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Dehydration--MeltingPhenomenainLeptyniticGneissesandtheGenerationofLeucogranites:aCaseStudyfromtheKeralaKhondaliteBelt,SouthernIndia

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JOURNAL OF PETROLOGY VOLUME 37 NUMBER 6 PAGES 1285-1305 1996

I. BRAUN1*, M. RAITH1 AND G. R. RAVINDRA KUMAR1

'MINERALOGISCH-PETROLOGISCHES INSTITUT, UNIVERSITAT BONN, POPPELSDORFER SCHLOB, D-53II5 BONN, GERMANY"CENTRE FOR EARTH SCIENCE STUDIES, AKKULAM, TRIVANDRUM 6950J1, INDIA

Dehydration-Melting Phenomena inLeptynitic Gneisses and the Generation ofLeucogranites: a Case Study from theKerala Khondalite Belt, Southern India

Pan-African high-grade metamorphism in the Kerala Khonda-lite Belt (South India) led to the in situ formation of garnet-bearing leucosomes (LJ) in sodic quartz-alkali feldspar—biotitegneisses. Microtextures, mineralogy and the geochemical char-acteristics of in situ leucosomes (LJ) and gneiss domains(GnD) indicate that the development of leucosomes wasmainly controlled by the growth of garnet at the expense ofbio-tite. This is documented by the selective transfer of FeO, MgO,

' Y, Sm and the heavy rare earth elements into the LJ domains.P-Tconstraints (T>800°Q ?>6kbar, a.H,o~0-3) suggestthat the leucosomes were formed through complete melting ofbiotite in fluid-absent conditions, following the model reactionBiotiU + Alkali feldspar + Qjiartz±Z Garnet+IlmeniU + Melt.The fraction of melt generated during this process was low(<J0 vol.%). The identical size of the leucosomes as well astheir homogeneous and isotropic distribution at outcrop scale,which lacks any evidence for melt segregation, suggest that themigmatite remained a closed system. Subsequent to migmatiza-tion, the leptynitic gneisses were intruded by garnet-bearingleucogranitic melts (L2), forming veins parallel and sub-perpendicular to the foliation. The leucogranites are rich inpotassium (K2O~5-5 wt%), (Ba~400 p.p.m.) and Sr(~300 p.p.m.), and exhibit low concentrations of Zr (—Wp.p.m.), Th (<1 p.p.m.) and Y (<10 p.p.m.). The chondrite-normalized REE spectra show low abundances (La^~20,Lun ~ 3) and are moderately fractionated (La^/Lus ~ 7). AnEu anomaly is absent or weakly negative. The higher Sr/ Srratio at 550 Ma (0-7345) compared with the migmatite(0-7164) precludes a direct genetic relationship between lepty-nitic gneisses and leucogranites at Manali. Nevertheless, thechemical and mineralogical compositions of the leuocogranitesstrongly favour a derivation through fluid-absent biotite melting

of isotopically distinct but chemically comparable Manali-typegneisses. The undersaturation of %r, Th and REE, a typicalfeature of leucogranitic melts generated during granulite fadesanatexis of psammo-pelitic lithologies and attributed to dis-equilibrium melting with incomplete dissolution of accessoryphases (zircon, monazite), is weakly developed in the leuco-granites of Manali It is concluded that this is mainly due tothe sluggish migration of the melts in static conditions, which

facilitated equilibration with the restitic gneisses.

KEY WDRD& dehydration-milting leptynitic gneisses; in situ leuco-somes; leucogranites; Kerala Khondalite Belt

INTRODUCTIONMigmatites terranes have attracted considerableinterest because they offer windows into those levelsof the deeper crust where granitic melts are gen-erated by partial melting and segregation in aspectrum of lithologies and in contrasting physico-chemical regimes (see Mehnert, 1968; Atherton &Gribble, 1983; Ashworth & Brown, 1990; Brown,1994; Brown et al., 1995). The interpretation of theprocesses involved in the formation of migmatites,however, is not straightforward. A major problemconcerns the origin of the leucosome domains. Thesemay form through a variety of contrasting processes:(1) melting reactions with or without participationof hydrous phases and in the presence or absence of afree fluid phase (sec Thompson, 1982; Waters &Whales, 1984; Watt & Harley, 1993; Carrington &Harley, 1995); (2) subsolidus dehydration reactions

•Corraponding author. Rue 0228-732763;e-mail: ingo.braun@uni-bonn.de © Oxford University Preu 1996

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JOURNAL OF PETROLOGY VOLUME 37 NUMBER 6 DECEMBER 1996

(Sawyer & Barnes, 1988; Stuwc & Powell, 1989); (3)feldspathization of early quartz segregations (Harteetal., 1991; Masberg, 1996).

For a discrimination of partial melting vs sub-solidus processes, the microtextures, mineral com-position systematics and element fractionation datamay provide important clues (McLellan, 1983;Sawyer & Barnes, 1988; Powell & Downes, 1990).The interpretation of the data, however, is often notunequivocal. In most cases the P-T conditions pre-vailing during the leucosome development cannot betightly constrained and, more important, the fluidregime which strongly controls the P-T location ofthe dehydration and melting equilibria remainspoorly known. Changes of the fluid regime (OH,O)

m

space and time are likely to occur and might triggerdifferent dehydration and dehydration-melting pro-cesses in closely associated domains or even within asingle domain of the rock. Furthermore, because ofthe marked compositional differentiation and tex-tural modifications between leucosome and adjacentgneiss domains, the mineralogy, texture and bulkchemical composition of the precursor gneiss canonly be inferred based on certain assumptions (e.g.closed system behaviour, known P—T-ay^o condi-tions, etc.). The uncertainties in such an approachgenerally impede a comprehensive characterizationof the initial and progressing stages of leucosomedevelopment as a function of the intensive variablestemperature, pressure and water activity. In parti-cular, the recognition of the proportion and chemicalcomposition of the melt phase poses a most intricateproblem. It is evident that field-oriented studies oncrustal anatexis have good prospects only if they arebased on migmatites with a discernible evolutionaryhistory.

Within the Late Proterozoic Kerala KhondaliteBelt in southern India, the widespread biotite-bearing gneisses have been subjected to partial ana-texis at upper amphibolite to granulite fades condi-tions (Srikantappa et al., 1985; Chacko etal., 1992).These migmatites show a sequence of garnet-bearingleucosome types which documents the progress ofmigmatization through continued biotite dehy-dration—melting. Initial stages are represented byisolated small in situ leucosomes—described in thispaper—which formed through biotite breakdown atpresumably very low degrees of melting. From tex-tural and geochemical criteria the presence of a meltphase at this stage is difficult to constrain. In con-trast to this, in other localities a significantly higherdegree of migmatization is achieved and field obser-vations clearly indicate that melting was extensive.There the formerly isolated leucosomes combine andbuild up a network of thin veins which tends to dis-

integrate the gneissic structure. The leucosome togneiss ratio steadily increased and eventually resultsin a leucocratic matrix that contains small gneissdomains of variable size and random orientation.The segregation, coalescence and migration of thegenerated melt finally leads to the intrusion ofgarnet-bearing leucogranites into the migmatites.Fortunately, the whole ensemble has not been over-printed by subsequent ductile shear deformation, asis the case in many high-grade terrains exposingcomparable phenomena of migmatization, e.g. theleptynitic and khondalitic granulites of Lapland(Barbey & Cuney, 1982), Sri Lanka (Prame & Pohl,1994), the Eastern Ghats Belt of India (Dasgupta etal., 1992) and southern Madagascar (Nicollet,1990). Among the numerous visited localities to theeast and north of Trivandrum, the active quarries atManali (Fig. 1) ideally expose the dehydration-melting phenomena and therefore have been chosento investigate three major aspects of crustal anatexis:(1) the processes through which granitic melts aregenerated at conditions of a fluid-absent granulitefacies regime; (2) the mechanisms of melt segre-gation and melt migration; (3) the geochemicalcharacteristics of these melts and their affinity withgranites from distinct lithologies and geotectonicsettings.

