GeolCarp_Vol68_No5_445

GEOLOGICA CARPATHICA

, OCTOBER 2017, 68, 5, 445–463

doi: 10.1515/geoca-2017-0029

www.geologicacarpathica.com

Geochemical characteristics and conditions of formation

of the Chah-Bazargan peraluminous granitic patches,

ShahrBabak, Iran

ABDOLNASER FAZLNIA

Department of Geology, Urmia University, 57153-165 Urmia, Islamic Republic of Iran; a.fazlnia@urmia.ac.ir, nfazlnia@yahoo.com

(Manuscript received November 27, 2016; accepted in revised form June 9, 2017)

Abstract: Xenoliths of garnet–biotite–kyanite schist from the Qori metamorphic complex (southern part of the

Sanandaj–Sirjan zone, northeast Neyriz, Zagros orogen in Iran) in the 173.0±1.6 Ma Chah-Bazargan leuco-quartz diorite

intrusion were studied. This intrusion caused these schist xenoliths to be metamorphosed to the pyroxene hornfels facies

(approximately 4.5±1.0 kbar and 760±35 °C), converting them to diatexite migmatite as a result of partial melting of the

xenoliths. These melts are granites in composition. Melt volumes of 20 to 30 vol. % were calculated for small patches of

the peraluminous granites. It is possible that anatectic melting affected only the leucosome, such that melting was more

than 20 to 30 vol. %. It is possible that a large amount of melt was not extracted due to balanced in situ crystallization,

the adhesion force between melt and crystal (restite), and high viscosity of the leucosome. The Chah-Bazargan

peraluminous granites are depleted in trace elements such as REEs, HFSE (Ti, Zr, Ta, Nb, Th, U, Hf, Y), Ba, Pb, and Sr.

These elements are largely insensitive to source enrichment, but sensitive to the amounts of main and accessory minerals.

These elements were hosted by minerals such as garnet, biotite, muscovite, K-feldspar, plagioclase, ilmenite, apatite,

monazite, and zircon in the source (diatexitic migmatitic xenoliths).

Keywords: geochemistry, partial melting of xenoliths, peraluminous granitic patches, Jurassic.

Introduction

Migmatites provide examples of nascent granites, but detailed

studies often reveal that their leucosomes are the locations of

melt depletion rather than crystallization, or at best status,

crystal-melt mixes (e.g., Mehnert 1968; Ashworth 1985;

Sawyer2008a, b).Insomeinstances,segregatedandhomoge-

neous granites within migmatitic terrains of the mid-crust can

be related to specific sedimentary sources and melting reac-

tions as exemplified by Himalayan leucogranites, (Harris et al.

1995) because the melts have not migrated far from their

sources. However, some recent studies (Carvalho et al. 2016)

have shown that leucosome can also be connected to the gra-

nite melt far from their sources.

The processes of melt formation and extraction and crustal

source composition strongly influence the chemistry of

granitic melts. The melts have very low levels of trace ele-

ments such as Rb, Zr, Th, U, and Y where melt-residue separa-

tion is very efficient, as in leucosomes of stromatic migmatites

(metatexites), (Bea 1996a; Sawyer 1996; Sheppard et al.

2003). The depleted nature of the melts is typically ascribed to

disequilibrium melting where the rate of melt extraction

exceeds the rate at which accessory phases dissolve (Sawyer

1991), or to shielding of accessory phases by inclusion in

mafic minerals during melt formation and extraction (Bea

1996b). Metatexite is a migmatite heterogeneous at the out-

crop scale and coherent pre-partial melting structures are

widely preserved in the paleosome (where the microstructure

appears unchanged) and possibly in the melanosome (resi-

duum) part of the neosome where the fraction of melt was low

(Makrygina 1977; Bucher & Grapes 2011).

Diatexite is a migmatite in which neosome is dominant and

melt was pervasively distributed throughout. Pre-partial-

melting structures are absent from the neosome and commonly

replaced by syn-anatectic flow structures (e.g., magmatic or

submagmatic foliations, schlieren), or isotropic neosome.

Neosomes are diverse, reflecting a large range in the fraction

of melt, and they can range from predominantly leucocratic to

predominantly mesocratic (e.g., unsegregated melt and resi-

duum) to predominantly melanocratic. Palaeosome occurs as

rafts and schollen, but may be absent (Sawyer 2008b).

Diatexite migmatites represent high degrees of partial melting,

typically in the highest grade parts of migmatite terrains

(Mehnert 1968; Sawyer 2008b), and contain large and variable

proportions of restite. Diatexites are more homogenous than

metatexites, because there is considerable movement of the

melt fraction from one place to another within the diatexite

migmatites (Sawyer 2008b).

Terms appropriate to metatexite migmatites are patch, dila-

tion, net, and stromatic structures. These structures are formed

at the very onset of partial melting of the source. At the onset

of partial melting, the fraction of melt in a migmatite is very

small of course and this precludes the development of

an eye-catching morphology. Nevertheless, it is very impor-

tant to identify these migmatites because their appearance

defines the lower-grade limit to migmatite terrains. Partial

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melting in a rock typically starts at a few dispersed sites where

the conditions are optimal for the melt-producing reaction to

proceed(Raymond2007;Sawyer2008a, b).

Terms appropriate to diatexite migmatites are nebulitic,

schollen, and schlieren structures. As the fraction of melt and

neosome creation increase in a metatexite migmatite, the

pre-anatectic structures in the migmatite are progressively

destroyed. However, new micro- and macrostructures are pro-

duced during anatexis and become evident in the neosome.

The precise morphology that develops depends on whether

deformation occurred or the original distribution of fertile

rocktypes(Raymond2007;Sawyer2008a, b).

This study presents field, petrographic and geochemical

data and uses them to reconstruct the partial melting history of

migmatitic metapelitic xenoliths from Chah-Bazargan batho-

lith, in the southern part of the Sanandaj–Sirjan zone, north-

east Neyriz, Zagros orogen in Iran. This study demonstrates

the relationships among the migmatites, leucogranites, and

pegmatites, and shows that these rocks formed in the middle

crust as a consequence of advective heating by quartz dioritic

magma.

Geological setting

Southern Iran can be divided into a set of three parallel

NW–SE trending tectonic zones including: the Zagros Fold-

Thrust Belt, the Sanandaj–Sirjan Zone, and the Tertiary–

Quaternary Urumieh–Dokhtar magmatic arc (Alavi 1994;

Mouthereau et al. 2012; Mohajjel & Fergusson 2014; Hassan-

zadeh & Wernicke 2016), (Fig. 1). The Zagros is the largest

mountain belt and the most active collisional orogen associ a-

ted with Arabia/Eurasia convergence. It belongs to the Alpine–

Himalayan orogenic system that resulted from closure of the

Neotethys Ocean during the Cenozoic (Alavi 1994; McQuarrie

et al. 2003; Mouthereau et al. 2012; Hassanzadeh & Wernicke

2016). The tectonic history of these zones as part of the

Tethyan region has been summarized by many authors (e.g.,

Berberian & King 1981; Alavi 1994; Omrani et al. 2008;

Khadivi et al. 2012; Mouthereau et al. 2012; Fazlnia et al.

2013; Mohajjel & Fergusson 2014; Shafaii Moghadam et al.

2014; Hassanzadeh & Wernicke 2016). The Sanandaj–Sirjan

zone juxtaposed various metamorphic and magmatic rocks

that mostly formed in the Mesozoic era. It is believed that

the zone mostly consists of arc-related calc-alkaline granitoid,

gabbro and some volcanic rocks along with amphibolite

and kyanite-garnet schist formed during the subduction of

Neotethys beneath the Iranian plate (Berberian & King 1981;

Alavi 1994; Mouthereau et al. 2012). During the Palaeozoic

period, the Sanandaj–Sirjan zone was a part of northeast

Gondwanaland separated from the Eurasian plate by the Palaeo-

Tethys Ocean (Golonka 2004; Mouthereau et al. 2012; Fazlnia

& Alizade 2013). A north-dipping subduction system develo-

ped along the Palaeotethys margin (Golonka 2004). This sub-

duction system played a significant role in driving the Late

Palaeozoic and Early Mesozoic movement of plates in this area.

