, Al-spinel, diopside and pargasitic amphibole replacing garnet. After having reached their
metamorphic peak, the garnet peridotites were exhumed to mid-crustal levels. The composition of orthopyroxene in symplectites with Al-rich spinel was used to obtain P-T conditions during decompresion. The garnet-orthopyroxene Fe2+-Mg exchange thermometer in combination with the Al-in-orthopyroxene barometer yields P-T conditions of ~800 °C and 2 GPa.
Stage IV: the retrogression stage, occurred under lowest P-T conditions and is characterized by the formation of tremolitic amphibole, gedrite, chlorite, serpentine and talc. Pargasitic amphibole was partly replaced by tremolite, pyroxene by serpentine and chlorite, and olivine by serpentine and talc. It is assumed that pressure and temperature further decreased during this stage. The increased activity of H2O caused retrogression under low P-T conditions.
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