GEOLOGICAL SETTINGThe Kerala Khondalite Belt (KKB) south of theAchankovil Shear Zone in Kerala, the youngestcrustal terrain of Peninsular India, was accreted tothe Late-Archaean and Proterozoic granulite ter-rains in the north during the Pan-African orogeny(Buhl, 1987; Choudhary et al., 1992; Kohler et al.,1993). Accounts on the geology and metamorphicevolution of the KKB were given by Srikantappa etal. (1985), Santosh (1986, 1987), Ravindra Kumar& Chacko (1986) and Chacko et al. (1987, 1992).The KKB became well known through its specta-cular exposures of arrested charnockite formation(Srikantappa et al., 1985; Hansen et al., 1987;Jackson et al., 1988; Santosh et al., 1990; Raith &Srikantappa, 1993).

The studied quarries at Manali lie in the PonmudiUnit, which forms the central and northern part ofthe KKB (Fig. 1). The unit is made up of anintensely deformed series of high-grade psammo-pelitic metasediments. The dominant rock types aremigmatitic garnet-biotite gneisses (leptyniticgneisses—dealt with in this paper—and graniticaugen gneisses), garnet-biotite-sillimanite gneisses(khondalites) with gradations into quartzitic typesand garnet—biotite—sillimanite—cordierite gneisses.

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BRAUN itaL DEHYDRATION-MELTING OF LEPTYNITIG GNEISSES

T—Madras

12°

— 9°00' N

Ponmudi Unit

ArabianSea

0— 8°3O'

10I

km Trivandrum

76°30' E

Nagerkovil Unit

Fig. 1. Geological sketch map of the northweiteni part of the Kerala Khondalite Belt showing the loc»tion of Manali (filled star) andadditional outcrops with lodic leptynitic garnet—biotite gneissei (open star). The inset map shows the major lithouniu and shear zones ofsouthern Peninsular India. 1, Phanerozoic cover, 2, crustal terrains affected by Early Proterozoic granulite-facies metamorphism ~2'5Ga ago; 3, crustal units of the Kodailcanal Massif (KM) affected by Late Proterozoic granulite-facies metamorphism ~550 Ma ago; 4,crustal units of the Kerala Khondalite Belt (KKB) affected by Late Proterozoic granulite-faciei metamorphism ~550 Ma ago; 5,Archaean gneiis-granitoid-greenstone terrain of the Dharwar Craton (DC): N, Nilgiri Hills; BR, Biligirirangan HilU; S, Shevaroy

Hills; MSZ, Moyar Shear Zone; BSZ, Bhavani Shear Zone; PCSZ, Palghat-Cauvery Shear Zone; ASZ, Achankovil Shear Zone.

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JOURNAL OF PETROLOGY VOLUME 37 NUMBER 6 DECEMBER 1996

Rarely, folded, stretched and boudinaged bands ofcalc-silicate rocks and basic granulites do occur,documenting as marker horizons the intense poly-phase ductile deformation of the entire series (Sri-kantappa et al., 1985; Chacko et al., 1987, 1992;Yoshida & Santosh, 1994). The coarse-grainedgranitic garnet-biotite gneisses often display a con-spicuous augen texture of recrystallized K-feldsparporphyroblasts. They have been mainly recognizedin the northern part of the Ponmudi Unit and wererecently interpreted to be porphyritic granite bodiesintrusive into the metasedimentary sequence ofleptynitic and khondalitic gneisses (Braun, 1994).Contrary to previous interpretations (RavindraKumar & Chacko, 1986; Chacko et al., 1992), gran-itoid orthogneisses apparently constitute animportant component of the KKB.

High-grade metamorphism and polyphase defor-mation in the KKB occurred during the Pan-Africanevent, ~550 m.y. ago (Buhl, 1987; Choudary et al.,1992; Kohler et al., 1993) and resembles thetectonothermal evolution of the Highland Complexin Sri Lanka (Holzl et al., 1991, 1994) and theAndroyen Complex in southern Madagascar(Nicollet, 1990). Geothermobarometric data indicatea subtle regional P-T gradient from upper amphi-bolite to granulite facies (760±50°C, 5-6 ±0-8 kbar,Xnto = 0-2—0-3) in the Ponmudi Unit to pervasivegranulite facies (790±50°C, 6-3 ±0-8 kbar,X^o — 0-2-0-3) in the Nagerkovil Unit, which formsthe southern part of the KKB (Srikantappa et al.,1985; Chacko et al., 1987; Ehl, 1989).

DEHYDRATION-MELTINGPHENOMENA IN THELEPTYNITIC GNEISSESField aspectsThe characteristic feature of leptynitic gneisses inthe Ponmudi Unit is their conspicuous migmatiticstructure. Garnet-bearing leucosomes of a fewcentimetres size developed in fairly homogeneous,medium-grained quartz-feldspar-biotite gneisses ofgranitic to granodioritic composition. Garnet eitheraggregates in the centre of the leucosomes oroccurs in streaky alignment which mimics theformer gneissic foliation. The isotropic and unde-formed fabric of the quartzofeldpathic matrix ofthe leucosomes precludes that the garnet streaksoriginated through penetrative deformation of thegneisses.

At Manali the in situ leucosomes (LI) are com-posed of alkali feldspar, quartz and garnet. Garnetalways occurs aggregated in the centre of the

leucosomes, and is separated from the quartzofeld-spathic matrix by a rim of quartz. The boundariesof the leucosomes with the biotite gneiss are dis-tinct. In sections perpendicular to the foliation theleucosomes usually exhibit lens-like shapes andoccur as isolated domains (Fig. 2a-c). Rarely,they combine into layers parallel to the gneissicfabric. In the foliation plane the interconnectivitybetween the leucosomes is much more pronouncedand they rather display circular to irregular shapes.The leptynitic gneisses thus can be regarded as athree-dimensional biotite gneiss network with'interstitial' garnet-bearing in situ leucosomes. Thesize, distribution and orientation of the leucosomesin the leptynitic gneiss at Manali are remarkablyuniform over a distance of several hundred metres.The isotropic fabric indicates that their formationpostdates the polyphase deformation of the hostgneiss and that they developed in essentially staticconditions.

The participation of melt in the leucosome for-mation is difficult to constrain. Macro- and micro-textures do not provide evidence for the generationof large volumes of melt during migmatization. Aspointed out above, the migmatitic structure of theleptynitic gneisses is homogeneous over great dis-tances. We did not see paths of melt segregation orcoalescence of melt in pools nor did we recognizerocks that could be interpreted as the restates ofleptynitic gneisses after melt extraction. Followingmigmatization, the fluid species which were liber-ated through biotite breakdown and resolved in themelt fraction must have left the system, as norehydration has affected the dry leucosome assem-blage. However, the amount of fluids was smalland their escape should not have significantlychanged the bulk chemical composition. This leadsus to assume a closed system behaviour duringmigmatization, at least at the decimetre to metrescale. The composite of gneiss domains and in situleucosomes therefore is considered to satisfactorilymatch the chemical composition of the precursorbiotite gneiss.

Following the formation of the in situ leucosomes,garnet-bearing leucogranitic melts intruded the lep-tynitic gneisses. They were emplaced as sheets anddykes subparallel to the gneiss foliation, with thick-nesses in the centimetre to metre scale, and as thinveins cross-cutting the foliation (Fig. 2a). Theabsence of cross-cutting relations between the dif-ferent types of veins and the almost identical chem-ical and mineralogical composition of theleucogranites suggests their formation throughsimultaneous emplacement of melt in a tensionalstress regime which facilitated the formation of veins

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BRAUN et aL DEHYDRATION-MELTING OF LEPTYNITIC GNEISSES

(a)

(b) (c)

Fig. 2. Photographs illustrating the field setting and the macrotextures of leptynitic gneisses at Manali. (a) Outcrop view showing thespatial relationship between leucogranites and leptynitic gneiss. The leptynitic gneiss consists of in situ leucosomes (LI) set in three-dimensional gneiss-network. The leucogranitej (L2) postdate the formation of in situ leucosomes (LI) and were emplaced as dykes andveins either subperpendicular or parallel to the foliation of the gneisses. The diameter of the lens cap is 55 mm. (b) This photographshows the rather homogeneous distribution of garnet-bearing in situ leucosomes (LI) in the leptynitic gneiss. The leucosomes occurisolated or tend to combine into a network and their sizes do not exceed 3 cm. The width of the photograph is 20 cm. (c) A close-upview of the leptynitic gneiss displays the sharp contact relations between in situ leucosomes and gneiss domains. Garnet is concentrated inthe centre of the leucosomes, which exhibit a granoblastic texture and do not adopt the weak foliation of the biotite-bearing gneiss

domains. The long side of the photograph is 8 cm.