From early Permian to early Triassic times, the Sanandaj–

Sirjan zone had been situated along the southern margin of the

Eurasian plate and separated from northern Gondwanaland by

the Neotethyan Ocean (Mouthereau et al. 2012). During Late

Triassic–Early Jurassic times, several microplates were

sutured to the Eurasian margin, closing the Palaeotethys Ocean

(Golonka 2004). A north-dipping Neotethys subduction zone

beneath the Sanandaj–Sirjan plate was started approximately

in the Bajocian (Middle Jurassic; Golonka 2004; Yousefirad

2011; Fazlnia et al. 2013; Sheikholeslami 2015; Hassanzadeh

& Wernicke 2016). The formation and evolution of the

Neotethys started from Late Palaeozoic times (Hassanzadeh &

Wernicke 2016). Therefore, the tectonic regime between the

Arabian margin and Sanandaj–Sirjan plate altered from

passive to convergent (Ricou 1994). During the Mesozoic,

the oceanic crust of the Neotethys was subducted beneath

the Eurasian plate (Golonka 2004; Molinaro et al. 2005; Agard

et al. 2011; Yousefirad 2011; Mouthereau et al. 2012; Karimi

et al. 2012; Fazlnia et al. 2013; Mohajjel & Fergusson 2014;

Sheikholeslami 2015), and the Sanandaj–Sirjan zone occupied

the position of a magmatic arc (Berberian & Berberian 1981;

Agard et al. 2005; Agard et al. 2011; Karimi et al. 2012;

Mouthereau et al. 2012; Fazlnia et al. 2013; Chiu et al. 2013;

Mohajjel & Fergusson 2014; Akbari et al. 2016; Hassanzadeh

& Wernicke 2016). Subduction and arc magmatism began in

latest Triassic/Early Jurassic time, culminating at ~170 Ma

(Hassanzadeh & Wernicke 2016). The final closure of the

Neotethys and the collision of the Arabian and Eurasian plates

took place during the Tertiary period (Berberian & Berberian

1981; Alavi 1994; Golonka 2004; Molinaro et al. 2005;

Omrani et al. 2008; Agard et al. 2011; Mouthereau 2011;

Yousefirad 2011; Khadivi et al. 2012; Mouthereau et al. 2012;

Mohajjel & Fergusson 2014; Sheikholeslami 2015). Based on

Hassanzadeh & Wernicke (2016) the collision took place

during the mid-Tertiary. During the same period, the Zagros

Fold-Thrust Belt formed as part of the Alpine–Himalayan

mountain chain, extending about 2000 km from eastern Turkey

to the Oman line in southern Iran (Berberian & King 1981;

Alavi 1994; Agard et al. 2005; Omrani et al. 2008; Agard et al.

2011; Mouthereau 2011; Mouthereau et al. 2012; Mohajjel &

Fergusson 2014; Sheikholeslami 2015). The Chah-Bazargan

intrusion is located in northeast Neyriz which is a part of the

south Sanandaj–Sirjan zone.

There are several outcrops of intrusion-bordering migmatites

in the middle part of the Sanandaj–Sirjan zone. The migma-

tites occurred around the Alvand aureole near Hamadan

(Fig. 1), western Iran (Saki et al. 2012). They suggested that

regional metamorphism, granitic magmatism (Alvand pluton),

and contact metamorphism reflect arc construction and colli-

sion during subduction of a Neotethyan seaway and subsequent

Late Cretaceous–early Tertiary oblique collision of Afro-Arabia

(Gondwana) with the Iranian microcontinent. The Chah-

Bazargan intrusion and migmatitic xenoliths within the intru-

sion are like those in the Alvand aureole near Hamadan (Fig. 1).

Rocks of the Chah-Bazargan intrusion are composed of

quartz-diorite (Table S1) along with small patches of gabbroic

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intrusions (Fazlnia et al. 2013), migmatitic xenoliths (several

centimetres to several tens of metres in size), tourmaline-

bearing pegmatites and peraluminous garnet- and cordie rite-

bearing granites (metre to several tens of metres in size;

Fazlnia et al. 2007; Fig. 1; Table S1). The initial Chah-

Bazargan intrusion is mostly composed of plagioclase

(90–95 vol. %) and quartz (5–10 vol. %), as granular and cumu-

lative textures, along with accessory minerals (1–2 vol. %)

such as clinopyroxene and titanite. This intrusion crystallized

at 173.0±1.6 Ma (Fazlnia et al. 2007) into medium to high

grade parts of the arc-related Qori Barrovian-type metamor-

phic complex (QMC; Fazlnia et al. 2013; Sheikholeslami

2015), which primarily consists of meta-basites (actinolite

schist to garnet amphibolite) and meta-pelitic (biotite to

garnet–kyanite–biotite schist), interspersed with meta-psam-

mitic, meta-ultramafic (olivine–orthopyroxene–spinel–horn-

blende schist), and marbles layers (Table S1). The Talle-

Pahlevani gabbroic intrusions (Fig. 1) infiltrated into the

Qori metamorphic complex as a result of Neotethys sub-

duction beneath central Iran 170.5±1.9 Ma (Fazlnia et al.

2009; Sheikholeslami 2015). Therefore, there is a possibility

that the Chah-Bazargan quartz-dioritic and Talle-Pahlevani

gabbroic intrusions (Table S1) were formed of the same

magma. This is highlighted by the very similar spider diagram

patterns (Fazlnia et al. 2009, 2013) of the intrusive rocks.

Consequently, it is probable that the Chah-Bazargan quartz-

diorites are most likely cumulates of a basaltic to andesitic

magma and the Talle-Pahlevani gabbroic intrusions were

Fig. 1. Simplified geological map of north-eastern Neyriz (modified after Sabzehei et al. 1992). More information about sample locations are

present in Table S2.

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formed at the base of the Chah-Bazargan quartz-dioritic

intrusions.

The Barrovian-type metamorphic event in the QMC

occurred ca. 187.0±2.6 Ma (Fazlnia et al. 2007, 2009; Sheik-

holeslami 2015). Regional metamorphic mineral assemblages

inmeta-pelitesmainlyconsistofKy + St + Grt + Bt + Ms + Pl + Qtz

and Ky + Grt + Bt + Pl + Qtz ± Ms. Some outcrops of sedimen-

tary and low grade metasedimentary rocks can be found

among the high grade metamorphic rocks due to late stage

shearing of the Zagros fold belt (Berberian & King 1981;

Sabzehei et al. 1992; Saki et al. 2012; Sheikholeslami 2015).

All rock types are sheared strongly and thrust as imbricate

slices over the Neyriz ophiolite (Berberian & King 1981;

Sabzehei et al. 1992; Alavi 1994; Babaei et al. 2001; Mohajjel

et al. 2003; Sheikholeslami et al. 2008; Fazlnia et al. 2009;

Sarkarinejad et al. 2009; Sheikholeslami 2015). The peak

pressure and temperature for the Qori metamorphic complex

(Fig.1)havebeenestimatedtobe9.2±1.2kbarand705±40˚C

resulting from crustal thickening during the Early Cimmerian

orogeny between 187 and 180 Ma (Fazlnia et al. 2007, 2009).

This event occurred as a result of the beginning of Neotethys

subduction beneath central Iran (Fazlnia et al. 2013;

Sheikholeslami 2015). The studied rock types are related to

this event.

The host rock (medium to high grade parts of the QMC) was

disrupted as the primary magma (Chah-Bazargan gabbroic

intrusions) was injected. Xenoliths of the host rock underwent

high temperature contact metamorphism. Some meta-pelitic

xenoliths were completely assimilated by magma and con-

verted the mineral assemblage of the surrounding Chah-

Bazargan quartz-diorite to biotite granodiorite-tonalite

intru sion (Fazlnia et al. 2007). Small peraluminous patches of

two-mica granite and tourmaline-bearing pegmatites occur in

association with aggregations of meta-pelitic xenoliths within

the intrusion (Fazlnia et al. 2007). Previous studies (Sabzehei

et al. 1992; Jamshidi 2003) did not report any migmatitic

xenoliths and peraluminous two-mica granite in the intrusion.

Sheikholeslami et al. (2003) concluded that the Chah-Bazargan

intrusion was emplaced at ca. 160±10 Ma on the basis of biotite

K–Ar ages. Fazlnia et al. (2007) demonstrate that the crystal-

lization of the primary quartz-dioritic magma and peralumi-

nous granite occurred 173.0±1.6 Ma and 164.3±8.1 Ma,

respectively, and melting recorded by the migmatitic xenoliths

167±3.1 Ma considering the zircon SHRIMP U–Pb ages.

Additionally, the western edge of the QMC underwent

another Barrovian-type metamorphism at 147.4±0.76 Ma as

a result of crustal thickening during the initiation of the

Neotethyan mid-ocean ridge subduction beneath central Iran.