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JOURNAL OF PETROLOGY VOLUME 37 NUMBER 6 DECEMBER 1996

in the foliation plane and in a subpcrpendicular setof conjugated extensional planes.

A late-stage phenomenon of the high-grade meta-morphic evolution of the KKB is the structurallycontrolled process of arrested charnockitization(Harris et al., 1993; Raith & Srikantappa, 1993, andreferences therein). At Manali, in some parts of theoutcrops the leptynitic gneisses and the leucograniteveins are affected by this local process of dehydrationalong the foliation and a set of fractures, similar tothe phenomena observed in Kottavattam (Raith &Srikantappa, 1993, Fig. 2a).

Parageneses, modes and microtextures ofgneiss domains, in situ leucosomes andleucogranitesThe gneiss domains (GnD) are homogeneous, ofmedium grain-size and exhibit a granoblastic micro-texture with strongly embayed gTain boundaries.The foliation is ill developed, and is defined bybiotite flakes crudely aligned within the quartzo-feldspathic matrix. Accessory phases are zircon,monazitc, apatite and ilmenite. The mode of thegneiss domains is granodioritic according to theclassification of LeMaitre (1989) (Table 1).

Potassic feldspar and plagioclase form coarsegraphic intergrowths surrounding relict mesoperthitegrains. These microtextures are a characteristicfeature of leptynitic gneisses throughout thePonmudi Unit. The intergrowths developed betweenadjacent mesoperthite grains through subsolvusreplacement reactions. Individual intergrowthdomains retain the lamellae orientation of the meso-perthite grain from which they expanded into the

opposite grain. Towards the replacement front, theintergrowth becomes increasingly coarse and in somecases gives way to an aggregate of individual potassicfeldspar and plagioclase grains. These observationssuggest that the feldspar phase in the precursorgneiss (PGn) was essentially represented by alkalifeldspar.

The in situ leucosomes L1 are characterized by themineral assemblage alkali feldspar, quartz andgarnet, with ilmenite, zircon, monazite and apatiteas accessory phases. Garnet grains aggregate in thecentre of the leucosome domains, display anhedralshapes with strongly embayed grain boundaries andcontain abundant rounded inclusions of quartz,which also rims the garnet clusters.

The quartzofeldspathic matrix resembles that ofthe gneiss domains with a granodioritic mode (Table1) and the coarse two-feldspar intergrowth texturearmouring relict mesoperthite. Compared with thegneiss domains, the modal feldspar abundance isslightly lower (Table 1), suggesting its participationin the garnet-forming (melting) reaction. The grainsize of alkali feldspars is virtually the same as in thegneiss domains, whereas the mean grain size ofquartz is slightly larger (~l-5 mm) than in thegneiss domains (0-5-1 mm). Biotite is almost absent.It rarely forms rounded inclusions in garnet or smallrelicts in the quartzofeldspathic matrix. Instead,euhedral plates of ilmenite grew at sites of biotitebreakdown and occur in random orientation.

The leucogranites (L2), compared with the in situleucosomes (LI), have a distinctly higher modalabundance of K-feldspar but a significantly lowergarnet content. Biotite is absent. Grain sizes arecomparable with those in the leptynitic gneisses. The

Table 1: 'Near3 modal composition of the investigated samples,

calculated with the computer program MONA (Metzner &

Grimmeisen, 1990)

wt%

Quartz

Feldspar

ab, an, or

Biotite

Garnet

GnD

29

67

37,12,18

4

—

PGn

32

60

35,11,14

8

—

L1

32

65

29,10,16

—

13

L2

28

68

30,5,33

—

4

QFG

23

77

43,13,21

—

—

QFL

30

70

38,11,21

—

—

PGn gives the data of a leptynitic gneiss sample, comprising gneiss and in situ leucosomedomains (Fig. 2), which approximates the Precursor Gneiss before leucosome formation. GnD,Gneiss domain; L1, in situ leucosome; 12, leucogranite; QFG and QFL quartzofeldspathicmatrices of GnD and L1.

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BRAUN it aL DEHYDRATION-MELTING OF LEPTYNITIC GNEISSES

quartzofeldspathic matrix also exhibits granoblasticmicrotextures with strongly embayed grain bound-aries and abundant mutual inclusion relationships ofthe phases. Garnet commonly forms inclusion-free,subhedral to euhedral grains, suggesting its growthin a melt phase. It is not rimmed by quartz.

Alkali feldspars of the leucogranites are spindleperthite with a second generation of finer stringsexsolved between the coarser spindles. Large alkalifeldspar grains often show an increase in lamellaethickness towards the margin and are separated fromadjacent alkali feldspar grains by small-scalereplacement textures which resemble those in theleptynitic gneiss. The core regions of the spindleperthites contain numerous small inclusions of a lightprismatic mineral which may be tourmaline. Meso-perthites with their surrounding two-feldspar inter-growths, so typical of the gneiss and in situ leucosomedomains, usually are absent in the leucogranites.They have only been recognized close to the contactwith the leptynitic gneiss and it is suggested thatthey were taken up from the host gneiss duringleucogranite emplacement.

Plagioclasc is confined to the perthitic alkali feld-spars and to the graphic intergrowths.

ANALYTICAL PROCEDURESMicroanalyses were performed with a CamecaCamebax electron microprobe at the University ofBonn. Operating conditions were 15 kV acceleratingvoltage and 15 nA specimen current and countingtimes were 20 s (peak) and 10 s (background). Dataprocessing was performed with the PAP correctionprocedure (Pouchou & Pichoir, 1984). The beamdiameter in general was 1-2 /im. Integrated analysesof mesoperthites and graphic feldspar intergrowthswere carried out by point analysis with an enlargedbeam diameter of 5—10 /im or using the scanningoption of the microprobe. The results of bothmethods were similar, but the latter generallyyielded lower sums (94-96 wt%).

The major and trace element composition ofwhole rocks was analysed with a Phillips X-rayfluorescence spectrometer PW 1480.

Rare earth elements were analysed by inductivelycoupled plasma atomic emission spectrometry (ICP-AES) at the Universities of Clermont-Ferrand (foursamples) and Marburg (one sample), and detaileddescriptions of the sample preparation and themeasurement have been given by Cantagrel & Pin(1994) and Heinrichs & Herrmann (1990),respectively.

Oxygen isotope analyses were carried out on 10-15 mg aliquots of powdered whole-rock samples.

Purified fluorine was used for extraction of oxygen,which was then converted to CO2. Duplicate18O/16O measurements were performed on a VG-Isogas SIRA-9 triple-collector mass spectrometer;the analytical reproducibility is 0-1 %o.

Rb—Sr isotopes were determined on a CamecaTSN 206A and VG 54E double-collector mass spec-trometer at the Laboratory of Geochemistry at theUniversity Blaise Pascal, Clermont-Ferrand.

MINERAL CHEMISTRYMesoperthitic alkali feldspars in the gneiss domains(GnD) and the in situ leucosomes (LI) have identicalintegrated compositions with average values ofAb5iOr35_36An14_13 (Table 2). Graphic intergrowthsof plagioclase and potassic feldspar which developedfrom the mesoperthites have approximately the samebulk composition (Ab54Or33_38Ani3_8). In contrast,spindle perthitic alkali feldspars in the leucogranites(L2) are more potassic and have a distinctly loweranorthite content (Ab39Or56An5). These changes infeldspar composition arc also reflected by the con-trasting K.2O/Na2O ratios of the rocks (GnD andLI =0-86; L2 = l-65-l-76; sec Table 4 below) andthe more granitic composition of L2.

Plagioclase in the gneisses predominantly occurs asexsolution lamellae in mesoperthite as well as incoarse graphic intergrowths with potassic feldspar. Ithas a remarkably constant oligoclase compositionwith 22 ± 1 mol % anorthite. In the leucogranites,plagioclase lamellae in spindle perthite are slightlymore sodic (18 ±1 mol % An) (Table 2). Potassicfeldspar in the graphic intergrowths and in spindleperthites of L2 is more sodic (AbssOrggAn]) than thelamellae in the mesoperthites of GnD and LI

Biotite is mainly confined to the gneiss domains.Rare relic grains in the quartzofeldspathic matrix ofthe leucosomes and as armoured inclusions in garnethave lower Xyc ratios and almost no Al in six-foldcoordination, but higher Ti contents and X^A ratiosthan biotites of the gneiss domains (Table 3).Fluorine contents are uniformly high (A"F~0-27-

0-30).Garnets of the in situ leucosomes and the leuco-

granites are essentially almandine-pyrope solid solu-tions (Table 3). The compositional range is veryrestricted (Alm69-64, Pyr27-30. Grossi.9_3.3, Spess2-5-1.5) with slightly decreasing XFe ratios from LI to L2and a simultaneously increasing pyrope, grossularand spessartine content. The grains are weaklyzoned. Rim compositions show a slight increase inalmandine (LI), pyrope and spessartine contents(L2) at the expense of grossular (LI and L2).

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Table 2: Average microprobe analyses of feldspars from the gneiss domains (GnD), the in situ leucosomes (LI) and the

leucogranites (L2)

wt%

SiO2

AljO,

CaO

NajO

£

sr*+

Al3*

Ca I +

Na*

ir

Alkali feldspar

GnD

MesoperthHe

("=5)

62-58

20-89

2-95

5-88

6-97

98-46

2-858

1-126

0-146

0-510

0-364

End-members (mol%)

Ab

Or

An

50-6

35-1

14-3

L1

Mesoperthite

(" = 6)

62-90

21-10

2-74

5-86

6-42

99-18

2-850

1-128

0-130

0-516

0-370

50-5

36-5

130

L2

Spindle perthite

(n = 6)

64-70

19-84

105

4-66

10-08

100-36

2-921

1073

0051

0-408

0-580

39-2

55-9

4-8

Graphic

intergrowth

63-39

21 06

2-30

6-27

6-20

99-36

2-855

1-120

0-113

0-548

0-358

540

35-1

10-9

Plagioclase

GnD and L1

Lamellae in

mojoperthrts

and In graphic

intergrowths

(o = 32)

62-77

23-34

4-62

8-89

0-22

99-91

2-783

1-219

0-220

0-764

0013

76-7

1-2

220

L2

Lamellae in

•plndle perthhe

(n = 6)

64-27

23-17

3-95

9-66

0-18

101-30

2-802

1-191

0-185

0-817

0010

80-8

1 0

18-2

Potassic feldspar

GnD and L1

Lamellae in

mesoperthltas

and in graphic

intergrowths

C = 22)

64-36

18-67

0-16

1-73

14-59

99-61

2-970

1018

0005

0-144

0-865

14-2

860

0 8

L2

Matrix of

spindle perthite

(n = 6)

6607

19-38

0-33

3-83

11-75

101 -43

2-964

0-513

0-014

0-335

0-673

32-6

66-9

1-5

o

OrOO

o

<J1

Oo

n is the number of analyses taken for calculating the given average value. All calculations were carried out on the basis of five cations.

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BRAUN et al. DEHYDRATION-MELTING OF LEPTYNITIC GNEISSES

Table 3: Representative microprobe analyses ofbiotitefrom the gneiss domain and the

in situ leucosome and of garnet (core and rim) from the in situ leucosome LI and the

leucogranites L2

SiO2

TiOj

AljO3

FeO

MgO

NajO

K2O

F

Cl

OH

F=O

CI=O

I

Si4*

Ti4*

Aim

Fe2+

Mg2 +

Na*

F

Cl

OH

xN.xr

Biotite

GnD

36-96

6-41

15-18

14-19

12-61

001

9-89

2-30

0-16

2-86

-0-97

- 0 0 4

98-89

2-778

0-306

1-222

0-122

0-893

1-414

0009

0-948

0-546

0-021

1-433

0-39

000

0-27

L1

37-88

6-16

1505

10-36

17-75

0-32

9-74

262

0 16

2-86

- M O

-0-04

101-11

2-742

0-334

1-258

0026

0627

1-915

0-045

0-899

0-601

0020

1-379

0-25

0-05

0-30

wt%

SiO2

AljOj

FeO

MnO

MgO

CaO

Z

Si4*

AP+

Fe2+

Mn2 +

Mg2*

Ca2*

Garnet

Core

L1

37-85

21-16

31-96

0-67

7-16

1-06

99-85

2-970

1-955

2097

0-045

0-838

0-088

End-memberj (mol%)

Aim

Pyr

Gross

Spess

Xr,

68-4

27-3

2-7

1-5

0-71

L2

38-31

21-63

30-15

1-01

7-69

1-16

99-83

2-995

1-985

1-930

0065

0-895

0095

64-5

300

3-3

2-2

0-69

Rim

L1

37-86

21-10

32-34

0-69

7-12

0-88

99-97

2-968

1-950

2-120

0045

0-833

0075

69-1

27-1

2-2

1-5

0-72

L2

38-18

21-70

30-45

1-12

787

0-73

10004

2985

2000

1-920

0075

0-920

0060

64-6

30-8

2 0

2-5

0-68

METAMORPHIC CONDITIONSDURING LEUCOSOMEFORMATIONPrevious geothermobarometric data obtained forleptynitic gneisses, garnet-sillimanite-cordieritegneisses and charnockites in the KKB point at equi-libration conditions of the gneiss assemblage of

7~750°C, P = 5-6 kbar and aH,o~0-3 (Santosh,1986; Chacko et al., 1987; Ehl, 1989; Raith & Sri-kantappa, 1993). For in situ leucosomes, thermo-metry based on the oxygen isotope fractionationbetween garnet and quartz also indicates equi-libration temperatures of 750cC (Kohler et al., 1993).

In contrast to these findings, distinctively highertemperatures are indicated by the results of feldspar

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JOURNAL OF PETROLOGY VOLUME 37 NUMBER 6 DECEMBER 1996

thermometry using the Fuhrman & Lindsley (1988)model as modified by Kroll et al. (1993). For themesoperthites (GnD and LI), extreme temperaturesof equilibration are indicated by the high anorthitecontents of 12-14 mol % (Table 2). The bulk com-positions plot close to the 1000°C isotherm at 5 kbar(Fig. 3). This estimate seems to be unrealisticallyhigh, considering that at these temperatures biotite isno longer stable and the leptynitic gneiss should haveundergone extensive melting (Vielzeuf & Montel,1994; Patifio Douce & Beard, 1995). However, evenif the uncertainties in the position of the ternaryfeldspar solvus at temperatures above 900°C and themineral composition data are taken into account,temperatures of the order of at least 900°C have tobe expected. Such high peak-metamorphic tempera-tures are corroborated by the occurrence of coex-isting spinel + quartz in khondalites and ofwollastonite in calc-silicate rocks. Spindle perthites(L2) have lower anorthite contents (~5 mol %) andtheir bulk compositions indicate minimum tempera-tures of 900°C for the crystallization of the leuco-granitic melts (Fig. 3).

GEOCHEMISTRYThe garnet-biotite gneisses of the Kerala KhondaliteBelt (KKB) are subdivided into a sodic and apotassic group with K2O/Na2O (wt %) < 1 and > 1,respectively (Srikantappa et al., 1985; Chacko et al.,1992). The two groups also have contrasting petro-graphic features. Sodic gneisses are fine- to medium-grained rocks, commonly interbanded with khonda-litic garnet-biotite-sillimanite and garnet—biotite-sillimanite-cordierite gneisses, and possibly have asedimentary origin. The majority of the potassicgneisses, on the other hand, are rather coarse-grained rocks, often with a conspicuous augentexture, defined by deformed and recrystallized K-feldspar megacrysts, and probably representdeformed granites (Braun, 1994).

The investigated leptynitic gneisses at Manalibelong to the sodic group.

Major and trace elementsTable 4 gives major and trace element data and theoxygen isotopic composition for the gneiss domain

An

100

Fig. 3. Ternary feldspar diagram ihowing the location of the 800, 900 and 1000°C jolvi at 5 kbar and the compositions of mesoperthitesfrom gneiss domains (GnD) and in situ leucosomes (LI) of the leptynitic gneisses (crouci) as well as of ipindle perthites from the leuco-granites (diamonds). The lolvi were calculated with the computer program SOLVCALC (Nekvanl & Wen, 1993) using the activity

model of Fuhrman &. Lindiley (1988).

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Table 4: Major and trace element compositions of the investigatedrocks (for abbreviations see Table 1) as

well as qfbiotite and garnet mineral separates; additionally, the oxygen isotope composition (expressed as

51S0SMOW) and the K20/Na20 ratio are given

wt%

SiO2

T1O2

AfeO,FeO

MnO

MgO

CaO

Na20

K20

P20B

Z

p.p.m.