The metamorphic circumstance generated garnet amphibolites

occurred at pressures and temperatures between 7.5 and 9.5

kbar (at depth of 28 to 36 km) and 680 and 720 °C, respec-

tively,basedontheGrt – HblandHbl – Plthermometersand

Grt – Hbl – Pl – Qtz barometer (Fazlnia et al. 2009; also see

Sheikholeslami 2015). There is no evidence for the occurrence

of this metamorphism in the eastern part of the study area

(e.g., Chah-Bazargan, Chah-Dozdan, and Chah-Sabz).

Field and petrographic observations

Quartz diorites are leucocratic and contain xenoliths of

meta-pelitic migmatite. These xenoliths are between several

centimetres and several decimetres in diameter. The mag-

matic rocks contain up to 93 % plagioclase, with minor quartz,

apatite, epidote, titanite, ilmenite, and zircon. Zircon grains

obtained from two samples have prismatic euhedral shapes

and probably crystallized from quartz dioritic magma (Fazlnia

et al. 2007). The initial texture of quartz-diorites was granular,

but this early magmatic texture has been overprinted to

mylonite as a result of shearing during the Neotethys closing

in the Late Cenozoic (Mohajjel et al. 2003; Golonka 2004;

Davoudian et al. 2008). The accessory minerals mentioned are

euhedral and form the matrix along with quartz, suggesting

magmatic crystallization in small pegmatitic and coarse-

grained patches.

There are five types of xenoliths: (a) cognate enclaves: fine-

grained inclusions of quartz diorite, (b) basaltic andesite to

andesite, (c) meta-pelite, (d) meta-basite, and (e) xenoliths

with large grains of quartz which contain abundant inclusions

of orthopyroxene, clinopyroxene, two types of amphibole,

plagioclase, biotite, muscovite and tourmaline. Here we

describe only the meta-pelitic xenoliths derived from the

country rocks, because they are plentiful and played a signifi-

cant role in contaminating the quartz dioritic magma and also

producing peraluminous granites and tourmaline pegmatites.

It should be noted that many of the xenoliths are migmatite.

Many meta-pelitic xenoliths throughout Chah-Bazargan

batholith underwent high-grade contact metamorphism within

the batholith. Some of them have abundant bands, pods and

patches of leucocratic quartzo-feldspathic leucosome that is

interpreted as former melt visible in hand specimens (Fig. 2)

and microscopic scale (Fig.3a, b). Segregation of the melt

fromtheresidualphases(melanosome;Fig.2a–c, e)ofmeta-

pelitic (migmatitic) xenoliths such as cordierite, biotite and

garnet (in some xenolithic aggregations) have formed small

peraluminous granite patches in the intrusion. The small dark

patches are fragments of melanosome just to the right of the

mesosome (a mixture of melt and the refractory and relic

parts; Fig. 2b), up and center of the Fig. 2e.

Metapelitic xenoliths in the Chah-Bazargan batholith can be

subdivided into stromatic migmatites with mesosomes and

leucosomes(Fig.2a, c),andnebuliticmigmatites(Fig.2b,d–e).

Stromatic migmatites represent the lower-grade migmatites,

extensively similar to metatexites as defined and described by

Brown (1979; also see geochemistry section). Stromatic mig-

matites consist of small-scale (several mm to several cm)

alternating layers of neosome and mesosome. The pre-

migmatisation fabric is well preserved within the paleosome

(Fig.2a, c)andtheratioofleucosometomelanosomeinthe

neosome may vary. The relationship between the melano-

somes and leucosomes of the stromatic migmatites is mostly

gradational(Fig.2a, c).

Nebuliticmigmatites(Fig.2b, d)aresimilartothediatexites

(thereareschlierenintheFig.2b, e)ofMehnert(1968),Brown

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(1979), and Sawyer (2008b). They usually represent higher-

grade migmatites. Nebulitic migmatites (migmatite with dif-

fuse relics of pre-existing rocks or rock structures) contain

irregular islets of neosome dispersed in the paleosome, the

limits between these two are blurred and irregular. Typically,

they are located close to small patches of peraluminous granite

in the Chah-Bazargan intrusion. Leucosomes occur mostly as

concordant veins with diffuse and irregular borders towards

the melanocratic rock portions. There is considerable variation

in the proportion of mafic relative to leucocratic material,

usually the mafic material forms ample mafic schlieren orien-

ted parallel to the foliation (Fig. 2b). The relationship between

the nebulitic migmatites and small peraluminous granitic

patches is mostly gradational. Diatexite migmatites with

Fig. 2. Photos of migmatitic xenoliths. a — Outcrop of stromatic-

structured metatexite migmatites with mesosomes and leucosomes;

b — Morphology of nebulitic-structured diatexite migmatites. This is

a mafic schlieren oriented parallel to the foliation in the upper right;

c — Outcrop of stromatic-structured metatexite migmatites. The rela-

tionship between the mesosomes and leucosomes is gradational;

d — Diatexite migmatites with a simple morphology. They are

characteristic of the highest grade parts of xenoliths where the propor-

tion of neosome is very high. Schlierens (melanosome) are dispersed

throughout the leucosome.; e — The individual melanosome (mafic

schlieren) in nebolitic-structured diatexite migmatite.

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a mixed morphology of melanosome and leucosome (Fig. 2d)

are characteristic of the highest grade parts of the xenoliths

where the proportion of neosome is very high (see also Sawyer

(2008b) for more discussion).

K-feldspar in the meta-pelitic (migmatitic) xenoliths occurs

as small to large irregular to regular perthitic crystals

(0.2–5 mm), which shows eutectic intergrowth with quartz.

Plagioclase occurs as a large and euhedral mineral (Fig. 3)

with zoning (Fig. 3c, e; mineral chemistry section shows

plagio clase composition). Cordierite is commonly subhedral

to euhedral with inclusions of spinel, quartz, and biotite in the

samegrain(Fig.3d, e, i).Garnetinmeta-peliticxenolithswas

either consumed or present as relict phases in quartz and pla-

gioclase(Fig.3b, e)asaresultofpartialmeltinginmeta-pelitic

(migmatitic) xenoliths. Sillimanite is found as both fibrolite

mats and prismatic grains (Fig. 3d) during contact metamor-

phism in the meta-pelitic xenoliths. The former is present as

a retrograde phase along with biotite, poikilobastic plagioclase

and ilmenite. The latter is present in prograde mineral assem-

blages (Table S2) along with garnet, spinel, cordierite and

K-feldspar (Fig. 3d) during contact metamorphism; it is also

presented as a result of a replacement process in late-stage

muscovite (Fig. 3h). Muscovite in many meta-pelitic xenoliths

is only present within quartzo-feldspathic veins (Fig. 3f),

suggesting that it may have been formed during the late stage

of crystallization of the melt (restite-melt back reaction), but

in the other parts it is probably a retrograde phase around

cordierite and/or sillimanite (Fig. 3h). Spinel occurs together

with prograde mineral assemblages in the matrix (Table S2;

Fig. 3g) or as an inclusion phase in cordierite (Fig. 3f), but

spinel and quartz are not in contact together. Some metapelitic

xenoliths that have up to 80 % cordierite, biotite, and

K-feldspar have corundum in the matrix (Fig. 3j) but no

quartz. Some meta-pelitic xenoliths have ~75 % cordierite,

suggesting that they are residues after partial melting or reflect

an unusual starting bulk composition.

Small patches of peraluminous granite (one metre to several

tens metres across) that occur as sharp lenses and tourmaline

pegmatites (tens centimetres to several metres across and tens

of metres in length; average grain size is 1–50 mm), veins or

sheets are located adjacent to diatexitic xenoliths. Peraluminous

granites have two kinds of mineral assemblages (average grain

size is 0.2–5 mm): (a) Kfs–Pl–Qtz–Bt–Ms–Crd–Sil–Tur, and

(b) Kfs–Pl–Qtz–Bt–Ms–Grt–Sil–Tur±Crd (Tables S1, S2;

mine ral abbreviations after Kretz (1983)). K-feldspar, quartz

and plagioclase are abundant minerals in this rock type.

Mineralogically and texturally, they are similar to quartzo-

feldspathic melt veins within metapelitic xenoliths (leuco-

some; Fig. 2). Texturally, all peraluminous granites are

granular and granophyric with perthitic alkali feldspar sug-

gesting that quartz, K-feldspar and albite crystallized as eutec-

tic intergrowths. Cordierite and garnet occur as porphyroblastic

xenocrysts similar to the diatexitic xenoliths. Garnet is sub-

hedral and generally rounded without inclusions. Cordierite is

subhedral with many inclusions of quartz, spinel, biotite, mus-

covite, and tourmaline. Sillimanite occurs as prismatic inclu-

sions in muscovite, whereas muscovite and other minerals are

presented in a granular texture. This suggests that sillimanite

is xenocrystic from the metapelitic xenoliths whereas musco-

vite is the result of late magmatic crystallization.