Zn

Ga

Rb

Sr

Y

Nb

Zr

Bo

Pb

La

Ce

Pr

Nd

Sm

Eu

Gd

Tb

Dy

Ho

Er

Tm

Yb

Lu

Th

U

KiO/NajO

& " S M O W

GnD#

72-45

0-33

15-76

0-74

b.d.

0-43

224

4-17

3-47

0-06

99-64

49

23

113

525

b.d.

3

137

644

27

27-30

47-60

4-30

14-40

1-89

0-68

0-78

—

0-11

—

007

—

008

002

20

b.d.

083

850

PGn"

73-33

0-30

16-36

1-76

0-02

0-64

212

3 9 4

3 12

0-07

100-66

50

23

93

471

7

4

136

555

23

26-90

46-10

4-67

16-60

2-50

0-63

1-81

—

1-11

—

0-65

—

0-48

0-07

9

b.d.

0-79

8-40

L T

71-66

0-28

15-28

4-27

008

088

1-96

3-37

2-79

0-06

100-53

61

19

72

441

18

3

140

497

27

26-90

46-10

4-78

1700

3-50

0-64

3-70

—

3-25

—

1-82

—

1-70

0-24

18

b J .

083

8-70

L2t

discordant

72-73

0-03

1502

1-33

0-04

0-26

122

3-10

5-45

0-11

99-28

18

25

184

33310

1

33

630

35

8-45

16-06

—

6-20

1-53

0-48

1-46

—

1-06

—

0-65

—

0-75

0-12

b.d

b.d.

1-76

9-17

L21

parallel

73-60

0-04

14-69

0-94

003

0-21

107

3-38

5-68

0-16

99-70

26

21

197

288

7

3

45

383

38

10-30

19-30

2-25

7-97

1-69

0-36

1-33

—

106

—

0-69

—

0-77

0-11

1

3

1-65

925

QFG

71-43

003

1704

b.d.

b.d.

b.d.

2-56

4-91

3-30

007

99-34

b.d.

25

75

586b.d.

b.d.

77

654

21

36-00

4300

b.d.

11-00

b.d.

—

—

—

—

—

—

—

—

—

b.d.

b.d.

0-67

b.d.

QFL

73-62

003

15-32

b.d.

b.d.

004

228

4-37

3-32

008

9906

b.d

24

74

543

3

3

83

639

19

24-00

42-00

b.d

11-00

b.d

—

—

—

—

—

—

—

—

—

b.d

b.d

0-76

b.d

Bkitite

(GnD)

38-31

568

15-78

15-96

0-03

11-34

0-20

0-28

932

004

96-94

844

42

850

41

12

50

272

1431

10

2600

91 00

b.d.

4300

7-00

—

—

—

—

—

—

—

—

—

55

b.d.

b.d.

b.d.

Garnet

(L1)

38-91

0-17

21-84

31-60

0-62

6-90

100

0 0 5

003

006

101-18

299

b.d.

b.d.

4

153

3

101

b j ±

8

b J .

3400

b.d.

1800

600

—

—

—

—

—

—

—

—

—

7

b.d.

bA.

b.d.

•REE ICP-AES analyses, performed at the University Blaise Pascal, Clermont-Ferrand.tREE ICP-AES analyses, performed at the University of Marburg.All other REE data were carried out by X-ray fluorescence at the University of Bonn,b.d., below detection limit

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(GnD), the in situ leucosome (LI) and two leuco-granite samples (L2). Additionally, the chemicalcomposition for a large leptynite slab (~ 30x20 cmin size) comprising gneiss domains and in situ leuco-somes was determined. As previously discussed, thefield relations and petrographic features indicate aclosed system behaviour of the leptynitic gneisses onthis scale and therefore the data for this slab (PGn)are regarded as representing the bulk chemistry ofthe precursor gneiss. The data are complemented bychemical analyses of the quartzofeldspathic matricesof the gneiss domain (QFG) and the in situ leucosomeLI (QFL) as well as of biotite and garnet mineralseparates.

The geochemical data of the precursor gneiss(PGn) closely match average values of the lowercontinental crust (Taylor & McLennan, 1985), andresemble those of quartzofeldspathic high-gradegneisses from the Central Granulite Belt of Sri Lankafor which a derivation from greywackes has beeninferred (Pohl & Emmermann, 1991; Prame & Pohl,1994). Compared with these, they are characterizedby distinctly lower concentrations of FeO, MgO,MnO, Y, Th and Zr, whereas A12O3, K2O and Srabundances are slightly higher.

A comparison of the major and trace element dataof the gneiss domain (GnD) and the in situ leucosome(LI) reveals significant differences (Table 4, Fig. 4).

%gain

LI

Sr Ba FeO MgO K2O Na-,O CaO

Fig. 4. Graphical illustration of the enrichment and depletion of•elected major and trace elementi in the gneui domain (GnD)(circlci) and the in situ leucosome LI (lozenges) relative to thecomposition of the precursor gneiu (PGn) for the leptyniticgneisses of Manali and for other leptynitic gneisses (shaded) of

theKKB.

The biotite-bearing gneiss domain is characterizedby higher concentrations of K2O, Na2O, Rb, Sr, Baand TiO2, whereas the garnet-bearing in situ leuco-some is enriched in FeO, MgO, MnO, Y and themedium and heavy rare earth elements [Figs 4 and6a (below); Table 4]. The quartzofeldspathicmatrices of both domains (QFG and QFL), inaccordance with their similar mode (Table 1), haveapproximately the same chemical composition(Table 4). This indicates that the observed elementfractionations in the first place were controlled bythe ferromagnesian phases, i.e. by selective transferand fixation of elements between the extendingleucosome domains, where garnet was growing, andthe shrinking gneiss domains, where the breakdownof biotite continued.

Compared with the in situ leucosomes, the leuco-granites (L2) have lower FeO, MgO and CaO con-tents, and significantly higher K2O contents (Table4). In the haplogranite system, the compositions ofthe leucogranites correspond to minimum meltsformed at low activities of water (aHio~0-3,Johannes & Holtz, 1990). Low TiO2, FeO and MgOcontents at high SiO2 and A12O3 values andK2O>Na2O are characteristic features of theserocks, which closely resemble leucogranites (France-Lanord & LeFort, 1988; Scaillet et al., 1990; Inger &Harris, 1993; Clarke et al., 1993; Watt & Harley,1993).

REE and isotope data

Rare earth elements

The chondrite-normalized REE spectrum of the lep-tynitic gneiss (PGn) shows low abundances, a mod-erate fractionation (La^/Lujy~ 30) and no Euanomaly (Table 4, Figs 5 and 6a). This is in obviouscontrast to the spectra for sodic and potassic garnetbiotite gneisses of the KKB, as all these rocks gen-erally show higher REE abundances and a markednegative Eu anomaly (Chacko et al., 1992; Raith &Srikantappa, 1993). However, the REE patterns ofother sodic leptynitic gneisses are similar to thatfrom Manali (unpublished data). This indicates thatthe garnet-biotite gneisses of the KKB are chemic-ally rather heterogeneous and that their protolithsprobably derived from different source regions.

LREE abundances are almost the same in the insitu leucosomes and the gneiss domains. In contrastto this, compared with the precursor gneiss (PGn),the spectra for GnD and LI, with the exception ofEu, show a complementary, moderate to strongfractionation of the medium and heavy rare earthelements (Fig. 6a). LI is markedly enriched in

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100.0-

(a) 100.0 -q

10 .0 -

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Fig. 5. Chondrite-normalized REE pattern of the investigatedsodic leptynitic gnein (PGn) compared with the range of ipectraof granitic augen gneisses (Raith & Srikantappa, 1993) and todicand potassic garnet-biotite gneisses (Chacko it al., 1992). Chon-

drite abundances are taken from Evenien it al. (1978).

MREE and HREE, whereas GnD is stronglydepleted in these elements. Eu is fixed at a constantvalue in both domains, as it is essentially con-centrated in alkali feldspar, the modal abundance ofwhich remained almost unchanged during leuco-some formation. As a consequence, LI and GnDdisplay a marked negative and positive Eu anomaly,respectively.

The leucogranitcs are characterized by low REEabundances and weakly fractionated REE patterns(Lajy/Lujy~7). An Eu anomaly is absent or slightlynegative. Compared with the in situ leucosome LIthe leucogranites have distinctly lower REE abund-ances (Fig. 6b). Compared with the leptynitic gneisscomposite (PGn) the LREE (La—Sm) are depletedby approximately one-third whereas the HREEabundances are almost the same.

Stable oxygen isotopes

The oxygen isotope composition of leptynitic gneissesin the KK.B is characterized by 5 O values in therange between 8 and 9-5%o (Table 4 and unpub-lished data). The 5 O value for the precursor gneiss(PGn) at Manali lies at 8-4%o. The very similar <518Ovalues for GnD and LI (Table 4) indicate that theleucosome formation was not accompanied by a sig-nificant isotopic fractionation between the twodomains. The leucogranites, on the other hand, areclearly enriched in 8O, and display 5lBO values of9-17%o, respectively.

1 0 . 0 -

•La Cc Pi Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

(b) 100.0 -

10.0 -

5a.

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Fig. 6. (a,b) Chondrite-normalized REE ipectra of the leptyniticgncio (PGn), iti in situ leucosome (LI) and gneiss domain (GnD),

and the leucogranites L2 at Manali. (See text for discussion.)

Rb—Sr isotopes

The sodic leptynitic gneisses of the KK.B are char-acterized by low "Rb/^Sr ratios (<l-0) and87Sr/86Sr ratios in the range of 0-72-0-73 (Kohler etal., 1993). At Manali, the in situ leucosomes LI aredepleted in Rb relative to the precursor gneiss(PGn), whereas the gneiss domains (GnD) show aslight enrichment (Table 5, Fig. 4). The Rb—Sr iso-chron defined by the two domains gives 535 Ma,which agrees well with U-Th-Pb ages of monaziteand zircon (Buhl, 1987; Braun, 1995) and Sm-Ndgarnet-whole-rock dates for garnet-biotite gneissesof the KKB (Kohler et al., 1993; Brandon & Meen,1995). Surprisingly, the data for the precursor gneiss(PGn) do not plot on the isochron. The deviation is

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Table 5: Rb and Sr abundances and

isotopic ratios of the leptynitic gneiss, its

gneiss and leucosome domains and the

leucogranite vein L2

Rb (p.p-m.)

Sr (p.p.m.)

"Rb /^ r

"Sr/^Sr

"Sr/^Sr^M.

GnD

113

626

0-574

0-72087

0-71637

PGn

93

471

0570

0-72208

0-71761

L1

72

441

0-443

0-71987

0-71640

197

288

1-990

0-75006

0-73446

M. IS the recalculated Sr isotope ratio of the samples atthe assumed time of leucosome formation.

attributed to incomplete removal of leucogranitematerial from the leptynitic gneiss during pre-paration of the LI—GnD composite sample.

The leucogranite compared with the leptyniticgneiss has higher 87Rb/*Sr and 87Sr/86Sr isotoperatios and also a higher recalculated Sr/86Sr ratioat 550 Ma, the assumed time of intrusion (Table 5).That melt emplacement closely followed migmati-zation is obvious from the ductile deformation of insitu leucosomes in the contact zone with foliation-concordant leucogranite sheets. The distinctly higherrecalculated 87Sr/B6Sr ratio at 550 Ma for L2 (Table5) indicates that the leucogranitic melts were notgenerated within the Manali leptynitic gneissensemble but originated at greater distance ingneisses with a significantly higher initial 87Sr/86Srratio. The few published Rb—Sr isotope data forleptynitic gneisses of the KKB, on a regional scale,show considerable heterogeneity (87Sr/86Sr550Mm =

0-71761—0-72813) and thus might well have been thesource for the leucogranitic melts.

DISCUSSIONFormation of in situ leucosomes LIIt is characteristic of migmatites that dehydration ordehydration-melting leads to the development oftwo spatially separated domains of distinct chemicaland modal composition and discernible textures, i.e.leucosome and restitic gneiss (melanosome). Thepetrographic and geochemical data alone often donot allow us to assess with certainty the presence andproportion of melt in the leucosome domain, andthus to discriminate between the two processes.

The mode of occurrence and compositional fea-tures of in situ leucosomes at Manali suggest thatthey represent the frozen-in initial stage of a de-

hydration-melting process which, at greater depth,through segregation and large-scale migration of themelt phase eventually gave rise to the leucogranites.If this interpretation holds true, understanding theformation of LI could provide important infor-mation about the generation of leucogranitic meltsat granulite facies conditions. In the following sec-tions we will briefly discuss specific chemical andtextural features of PGn, GnD and LI in relation totypical attributes of anatectic and subsolidus mig-matites, to elucidate the nature of LI and the relatedprocess of migmatization.

Microtextures and modes

Migmatization, whether caused by subsolidus ormelting processes, generally involves the preferredtransfer of felsic components into the leucosomedomains with simultaneous development of restiticgneiss domains enriched in mafic minerals. Leuco-somes of anatectic origin often attain the composi-tion of granitic minimum melts. Compared with theparent gneiss they show a marked increase in grainsize and isotropic granoblastic fabrics (McLellan,1983; Waters, 1988; Sawyer & Barnes, 1988; Stiiwe& Powell, 1989; Powell & Downes, 1990; Barbey etat., 1990).

The migmatites at Manali do not show thesecommon features. The quartzofeldspathic matrices ofin situ leucosomes and gneiss domains are remarkablysimilar in modal composition and texture. Theircompositions do not match those of graniticminimum melts. The leucosomes show higher modalabundances of mafic phases (garnet) than the gneissdomains (Table 1). These observations show that thedevelopment of leucosomes was essentially controlledby a selective transfer of femic components to thesites of garnet growth and did not involve noticeablemelt migration into these domains, although they donot preclude the presence of melt during leucosomeformation. Harte et al. (1991) explained the non-minimum composition of anatectic leucosomes inmigmatites of the Ballachulish contact aureole withmigration and redistribution of components withinthe melt during crystallization, leading to quartz- orfeldspar-dominated pools or pockets. Stiiwe &Powell (1989) and Powell & Downes (1990) con-sidered that the deviation in modal composition ofgarnet-bearing in situ leucosomes from graniticminimum melts is due to considerable meltextraction, which also prevented hydration of garnetduring freezing of the melt. The field setting atManali does not show evidence for extraction of meltfrom the in situ leucosomes and segregation or co-alescence into pools or pockets. The leptynitic

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gneisses at Manali and other Manali-type migma-tites throughout the Ponmudi Unit show identicalelement fractionation patterns between leucosomeand gneiss domains (Fig. 4), although the chemicalcomposition of in situ leucosomes shows remarkabledifferences and ranges from granitic to tonalitic.These differences are not easily explained by differ-ential extraction of melt, but instead strongly favoura mineralogical control of the dehydration process.

Mineral composition attributes

During partial anatcxis, plagioclase in the restiticgneiss domain compared with the leucosomebecomes enriched in anorthite component. If in theleptynitic gneisses of Manali migmatization wasmainly driven by partial anatexis, alkali feldspars inthe in situ leucosomes, compared with those in thegneiss domains, should have a less calcic and moresodic composition, probably similar to that of spindleperthites of the leucogranites. Instead, alkali feld-spars in both GnD and LI have identical composi-tions, which suggests that the leucosomes cannotrepresent pure melt domains (Johannes et al., 1995).On the other hand, similar feldspar compositions inGnD and LI could be established if the volume ofequilibration during and subsequent to migmat-ization exceeded that of gneiss and leucosomedomains (Powell & Downes, 1990). Considering theslow Al-Si diffusivity in feldspars, however, itappears unlikely that a distinct compositional con-trast between feldspars of the leucosome and thegneiss domain could have been eliminated. Themicrostructures also do not indicate a stage ofthorough annealing during which chemical equili-bration of the feldspars could have been achieved.