Analytical methods

All microprobe analyses were performed with a JEOL JXA

8900 microprobe at the University of Kiel, Germany. For the

analyses of major phases we used a 15 or 20 nA probe current

at an accelerating potential of 15 kV. Selected standard names

of the oxides SiO

, MnO, CaO, MgO, TiO

, Al

, FeO, Na

and K

O for all minerals are wolMAC, teph, wolMAC,

foMAC, rt_st8, crn657s, fay85276, ano133868, and

mic143966, respectively. Standard deviations (S.D. (%)) of Si,

Mn, Ca, Mg, Ti, Al, Fe, Na, and K for all analysed points are

0.12, 0.26, 0.15, 0.14, 0.12, 0.09, 0.26, 0.4, and 0.23, respec-

tively. Composition of perthitic K-feldspar was calculated by

analyses of BSE images and point-counting of the perthite.

Major-element mineral compositions in selected samples of

the Chah-Bazargan batholith are listed in Table S3. Analyses

of coexisting minerals were obtained for Sil–Crd–Grt-

and Crd–Kfs–Grt–Sil-bearing xenoliths, peraluminous

granites, host rocks (quartz-diorite), and contaminated

host rocks.

Table 1 lists the chemical compositions of 20 representative

samples obtained by XRF (X-ray florescence instrument;

Philips PW 1480) at the University of Kiel, Germany. Major

elements were measured using fusion beads. H

−

of samples

(moisture) was determined by heating powders at 110 °C for

2 hours and calculated from the decrease in powder weights.

LOI (loss on ignition) of samples was determined by heating

powders of the samples at 1000 °C for 2 hours. The decrement

Fig. 3. Photos of migmatitic metapelitic xenoliths. a — (XPL light) and b — (PPL light) high-grade contact metamorphism (nebulitic- structured

diatexite migmatite) along with bands, pods and patches of leucocratic quartzo-feldspathic melt (leucosome). Biotite shows a poikiloblastic

texture, suggesting dehydration melting of biotite; c — Plagioclase with oscillatory zoning surrounded the cordierite and biotite suggesting the

presence of melt in the migmatitic xenoliths (XPL light); d —Prismaticsillimanitealongwithbiotite + cordierite + plagioclase + K-feldspar + quartz

in the migmatitic xenoliths (PPL light). Spinel is present within cordierite; e — Plagioclase with oscillatory zoning surrounding absorbed garnet

and biotite manifest that melt is present in the migmatitic xenoliths (XPL light); f , g — Presence of spinel within cordierite (XPL light) and in

matrix (PPL light), respectively, suggests high-grade contact metamorphism in the migmatitic xenoliths; h — Presence of late-stage muscovite

around sillimanite; i — Picture of leucosome from nebulitic-structured diatexite migmatite. There is late-stage muscovite around biotite;

j — Presence of corundum in the matrix. This sample contains cordierite, biotite, and K-feldspar up to 80 %. Abbreviations are after

Kretz (1983).

451

THE CHAH-BAZARGAN PERALUMINOUS GRANITES — PETROLOGICAL CONDITIONS

GEOLOGICA CARPATHICA

, 2017, 68, 5, 445–463

452

FAZLNIA

GEOLOGICA CARPATHICA

, 2017, 68, 5, 445–463

of powders weights was then calculated.

Method Detection Limits (MDL) are deter-

mined by the X-ray florescence lab. For trace

elements, fourteen samples were analysed

with an AGILENT 7500cs ICP–MS (induc-

tively coupled plasma-

mass spectrometry)

instrument at the Uni versity of Kiel, Germany,

and six samples were analysed with an

ICP–MS instrument at the ALS Chemex

Company of Canada (Table 2). Method

Detection Limits (MDL) were determined by

the ICP–MS lab.

Mineral chemistry

Garnet

Garnet from all the meta-pelitic xenoliths

has a narrow range in Mg, Fe, Ca and Mn con-

tents, and is characterized by Fe-rich compo-

sitions and flat zoning profiles. Garnet from

Grt–Crd–Sil meta-pelitic xenoliths displays

higher Mg content with wide cores that have

uniform compositions (approximately Alm

Prp

, Sps

, Grs

) and rims up to 0.5 mm

wide, displaying a smooth increase in Mn and

decrease in Mg with constant Fe and Ca

(Fig. S1a). Garnet from Grt–Crd-bearing

meta-pelitic xenoliths is slightly zoned and

contains higher Mn (Alm

, Prp

, Sps

Grs

) (Fig. S1b). It also shows a slight

increase of Fe and Mn towards rims indica-

ting retrogression. Garnet of peraluminous

granites is weakly zoned and shows a slight

increase in Fe from the core to the inner rim

and then a slight decrease from the inner rim

towards the outer rim as well as a slight

decrease in Mn from the core to the inner rim

and then a slight increase from the inner rim

towards the outer rim with constant Mg and

Fe, suggesting retrogression (Fig. S1c).

Cordierite

The Mg# (= 100× atomic Mg / (Mg + Fe

))

values of cordierite in several meta-pelitic

xenoliths are in the range of 49 to 56. In some

xenoliths, Mg content of cordierite decreases

from the core to the rim. Some meta-pelitic

xenoliths have ~75 % cordierite, suggesting

that they are residues after partial melting or

reflect an unusual starting bulk composition.

Cordierite composition in peraluminous gra-

nite is broadly similar to that in the meta-

pelitic xenoliths.

Sample

140-1

187

190-B

189-E

260

264

272

181-E

182-E2

183-E1

188-E1

189-E3

190-E1

191-E5

192-E2

193-E3

111

-c

114-a

220

221

Average

Rock type

P-g

Xeno

Pelite

migmatite

metapelite

MDL

Grt

Crd

Mig

Granite

Xenolith

& Xenolith

wt.