REE systematics

Complementary REE patterns between leucosomesand melanosomes are often recognized in amphi-bolite- and granulite-facies migmatites and theyhave been used to distinguish subsolidus from ana-tectic leucosomes (Barbey et al., 1989, 1990; Watt &Harley, 1993; Bea et al., 1994; Johannes et al., 1995).Commonly, the leucosomes are significantly depletedin REE (except Eu) whereas the melanosomes areenriched in these elements. Anatectic and subsolidusin situ leucosomes are regarded as having beenformed through segregation of felsic components,whereas mafic minerals (e.g. garnet, orthopyroxene,cordierite) and most of the accessory phases (mon-azite, zircon), the main REE hosts, remained in themelanosomc or restitic gneiss domain. This finds itsexpression in the strong depletion of LREE andHREE in the leucosome and the simultaneous

enrichment of these elements in the restite. Theleucosomes should always develop an Eu anomaly.In subsolidus leucosomes, where feldspar componentspreferentially fractionated from the former gneissinto the leucosome, the Eu anomaly is positive(Sawyer & Barnes, 1988; Barbey et al., 1990). Inanatectic leucosomes the character of the Euanomaly depends on the behaviour of alkali feldsparduring melting and can be either positive or negative[see discussion by Carrington & Watt (1995)]. TheREE distribution observed in the leptynitic gneissesof Manali (Fig. 6a, Table 4) and other KKB local-ities (unpublished data) is distinct from those oftypical migmatites. The complementary patterns forSm and HREE of LI and GnD are obviously con-trolled by the preferential transfer of Sm and theHREE from the gneiss domain, the site of biotitebreakdown, to the leucosome, where the growinggarnet acted as a sink for these elements. Eu is con-trolled by alkali feldspar and fixed at an almostconstant value. As Eu should fractionate duringmigmatization (Johannes et al., 1995) the constantEu value for GnD and LI indicates that the bulk ofthe feldspars did not participate in the meltingreaction and consequently that the melting degreemust have been very low.

Extremely low LREE abundances in leucograniticmelts are attributed to the observation that monazitefails to equilibrate with water-undersaturatedgranitic melts, either because melt segregation ratesexceeded monazite dissolution rates or becausemonazite was shielded during melt generation andsegregation, e.g. in biotite (Watt & Harley, 1993;Nabelek & Glascock, 1995). Therefore, if the in situleucosomes at Manali were melt pools, LREE frac-tionation between them and the gneiss domainsshould be recognized with strong depletion of LREEin the leucosomes. Contrary to this, the LREEabundances in the in situ leucosomes are similar tothose of the gneiss domains and are even higher thanthe saturation level at temperatures of 900-1000°Cand water contents of 1-2 wt% (Montel, 1993).This, and the uniform Th abundances in both thegneiss and the leucosome domains, suggests thatmonazite as the main LREE carrier largely was inertduring migmatization, which makes it unlikely thatthe leucosomes were derived through segregation ofin situ partial melts. On the other hand, monazitegrains occurring in garnet and in the quartzofelds-pathic matrix of GnD and LI show complex Th—Pbzoning patterns, which clearly document diffusionalexchange, recrystallization and growth during Pan-African high-grade metamorphism (Braun, 1995),and thus might have interacted with a melt phase.

In conclusion, at the given P—T conditions

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(~900°C, ~6 kbar), the formation of Manali-typein situ leucosomes must have occurred through fluid-absent biotite melting at a very low degree ofmelting (~5 vol.%). The textural and geochemicalfeatures observed in the leptynitic gneiss in ouropinion are best explained with the model thatPowell & Downes (1990) and Stiiwc & Powell(1989) proposed for the generation of similar leuco-somes in metapelitic high-grade rocks. Accordingly,the leucosome domains developed through thenucleation of garnet at discrete places. The meltformed an intergranular film which enhanced theelement transfer between the expanding leucosomedomains, where garnet was growing, and theshrinking gneiss domains, where biotite was breakingdown. Diffusion must have been energeticallyfavourable compared with nucleation of new garnetgrains, and potential gradients mainly for Fe, Mgand the HREE between the leucosome and the gneissdomain were established, leading to the observedfractionation (Figs 4 and 6a). At Manali, these pro-cesses took place in static conditions and, in contrastto the migmatites described by Powell & Downes(1990) and Stiiwc & Powell (1989), presumablywere not accompanied by extraction of melt. Theensemble of leucosome domains and gneiss networktherefore can be considered as a closed system.

Dehydration-melting reactions

Despite the lack of any textural evidence, a processinvolving biotite melting is also strongly corrobo-rated by the dehydration—melting experiments onpsammo-pelitic rocks at variable water activity(LeBreton & Thompson, 1988; Vielzeuf & Hol-loway, 1988; Johannes & Holtz, 1990; Vielzeuf &Montel, 1994). These studies indicate that at thepeak-metamorphic conditions inferred for the lepty-nitic gneisses (~900°C, 5-7 kbar), even at lowactivity of water (<JH,O~0'3) melting must haveoccurred. Recent experimental work by Vielzeuf &Montel (1994) on fluid-absent melting of meta-greywackes has shown that at low activities of waterand within a narrow P-T range (795-820°C and4 kbar; 810-860°C and 10 kbar) garnet-bearingmelts are formed according to the incongruentdehydration-melting reaction

(1)

Although the starting material [greywacke with 40wt% quartz, 32 wt % plagioclase (An^), 25 wt%biotite] used in the experiments does not match themodal composition of the inferred precursor gneiss atManali, the results can be adopted to describe theformation of the in situ leucosomes (LI) in these

Bt + PI + Qtz ^ Grt (+Kfs) + L.

rocks. Additionally, the experimental results ofCarrington & Watt (1995) have shown that theconsumption or production of alkali feldspar duringdehydration—melting primarily depends on themolar H2O/K2O ratio of the melt relative to that ofbiotite. If this ratio is higher in the melt then K-feldspar will be produced; otherwise, it will reactwith biotite during incongruent melting. As we donot know the water content of L2 and of biotitebefore dehydration it is difficult to decide if alkalifeldspar was consumed or produced during leuco-granite formation. A plot of the compositions of L2and of biotite from the gneiss domains into theHKM diagram of Carrington & Watt (1995) showsthat the maximum water content of the melt atwhich biotite and alkali feldspar would break downsimultaneously is ~l-8 wt%, a characteristic valuefor melts generated at ~900°C and ~6 kbar (Car-rington & Watt, 1995, fig. 4). The fact that nohydrous mineral was generated during crystal-lization of L2 suggests that the amount of water inthe melt probably was even lower than 1 -8 wt %. Wetherefore infer that alkali feldspar in the presence ofquartz and biotite was consumed during incongruentdehydration—melting, according to the reaction

Bt + Akf + Qtz ^ Grt + Ilm + L. (2)

In addition to the anorthite component of the alkalifeldspar, the Tschermak component of biotite pro-vided an important aluminium source for the growthof garnet. Reaction (2) led to the completebreakdown of biotite in the leucosome domain.

Dehydration—melting started at discrete sites inthe gneiss and gave rise to nucleation and growth ofgarnet in the centre of expanding leucosome domainsand of ilmenite in their quartzofeldspathic matrix.

The observed contrast in the modal and chemicalcompositions of leucosome and gneiss domains showsthat considerable element exchange has occurredbetween the two domains and thus provides strongevidence for a simultaneous participation of thegneiss domains in the dehydration-melting process.It is suggested that the two domains communicatedvia an intergranular melt phase, however, with sig-nificant melt segregation into the leucosome domain.The development of leucosomes ceased when thealuminium sources within the shrinking gneissdomain became exhausted, probably with the con-sumption of the eastonite component in biotite.During the progress of reaction (2) the reactingbiotite became enriched in Mg and F and therebywas stabilized to higher temperatures, which alsomight have prevented further dehydration-melting(Dooley & Patino Douce, 1996).

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Mechanisms of leucogranite formation andmelt segregationContrary to the in situ leucosomes (LI), the mag-matic nature of the leucogranites (L2) is evidentfrom the field relations as well as the petrographicand geochemical data. They occur as distinct dykesand veins emplaced subparallel and perpendicular tothe foliation of the leptynitic gneisses, clearly post-dating the formation of the in situ leucosomes. Theirchemical composition closely matches that of leuco-granites. This, together with the absence of relictphases of the host gneisses, suggests that theyrepresent crystallized melts.

Considering the conformity in chemical and/ormodal composition as well as in mineral chemistrybetween in situ leucosomes and intrusive melts it istentative to assume a genetic relationship betweenthem (Sawyer & Barnes, 1988; Barbey et al., 1989;Bea et al., 1994). However, it is evident from the Rb—Sr isotope data that the leucogranites did not formwithin the leptynitic gneisses of Manali (Table 5).They represent intruded leucogranitic melts whichwere externally derived by partial anatexis ofgneisses with significantly higher B7Sr/ Sr ratios.Leptynitic gneisses in the KKB show considerableisotopic heterogeneity and therefore this finding doesnot exclude generation of the leucogranitic meltsfrom gneisses similar in modal and chemical com-position to those of Manali and through a dehy-dration-melting process as described by reaction (2).This suggestion is supported by the following obser-vations:

(1) The absence of sillimanite, cordierite or her-cynitic spinel as relict phases does not favour khon-dalites as possible sources for the melts, despite theirclose spatial relationship with the leptynitic gneisses.