Kiel

SiO

0.01

74.12

73.91

73.58

74.45

74.29

75.30

75.24

43.39

62.68

57.22

66.82

64.25

59.22

63.05

65.1

60.22

59.04

64.16

58.2

60.64

74.35

54.43

62.07

0.01

13.85

14.03

14.18

13.85

13.65

13.18

13.1

26.77

17.71

20.12

16.41

16.65

18.83

17.13

16.36

17.35

19.41

16.96

19.48

16.09

13.73

21.53

17.47

0.01

0.06

0.05

0.09

0.07

0.09

0.08

2.14

0.92

1.17

0.29

0.58

0.39

0.85

0.75

0.87

0.81

0.74

0.88

0.85

0.07

1.41

0.70

MgO

0.01

0.14

0.1

0.13

0.27

0.31

0.26

0.28

5.17

2.07

4.87

1.90

2.15

3.75

2.55

2.01

3.55

1.87

3.56

3.46

3.65

0.20

4.04

2.85

FeO*

0.04

1.28

1.10

1.38

1.21

1.20

1.24

1.23

15.74

6.92

10.53

5.84

4.85

6.27

6.33

5.88

7.49

5.80

5.65

6.96

7.50

1.24

11.06

6.26

CaO

0.01

0.65

0.72

0.59

0.71

0.66

0.63

0.56

0.84

1.34

1.21

2.44

3.05

1.59

2.21

2.45

1.22

0.64

0.74

0.52

0.75

0.65

1.13

1.56

0.01

0.10

0.1

0.12

0.1

0.12

0.03

0.15

0.08

0.05

0.12

0.13

0.09

0.1

0.19

0.17

0.15

0.21

0.1

0.09

0.14

0.01

2.04

1.82

2.32

2.95

2.73

2.87

2.83

0.79

1.79

0.84

2.16

2.88

2.44

1.73

1.81

1.94

0.43

1.58

1.71

1.93

2.45

1.14

1.86

0.01

5.95

6.20

6.10

5.05

5.21

5.04

5.10

1.76

3.90

1.55

1.70

2.55

4.12

3.87

2.94

4.18

6.81

2.33

3.75

4.09

5.59

2.40

3.63

MnO

0.01

0.06

0.07

0.06

0.04

0.05

0.04

0.40

0.1

0.34

0.18

0.24

0.20

0.24

0.18

0.17

0.27

0.06

0.08

0.16

0.05

0.28

0.18

Total

98.25

98.16

98.51

98.77

98.28

98.81

98.64

97.21

97.75

97.93

97.86

97.32

96.94

98.05

97.60

97.18

95.25

95.93

95.25

95.87

98.47

97.63

96.73

LOI

1.25

1.08

0.75

0.91

1.12

0.86

0.84

2.02

2.07

1.81

2.03

2.32

1.65

1.48

1.88

1.68

3.45

3.43

3.52

2.4

0.98

1.97

2.38

CIPW

norm

Qtz

37.09

37.26

34.79

35.37

35.91

36.91

36.98

10.74

26.62

28.56

35.01

24.51

15.51

25.04

30.89

19.82

22.33

35.36

23.00

21.54

36.275

21.97

25.3

35.16

36.64

36.05

29.84

30.79

29.78

30.14

10.40

23.05

9.16

10.05

15.07

24.35

22.87

17.37

24.70

40.24

13.77

22.14

24.17

33.035

14.20

21.45

17.26

15.40

19.63

24.96

23.1

24.29

23.95

6.68

15.15

7.1

18.28

24.37

20.65

14.64

15.32

16.42

3.64

13.37

14.47

16.33

20.775

9.65

15.74

2.57

2.85

2.14

2.80

2.56

2.34

1.99

3.97

5.67

5.48

11.78

14.35

7.04

10.38

11.44

4.81

2.06

2.69

1.21

2.35

2.45

5.04

6.82

Crn

3.1

3.28

2.98

2.50

2.58

2.15

2.20

22.1

8.47

15.05

6.7

3.89

7.78

6.29

6.01

7.87

10.57

10.85

12.17

7.63

2.75

15.21

7.98

2.71

2.34

2.24

2.82

2.95

2.87

2.90

38.99

16.55

30.17

15.31

13.75

20.58

17.02

14.90

21.47

14.47

18.13

20.09

21.76

2.775

28.57

17.77

Ilm

0.1

0.09

0.10

0.17

0.13

0.17

0.15

4.06

1.75

2.22

0.55

1.10

0.74

1.61

1.42

1.65

1.54

1.41

1.67

1.61

0.12

2.68

1.33

0.23

0.25

0.28

0.25

0.28

0.07

0.35

0.19

0.12

0.28

0.30

0.21

0.25

0.44

0.39

0.35

0.49

0.265

0.20

0.32

FeO* is total FeO; Kiel = Kiel University; Xeno = Xenolith; P-g = Per

-aluminous granite; Grt = Garnet; Crd = Cordierite; MDL: Method Detection Limit.

Table 1:

Representative whole rock geochemical analyses (XRF) of major elements of Chah-Bazar

gan rocks along with CIPW

norm.

453

THE CHAH-BAZARGAN PERALUMINOUS GRANITES — PETROLOGICAL CONDITIONS

GEOLOGICA CARPATHICA

, 2017, 68, 5, 445–463

Sample

140-1

187

190-B

189-E

260

264

272

181-E

182-E2

183-E1

188-E1

189-E3

190-E1

191-E5

192-E2

193-E3

111

-c

114-a

220

221

Average

Granite

Average

migmatite Xenolith

Average

metapelite & Xenolith

Average

Shale Li, 2000

Rock type

P-g

Xeno

Pelite

MDL

Grt

Crd

Mig

wt.%

Kiel

CCC

Kiel

CCC

0.2

3.32

2.23

2.85

5.05

6.65

7.59

7.32

266.33

138.90

185.42

64.41

85.25

112.20

106.2

73.6

98.32

108.2

137.7

123.1

110.7

5.00

196.88

101.97

130.00

0.1

1.06

0.89

0.97

2.46

2.89

3.23

2.12

153.54

79.94

94.01

64.61

58.60

74.13

60.2

81.1

71.43

69.4

58.6

82.7

75.3

1.95

109.16

69.61

90.00

0.1

0.69

0.49

0.88

1.02

0.95

0.77

0.59

30.24

14.06

19.73

8.97

10.12

17.98

12.1

14.2

15.59

18.2

13.1

10.3

14.1

0.77

21.34

13.47

19.00

0.1

0.91

1.08

1.12

1.62

1.55

1.30

1.41

106.1

34.16

62.31

25.48

19.87

32.54

30.5

34.4

31.58

31.2

46.4

22.9

38.8

1.28

67.53

31.37

50.00

0.1

165.12

144.19

148.56

114.38

138.95

157.08

165.05

67.66

132.61

88.47

47.81

40.32

54.17

77.1

39.5

54.67

114.1

75.3

85.6

63.5

147.62

96.25

65.21

140.00

0.5

6.08

6.28

5.69

15.04

11.21

7.54

13.17

43.25

102.21

80.25

52.49

75.71

41.21

69.4

68.9

58.62

47.4

79.5

94.1

83.7

9.29

75.24

67.10

170.00

0.1

3.78

3.54

4.56

6.31

7.42

5.57

6.14

53.41

26.60

35.34

43.55

51.13

67.14

55.8

55.2

59.12

38.3

53.7

48.9

65.4

5.33

38.45

53.82

26.00

0.1

65.12

55.29

49.67

46.60

55.15

50.81

44.42

352.27

175.40

241.31

178.87

191.32

219.31

263.3

155.7

207.32

148.6

174.3

170.5

193.8

52.44

256.33

190.30

160.00

0.1

42.85

32.22

38.65

4.22

4.58

3.43

3.93

38.41

13.77

19.12

9.14

12.15

31.24

21.3

17.6

20.12

25.3

51.6

43.7

34.8

18.55

23.77

26.70

11.00

1.0

36.78

47.43

43.15

76.43

58.99

24.25

66.08

132.92

389.15

120.31

54.24

72.61

157.19

187.3

122.3

131.54

432.1

201.5

345.6

398.3

50.44

214.13

210.27

580.00

0.1

0.87

0.96

1.08

1.40

1.27

1.14

1.32

47.33

34.34

40.27

15.76

13.20

32.74

28.4

18.7

25.24

39.2

31.3

44.8

50.9

1.15

40.65

30.02

43.00

0.1

4.39

4.12

5.12

6.03

5.87

5.55

5.06

98.18

66.96

76.48

31.26

30.15

65.34

58.2

42.1

52.12

64.1

60.3

79.7

83.2

5.16

80.54

56.65

82.00

0.02

0.31

0.26

0.23

0.45

0.40

0.36

0.41

11.32

8.37

10.26

3.88

4.45

8.43

7.5

6.1

7.21

6.8

8.3

9.8

11.2

0.35

9.98

7.37

9.80

0.3

0.88

0.97

1.13

1.77

1.46

1.37

1.58

41.77

31.40

35.89

14.52

17.89

32.12

29.4

21.4

25.71

27.3

34.1

32.5

41.8

1.31

36.35

27.67

33.00

0.05

0.35

0.28

0.30

0.63

0.50

0.46

0.54

7.37

6.1

6.73

3.26

5.07

8.49

7.1

4.9

7.33

5.2

8.3

7.4

9.1

0.44

6.74

6.62

6.20

0.02

0.05

0.03

0.04

0.07

0.05

0.04

0.06

0.37

1.20

0.71

0.66

1.02

1.31

1.2

0.8

1.21

0.94

1.3

1.1

1.5

0.05

0.76

1.10

1.20

0.05

0.41

0.34

0.49

0.79

0.62

0.57

0.67

7.33

5.50

6.63

4.19

6.27

9.28

8.9

6.4

8.07

6.3

8.5

7.6

9.8

0.56

6.49

7.53

5.10

0.01

0.07

0.08

0.09

0.18

0.17

0.13

0.15

1.44

0.84

1.12

0.91

1.25

2.02

1.8

1.2

1.67

1.2

1.8

1.6

2.1

0.12

1.13

1.56

0.84

0.05

0.71

0.62

0.67

1.18

1.07

0.96

1.1

10.30

5.08

7.24

6.87

8.45

12.83

11.3

9.1

11.09

7.6

11.5

9.8

13.5

0.90

7.54

10.20

4.70

0.02

0.14

0.13

0.15

0.23

0.20

0.19

0.22

2.20

1.03

1.57

1.54

1.88

2.75

2.5

1.9

2.37

1.7

2.5

2.2

2.9

0.18

1.60

2.22

1.10

0.03

0.51

0.43

0.40

0.65

0.63

0.56

0.61

6.29

2.86

3.93

4.46

5.68

7.56

6.7

5.8

6.73

5.2

7.5

6.4

8.2

0.54

4.36

6.42

3.00

0.01

0.07

0.08

0.09

0.1

0.09

0.10

0.96

0.43

0.59

0.68

0.87

1.15

1.0

0.9

0.92

0.8

1.2

0.9

1.2

0.09

0.66

0.96

0.44

0.05

0.64

0.69

0.76

0.84

0.76

0.65

0.69

6.35

2.91

3.79

4.44

5.79

7.71

6.7

5.5

6.46

5.1

7.5

6.2

8.4

0.72

4.35

6.38

2.80

0.01

0.12

0.10

0.14

0.12

0.1

0.09

0.94

0.43

0.60

0.66

0.87

1.13

1.0

0.8

0.91

0.8

1.1

0.9

1.2

0.1

0.66

0.94

0.42

0.1

3.12

2.37

2.75

2.23

2.50

2.21

1.88

10.95

5.33

4.89

5.72

4.84

9.78

7.6

6.3

8.41

6.3

8.6

8.1

9.8

2.44

7.06

7.55

5.00

0.1

2.68

2.16

3.1

1.120

0.89

0.40

0.72

3.1

0.98

2.46

0.94

1.37

2.68

1.8

1.5

2.25

2.7

2.5

2.9

3.4

1.58

2.18

2.20

1.30

0.1

15.25

17.46

20.12

25.92

20.45

14.47

13.39

5.26

24.59

18.34

13.51

19.87

21.23

29.7

16.4

23.55

17.7

20.8

24.2

28.7

18.15

16.06

21.57

20.00

0.2

1.14

0.90

1.39

2.67

2.24

1.91

1.76

18.93

13.92

15.72

9.73

10.68

14.28

11.5

9.1

15.88

13.1

14.2

16.4

12.2

1.72

16.19

12.71

12.00

0.1

0.72

0.90

1.01

2.24

1.52

0.88

0.68

1.68

2.1

2.04

2.1

2.61

2.75

2.3

2.5

2.71

2.3

1.8

2.1

1.14

1.94

2.42

2.70

751

626

1126

876

1126

1001

26783

11514

14643

3630

7259

4881

10638

9387

10889

10138

9262

11014

10638

876

17647

8773

4600

704

775

845

775

845

211

1057

564

352

845

916

634

775

1339

1198

1057

1479

795

611

1007

700

63166

65820

64759

53612

55310

53505

54142

18684

41403

16455

18047

27071

43739

41085

31212

44376

72296

24736

3981

43420

58616

25514

38579

28239

44367

39582

50457

64158

59374

62418

61548

17181

38930

18269

46977

62636

53067

37625

39365

42192

9352

34363

37190

41975

54558

24793

40474

12832

Rb/St

27.16

22.96

26.1

7.61

12.40

20.83

12.53

1.56

1.30

1.10

0.91

0.53

1.31

1.1

0.57

0.93

2.41

0.95

0.91

0.76

18.51

1.32

1.04

0.82

Rb/Ba

4.49

3.04

3.44

1.50

2.36

6.48

2.50

0.51

0.34

0.74

0.88

0.56

0.34

0.41

0.32

0.42

0.26

0.37

0.25

0.16

3.40

0.53

0.40

0.24

K/Ba

1717.4

1387.7

1500.8

701.4

937.6

2206.4

819.3

140.6

106.4

136.8

332.7

372.8

278.3

219.4

255.2

337.4

167.3

122.8

115.2

109.0

1324.4

127.9

231.0

48.69

Eu*

0.1

0.09

0.12

0.21

0.17

0.15

0.18

2.16

1.71

1.97

1.10

1.67

2.62

2.36

1.67

2.27

1.70

2.47

2.21

2.78

0.15

1.95

2.09

1.66

Eu/Eu*

0.30

0.22

0.23

0.22

0.20

0.18

0.22

0.1

0.47

0.24

0.40

0.41

0.33

0.34

0.32

0.36

0.37

0.35

0.33

0.36

0.22

0.26

0.35

0.48

/Yb

0.14

0.18

0.14

0.22

0.24

0.28

0.94

1.50

1.26

0.45

0.28

0.54

0.53

0.44

0.52

0.92

0.53

0.93

0.80

0.20

1.16

0.60

1.92

/Sm

0.54

0.75

0.79

0.49

0.56

0.54

0.53

1.40

1.23

1.31

1.06

0.57

0.84

0.88

0.83

0.75

1.65

0.82

1.32

1.22

0.57

1.32

0.99

1.52

/Yb

0.43

0.33

0.43

0.63

0.54

0.58

0.65

0.77

1.26

1.17

0.63

0.72

0.80

0.89

0.78

0.83

0.82

0.76

0.82

0.78

0.52

0.99

0.79

1.21

/Yb

1.33

1.28

1.17

2.20

1.97

0.34

0.26

0.25

0.47

0.41

0.44

0.49

0.73

1.32

1.12

0.46

0.55

0.69

0.67

0.56

0.75

0.70

0.64

0.71

Kiel = Kiel University; CCC=ALS Chemex Company of Canada; Xeno = Xenolith; P-g = Per

-aluminous granite; Mig = Migmatite; Grt = Garnet; Crd = Cordierite; MDL: Method Detection Limit.

Table 2:

Representative whole rock geochemical analyses (ICP-MS) of minor and rare earth elements of the Chah-Bazar

gan rocks.

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Biotite and muscovite

Biotite from different rock types has a wide range of compo-

sitions (Fig. S2; Table S3). It is more enriched in Mg in

meta-pelitic xenoliths compared to the peraluminous granites,

suggesting that biotite in peraluminous granite may have crys-

tallized from magma or changed in composition due to restite-

melt back reaction (also see Erdmann et al. 2009; Taylor &

Stevens 2010 for more information). In addition, the biotite

might also change composition because it has reacted with the

very large volume of granite around it (Lavaure & Sawyer

2011). Biotite in meta-pelitic xenoliths and contaminated

quartz diorite is similar in composition, suggesting that biotite

in the contaminated quartz diorites is not a result of magmatic

crystallization and so must have come from the meta-pelitic

xenoliths in the host magma. Biotite from meta-pelitic xeno-

liths with many veins (diatexite) has much higher Ti content

than meta-pelitic xenoliths lacking such veins (without mig-

matitic structure). This is probably due to higher metamorphic

temperature (see Henry & Guidotti 2002 for more discussion)

of the diatexite. Biotite in all rock types have a wide range of

Ti, which might be due to diffusional exchange, so that it is

confirmed by very small grains of ilmenite within biotite coro-

nas around garnet which are a result of retrograde reactions

after magma solidification.

Muscovite in all rock types, both prograde and retrograde,

has a similar composition (Table S3).

Spinel, ilmenite, and apatite

All analysed spinel grains are rich in FeAl

component,

withCr(~ 0.07p.f.u.)andrelativelyhighZn(~ 0.55p.f.u.).

Hercynite (spinel) from matrix is similar to that included in

cordierite.

All analysed ilmenites have compositions close to the

FeTiO

end-member (Table S3). Apatite from all rock types

has higher Mn and F but lower Cl contents.

K-feldspar

Many K-feldspar grains are perthitic. Perthitic K-feldspar

has a re-integrated composition of X

kfs

0.85–0.88. These com-

positions were calculated by analyses of BSE images and

point-counting of the perthite.

Plagioclase

Plagioclase has a wide range of Ca and Na contents

(Fig. S3). In quartz-diorites, plagioclase is andesine and shows

a narrow range of Ca and Na and a slight decrease in Ca and

increase in Na near the rim, but the main part of their profiles

are approximately flat (Table S3; Fig. S3a). Plagioclase grains

from contaminated quartz diorites are also mostly andesine,

showing a flat profile and a main decrease in Ca content near

the rim. Other plagioclase grains (Fig. S3a–c) have different

profiles, and indicate a pronounced decrease in Ca from the

core towards the rim, then a sharp increase in Ca towards the

outermost part of the rim, suggesting a magma mixing process

(Fig. S3b). In cordierite-rich metapelitic xenoliths (nebulitic

migmatites; diatexite), plagioclase is mostly andesine but

shows a decrease in Ca near the rim (Fig. S3c). Plagioclase in

the peraluminous granites (Fig. S3d) indicates a profile similar

to that from contaminated quartz diorites, but more enriched in

Na (oligoclase). The cores from the peraluminous granite

shown in Fig. S3d are substantially less calcic compared to the

plagioclase from the quartz diorite. The plagioclase core of

rocks may have been a part of plagioclase minerals crystal-

lized from primary quartz dioritic magma. It is possible that

the amount of calcium in cores of plagioclase from the peralu-

minous granite has fallen due to diffusion (see also García-

Arias&Stevens(2017a, b)andMoyenetal.2017formore

discussion).