(2) The <518O values are similar for the leptyniticgneiss (8-40%o) and the leucogranites (9-17-9-25%o).Although there are no whole-rock oxygen isotopedata available for khondalites of the KKB, com-parable metapelitic rocks of the Highland Complexof Sri Lanka have distinctly higher SlBO values(~10-12%o; Fiorentini et al., 1990; Prame & Pohl,1993). During partial anatexis the melt becomesenriched in ' O compared with the parent rock,owing to the increased modal abundance of mineralphases with high 18O values (quartz, feldspar). Thus,melts that were derived through partial anatexis ofmetapelites should display 518O values of at least 10-ll%o, which were significantly higher than those ofthe leucogranites.

(3) The chondrite-normalized REE spectra ofleucogranites and lepynitic gneisses show com-parable low abundances. LREE in the leucogranites

(La.y/Sm^-~3-5) are less fractionated than in thegneiss (Lajv/Sm_y~6), whereas HREE abundancesare similar in both rocks (Gdjv/Lujy~l-5 and 2 8 ,respectively).

Although there is no definite proof for a derivationof the leucogranites through partial melting ofManali-type gneisses, the preceding interpretation ofthe dehydration—melting phenomena provides aviable scenario for the generation of garnet-bearingperaluminous leucogranites through dehydration-melting of metapsammitic rocks at low degrees ofmelting. This process leaves behind a granuliticresidue of garnet, quartz, feldspar and ilmenite, withzircon, apatite and monazite as accessory phases. Infact, completely dehydrated lepynitic gneisses withgarnet occurring in clusters or streaky alignment arefound throughout the KKB and resemble suchgranulitic residues. They presumably represent thefinal stage of dehydration—melting of Manali-typegneisses and might have experienced melt extraction.

A comparison of the KKB leucogranitic meltsformed through fluid-absent melting of psammo-pelitic lithologies in granulite terrains reveals con-trasting REE characteristics. Granulite facies meltsare characterized by REE abundances which aresignificantly lower than the saturation levels formonazite and zircon. The weakly fractionatedspectra often display a well-developed positive Euanomaly (Barbey et al., 1989, 1990; Watt & Harley,1993; Carrington & Watt, 1995). These features areregarded as being mainly due to incomplete equili-bration of the melt with monazite and otheraccessory phases as well as to the consumption ofalkali feldspar during melting. Both processes char-acterize water-undersaturated conditions duringpartial anatexis and become more important withdecreasing <ZH,O

In the case of Manali leucogranites, an Euanomaly is either absent or weakly negative (Fig.6b). Although the water content of these meltscannot be constrained precisely, general considera-tions concerning the behaviour of monazite andfeldspar during melting at low a ^ o c a n help toexplain the REE patterns of L2. If H2O contents inL2 were similar to those of granulite facies melts(1-5-2-5 wt%) or even less, reaction (2) would havebeen close to degeneracy (Carrington & Watt,1995). In this case, the contribution of alkali feldsparto the melt would be small and as a consequence theREE spectra would develop only a weakly positiveEu anomaly and essentially reflect the behaviour ofthe accessory phases.

The LREE abundances of L2, according to themodel of Montel (1993), are close to the saturation

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level for monazite at a temperature of 900°C. Mon-azite grains in the leptynitic gneisses predominantlyoccur within the quartzofddspathic matrix and onlyrarely are included in biotite, and therefore wereaccessible to equilibration with the melt (e.g.Nabelek & Glascock, 1995). Interaction of the mon-azite grains with a melt phase is clearly documentedby broad Pan-African overgrowths on Early Proter-ozoic (~2-0 Ga) cores (Braun, unpublished data),which suggest that the melt might have attainednear-equilibrium saturation. We therefore concludethat monazite and alkali feldspar, the former with anegative and the latter with a positive Eu anomaly,were consumed during melting in such proportionsthat an Eu anomaly did not develop. The amount ofmonazite necessary to match the measured LREEabundances in L2 is ~0-005%, a typical value forLREE-poor felsic melts (Miller & Mittlefehldt,1982).

Chemical equilibration between the melt and therestitic gneiss is strongly influenced by the meltdynamics. Although partial anatexis in a dynamicenvironment is common in high-grade metamorphicterrains (Brown et al., 1995), the field relations atManali rather indicate that static conditions pre-vailed during migmatization. From experimentalwork it is evident that even at very low degrees ofmelting wetting angles between the melt, quartz andfeldspar are low enough to allow the melt to form aninterconnected network (Jurewicz & Watson, 1985;Laporte, 1994; Laporte & Watson, 1995). Therefore,melt segregation may occur already at the initialstages of partial anatexis. The rate of melt segre-gation largely depends on the prevailing stressregime and the physical properties of the melt, inparticular on its viscosity. In the static conditionsassumed to have prevailed during partial anatexis inthe KKB, the positive volume change accompanyingfluid-absent dehydration—melting alone could triggersegregation of melt even at low degrees of melting(Clemens & Mawer, 1990; Brown et al., 1995). Thegenerally high viscosity of water-undersaturatedgranitic melts, however, presumably inhibited segre-gation of the small melt volumes generated withinthe leptynitic gneisses. It is thus very likely that themigration rate was sufficiently low for chemicalequilibration between melt and restitic gneiss.

In this context, the behaviour of fluorine duringincongruent melting of biotite is an important aspectbecause of its strong influence on the solubility ofaccessory minerals in granitic melts. Experimentalwork by Keppler (1993, and references therein)shows that high fluorine contents in granitic meltsincrease their ability to dissolve accessory phasessuch as zircon, apatite or monazite. Accordingly, the

trace element characteristic of leucogranites in theKKB would indicate low fluorine activities. Aninteresting addition to this set of problems is the dis-covery of leucogranite and pegmatite veins withextreme contents of fluorapatite, zircon and mon-azite during recent field-work (Braun, 1994, 1995).They cut across the leptynitic gneiss ensemble andobviously were formed rather late in the meta-morphic history. It is suggested that these melts weregenerated through complete melting of residual bio-tites that were strongly enriched in fluorine duringthe preceding dehydration-melting processes.

ACKNOWLEDGEMENTSThis work forms part of the first author's Ph.D.thesis and was completed during a research stay atthe Department de Geologie, Universite BlaisePascal, Clermont-Ferrand (France), funded by theFrench Government ('Bourse de gouvernementfrangais') and the Deutscher Akademischer Aus-tauschdienst (DAAD). C. Nicollet is thanked forhelpful discussions on dehydration-melting pheno-mena, as well as on the relationship between theleptynitic gneisses of the KKB and similar rocks insouthern Madagascar with regard to theirGondwana position. D. Vielzeuf introduced I.B. tothe secret world of experimental petrology. Discus-sions on the results of fluid-absent dehydration-melting experiments and their application to naturalrocks helped to clarify our view concerning theprocess of leucosome and leucogranite formation atManali. D. Laporte read an earlier version of thepaper and provided helpful comments, particularlyon the wetting behaviour of granitic melts and theirability to segregate at low degrees of melting. We aregrateful to W. Grimmeisen and S. Jung (Marburg)and F. Cantagrel and C. Pin (Clermont-Ferrand) fortheir assistance in obtaining REE and Rb—Sr isotopedata. Numerous discussions with C. Pin and H.Martin on these data improved our understanding ofdehydration-melting processes and are very muchappreciated. We thank S. Hoernes for analyticalsupport (X-ray fluorescence, 18O isotopes) and dis-cussions on the results of oxygen isotope chemistry.H. Kohler (Miinchen) kindly provided unpublishedRb—Sr isotope data from garnet-biotite gneisses ofthe KKB. The careful review of Ian Fitzsimons andthe helpful comments of Simon Harley and ananonymous reviewer greatly improved the manu-script and are much appreciated. Financial supportof the field and analytical work by the DeutscheForschungsgemeinschaft is gratefully acknowledged.

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RECEIVED AUGUST 4, 1995REVISED TYPESCRIPT ACCEPTED MAY 21, 1996

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