Oscillatory zoning occurs within both core and rim domains

(e.g., Fig. 3c, e). Such zoning patterns are normally present

only in plagioclase of igneous rocks, rim wards enrichment in

Na is commonly interpreted as reflection of decreasing tem-

peratures during fractional crystallization. Therefore, these

zoning patterns strongly suggest that plagioclase in all rock

types, especially in metapelitic xenoliths, crystallized in the

presence of melt, with rims crystallized during cooling, and

also indicate that plagioclase with oscillatory zoning sur-

roundedthecordieriteandbiotite(Fig.3c, e).Theseobserva-

tions indicate that melt was present in the metapelitic

xenoliths.

Geothermobarometry

In this section thermobarometry has been used to estimate

the peak P–T conditions of metamorphism in the studied

metapelitic xenoliths and peraluminous granites. These results

provide information about (1) the conditions of partial melting

in metapelitic xenoliths, and (2) the crustal level of emplace-

ment of the quartz diorite.

Kriegsman (2001) discussed that the ultimate effect of mig-

matization comes from four successive processes: prograde

partial melting; melt extraction close to peak temperatures;

incomplete retrograde reactions between restite and in situ

crystallizing melts; and crystallization of remaining melt at

the solidus. Mineral assemblages formed in the peak and

retrograde metamorphic stages of the Chah-Bazargan migma-

titicxenolithsareBt + Grt + Sil + Crd + Spl + Crn + Pl + Kfs + Qtz

(Fig. 2a–g, i, j) and Ms + Chl + fibrous Sil + Qtz, respectively.

Based on Kriegsman (2001) and White and Powell (2002),

retrograde mineral assemblage in anatectic migmatites is

a result of partial retrograde reactions (back reaction) between

in situ crystallizing melt and restite. Kriegsman & Hensen

(1998) demonstrated that back reaction has significant impli-

cations for geothermobarometry. For this reason, suitable

mine rals, near the peak temperatures for geothermobarometry,

were selected. The minerals were chosen from sections far

from retrograde mineral assemblages. Analytical point of the

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different minerals such as garnet, plagioclase, and biotite were

defined on the basis of parts close to the peak temperatures

and chemical compositions (Table S3) and profiles of different

minerals (Figs. S1–S3). To investigate the peak metamorphic

conditions, garnet with high pyrope component, biotite with

low X

and high Ti level and plagioclase with high anorthite

component were selected.

Peak metamorphic conditions of regional metamorphic

rocks to the southwest of the Chah-Bazargan quartz diorite, in

the Qori metamorphic complex, were estimated by Fazlnia

et al. (2007) using several conventional geothermobarometers,

such as Grt–Ky–Qtz–Pl (GASP), Grt–Bt–Pl–Qtz, Grt–Ms–

Pl–Qtz, Grt–Pl–Bt–Ms and Grt–Hbl–Pl–Qtz barometers and

Grt–Bt, Grt–Hbl and Hbl–Pl thermometers. The peak pressure

and temperature of regional metamorphism in the Seghalaton

outcrop of QMC (eastern part of the study area; Fig. 1) at 187

to 180 Ma were estimated to be 7.5±1.2 kbar and 660±40 °C

(Fazlnia et al. 2007, 2009). The pressure estimation allows

depth of burial to be estimated at ca. 29 km. Following the

emplacement of the intrusion, a secondary metamorphic event

affected the QMC at 147 Ma due to the initiation of Neotethyan

mid ocean ridge subduction beneath the southern Sanandaj–

Sirjan zone. Trondhjemitic dykes were created as a result of

this event (Fig. 1). The peak P–T estimations of the arc-related

metamorphism are 9±1.2 kbar and 700±30 °C (Fazlnia et al.

2009; also see Sheikholeslami 2015).

Peak metamorphic contact condi-

tions in metapelitic xenoliths and per-

aluminous granites were estimated

using conventional calibrated thermo-

barometers, thermometric diagrams

are shown in (Fig. 4). The calibrations

include the Grt–Bt thermometers

(Thompson 1976; Holdway & Lee

1977; Ferry & Spear 1978; Hodges &

Spear 1982; Perchuk & Lavrent’eva

1983; Dasgupta et al. 1991; Bhatta-

charya et al. 1992; Gessmann et al.

1997; Kaneko & Miyano 2004;

Table S4), and Grt–Sil–Pl–Qtz

(Hodges & Spear 1982) and Grt–Bt–

Pl–Qtz (Wu et al. 2004), barometers

(Table S5). A thermometric diagram

of Zr-M index (Watson & Harrison

1983) was used for peraluminous

granites (Fig. S4). On the basis of X

in cordierite (Thompson 1976), meta-

pelitic xenoliths and peraluminous

granites, which include assemblage

Grt–Crd–Sil–Qtz (Table S2), are

plotted at pressures between 4.5 and

5.5 kbar (Fig. 4).

The current thermobarometeric

results are based on mineral core

com positions of matrix phases. The

thermobarometric results estimate

peak P–T conditions for metapelitic xenoliths, peraluminous

granite and partial melting of metapelitic xenoliths to be

~4.5±1.0 kbar and ~760±35 ºC (Fig. 4). The temperature value

is in agreement with petrographic evidence for the initiation of

hydrate breakdown melting of biotite in the presence of garnet

and sillimanite (Fig. 3a–b) and overlaps with the field of bio-

tite melting dehydration (Fig. 4).

Rock geochemistry

Peraluminous granites have restricted SiO

contents between

73–75 wt. %. CaO and MgO between 0.56–0.72 wt. %. and

0.11–0.31 wt. %, respectively. K

O + Na

O have a range

between 6.5 and 8 wt. %. These granites are enriched in Rb,

Zr, Ba and Pb and depleted in Ni, Cr, V, Nd, Sr, Y, Nb, and

have REE contents comparable to S-type granites (Brown

1994; Harris et al. 1995; Bea 1996b; Patiño Douce 1999;

Nabelek & Bartlett 2000; Healy et al. 2004; Stevens et al.

2007; Villaros et al. 2009; García-Arias et al. 2012; Moyen et

al. 2017). Low concentrations of Ni, Cr, V, Sr, Y, Nb, and REE

indicate that they probably remained in the residuum (metape-

litic xenoliths) during partial melting and segregation. Based

on Brown (1994), Brown (2007), García-Arias et al. (2012),

Brown (2013), Sawyer (2014), and García-Arias & Stevens

Fig. 4. Thermobarometric constraint on the P–T evolution of the Chah-Bazargan migmatitic

xenoliths and peraluminous granites. Thin horizontal dashed lines of X

cordierite values are

after Thompson (1976). Wet granite solidus, approximate ranges of dehydration of micas in

presence of quartz and plagioclase and minimum contents of felsic melts; modified from Patiño

Douce & Harris (1998), Holtz & Johannes (1994) and Spear (1993). Three ellipsoid fields repre-

sent crustal-thickening regional metamorphism which occurred 187–180 Ma, contact metamor-

phism 173 Ma, which is related to intrusion of the Chah-Bazargan batholith, and arc-related

regional metamorphism that occurred 147 Ma.

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(2017a, b)severalpotentialfactorsthatmaycontrolthecom-

position of the S-type magmas include: melt loss, batch and

fractional melting, spatially restricted equilibration of plagio-

clase during partial melting and the nature and amount of the

entrained mineral assemblage.

The presence of normative corundum (Table 1) indicates

that these granites are peraluminous, as seen in Fig. 5. All

granites plot in the range of peraluminous granites (Fig. 5) and

were probably extracted from migmatitic felsic metapelite-

metagraywacke (Fig. 6). Leucocratic peraluminous granites

are divided into garnet-bearing and cordierite-bearing granites

based on main minerals of the rocks.

In REE and multi-element plots, garnet-bearing and

cordie rite-bearing granites have approximately the same pat-

terns (Figs. 7a, 8a, S5). The garnet-bearing granites are slightly

enriched in REE in comparison with cordierite-bearing ones

(Fig. 8; Table 2). Also, there are higher U but lower Nb and Ta

values in the cordierite granites relative to the garnet granites

(Figs. 7a, 8a), additionally, the garnet granites have, unexpec-

tedly, rather lower HREE contents (Fig. 7a; Table 2).

The Chah-Bazargan peraluminous granites are characterized

by lower LREE but higher HREE contents and consequently

lower La

/Yb

, La

/Sm

and Gd

/Yb (Table 2) in comparison

with common peraluminous granites (see Brown, 1994 for

more discussions). Garnet-bearing granites show negative-Eu

anomaly(Eu/Eu* = 0.25)andareslightlyenrichedinHREEin

comparison with cordierite-bearing granites, especially Yb

and Lu, reflecting the presence of garnet. All peraluminous

granites have negative-Eu anomaly similar to metapelitic

xenoliths but less pronounced. Negative-Eu anomalies in

granites and also negative-Eu and -Sr anomalies in migmatitic

xenoliths, schist xenoliths, and metapelites show that plagio-

clase was not involved in partial melting reactions of meta-

pelitic xenoliths or had low percentages of contributions

and/or it resulted from protolith composition, and also that

negative-Eu and -Sr anomalies in granites resulted from the

protolith. Peraluminous granites show negative-La anomaly

because of few monazite grains in many metapelitic rock

types from the study area. The REE plots show that these

rocks have a Ce peak rather than La anomaly, reflecting the

enrichment of the source (Figs. 8a, 9a, S5).

Negative-Ba anomalies in all rock types (Figs. 7, S5) show

that abundance of Ba resulted from the protolith (metapelitic

xenoliths). Positive-K anomaly in granites, metapelitic xeno-

liths, and metapelites is due to K-bearing phases such as

K-feldspar and muscovite, which are still stable in all rocks.

Averages of Qori metamorphic metapelite and schist xeno-

liths plots between migmatitic xenoliths and peraluminous

granites can be seen in Fig. 5. Therefore, decrease in K and

Na and increase in Fe and Mg in the migmatitic xenoliths are

consistent with partial melting and melt extraction from pelitic

xenoliths with the mafic minerals such as garnet and cordierite

remaining in the residue.

Total REE, Y, Zr, Hf, Sr, Ba, Th, U, Ti and Nb in the Chah-

Bazargan peraluminous granites is lower than in the meta-

pelites, metapelitic xenoliths and migmatitic metapelitic

xenoliths (Fig. S5). Melts extracted from the metapelitic mig-

matites are depleted in trace elements such as Rb, Zr, Th, U, Y,

and REE, in order to be equivalent to granite plutons and

batholiths in the upper crust (Bea 1996a; Sawyer 1996;

Sheppard et al. 2003). Stability of minerals such as garnet,

cordierite, ilmenite, zircon, and monazite in the residuum

during partial melting causes them to be depleted during melt

extraction.

Discussion

Modelling

Decrease of SiO

, P

, Na

O, and K

O and increase of

, TiO

, MgO, and FeO* in migmatitic xenoliths in

comparison with metapelitic xenoliths and metapelites

Fig. 5. ACF (A is Al

– (Na

O + K

O), C is CaO, and F is

FeO

total

+ MgO) plot delineating fields (Healy et al. 2004) for the

Chah-Bazargan granites, migmatitic xenoliths, and metapelites and

xenoliths without migmatite texture.

Fig. 6. Compositions of the study granites compared to melts pro-

duced by experimental dehydration melting of metasedimentary

rocks (fields of melt compositions after Patiño Douce 1999).

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THE CHAH-BAZARGAN PERALUMINOUS GRANITES — PETROLOGICAL CONDITIONS

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demon strate that residual minerals were

stable phases of migmatitic xenoliths

during partial melting. In contrast, other

minerals were unstable phases during

partial melting reactions and formed

felsic parts of migmatites and small

patches of peraluminous granites.

Geochemical melting models based

on both batch and Rayleigh melting

modelling can be used to determine the

possible amount of partial melting in the

migmatitic xenoliths. Sawyer (1991),

Acosta-Vigil et al. (2006), Brown

(2007), Yakymchuk & Brown (2014),

and García-Arias & Stevens (2017a)

have discussed the most important fac-

tors influencing the composition of the

peraluminous melts such as equilibrium

and fractional melting and crystalliza-

tion during partial melting and crystalli-

zation, flow segregation, gravitational

settling, filter-pressing fractionation, the

amount of water in the original magma,

path of emplacement and cooling,

mineral assemblage of the protolith, and

P–T conditions. Based on presence and

movement of melt in contact with the

initial protolith (Figs. 2, 3a–b) batch

melting equations (Shaw 1970) can be

used for the Chah-Bazargan migmatitic

xenoliths. Melting was modelled using

the equilibrium batch melting equation:

ℓ

= 1

D (1−F)+F

= D

F +D (1−F)

where i is the element of interest, C

the original concentration in solid phase

(and the concentration in the whole

system), C

ℓ

is the concentration in the

liquid (or melt), C

is the concentration

remaining in the solid, F is the melt

fraction (i.e. mass of melt/mass of sys-

tem) and D is partition coefficient of the

interested element: D = C

ℓ

These equations are extremely useful

in describing the relative enrichment or

depletion of a trace element in the liquid

as a function of melting degree.

The averages of metapelites, peralu-

minous granites, and migmatitic xeno-

liths trace elements were used. Thus, the

concentrations of various elements of

Fig. 7. Continental crust normalized multi-element plots of Chah-Bazargan batholith samples.

a — Normalized multi-element diagram of peraluminous granites; b — Normalized multi-

element diagram of metapelitic migmatitic xenoliths; c — Normalized multi-element diagram

of schist xenoliths; d — Normalized multi-element diagram of metapelites from the Qori

metamorphic complex. Normalization values after Taylor & McLennan (1985).

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average initial protolith (C

; metapelitic xenoliths and

metapelites), peraluminous granite (C

ℓ

), and relict

protolith (C

; as restite = migmatitic xenoliths) were

considered (Tables 1, 2). The average composition of

shale (Li 2000) was used for modelling because the

Chah-Bazargan peraluminous granites are plotted in

the field of metagraywackes-felsic metapelites (Fig. 6).

Partial melting

According to Fig. S5, the patterns of metapelitic

xenoliths and metapelites were compared to shale.

The Chah-Bazargan peraluminous granites were used

as melt compositions (Tables 1, 2). Levels of the

migmatitic xenolith elements have not been altered

(Table S6; for more details see Champion & Smithies

2007).

Simple trace-element modelling was used to test

whether the Chah-Bazargan peraluminous granites

bear compositions that are consistent with derivation

by partial melting at low pressures (4.5 kbar; the upper

amphibolite facies) from a migmatitic metapelitic

(xenolith) source. Bulk partition coefficients were cal-

culated assuming 1 %, 5 %, 10 %, 20 %, 30 %, 40 %,

and 50 % partial melting (Table S7). Additionally, as

a measure of suitability of the modelled source compo-

sitions, the degree of partial melting was calculated for

highly incompatible elements and Cr assuming bulk

partition coefficients calculated by partition coef ficient

of different elements for each mineral (see the follo-

wing paragraphs; Table S8). Partition coefficients (K

)

of different elements are similar to those used above.

For a full discussion of partition coefficients usage for

modelling crustal melting see Harris et al. (2003).

We can infer from the results, summarized in

Table S7, apparently the behaviour of all elements,

such as the REEs (La to Lu). The HFSE (Ti, Zr, Ta,

Nb, Th, U, Hf, Y), Ba, Pb, and Sr is largely insensitive

to source enrichment, but sensitive to the amounts of

main and accessory minerals in the residue (diatexitic

migmatites). The abundance of garnet, biotite, plagio-

clase, apatite, ilmenite, zircon and monazite in the

source has increased the values of bulk partition coef-

ficients for all the elements considered above (C

Therefore, the large proportion of these minerals were

stable phases during partial melting of the source.

Hence, partition coefficients increase with increasing

levels of partial melting in the source (Table S7).

Similar to this study, many studies of melts extracted

from the migmatites indicate that these melts are

excessively depleted in trace elements such as REEs,

Nb, Rb, Zr, Th, U, and Y, to be the equivalent of granite

plutons and batholiths in the upper crust (Bea 1996a;

Sawyer 1996; Sheppard et al. 2003).

The behaviour of Na, K, and Rb is quite sensitive to

the proportions of main minerals such as biotite,

Fig. 8. Continental crust normalized REE plots of Chah-Bazargan batholith

samples. a — Normalized REE diagram of peraluminous granites;

b — Normalized REE diagram of metapelitic migmatitic xenoliths;

c — Normalized REE diagram of schist xenoliths; d – Normalized REE

diagram of metapelites from the Qori metamorphic complex. Normalization

values after Taylor & McLennan (1985).

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muscovite and K-feldspar in the residue (diatexitic migma-

tites). Abundance of these minerals in the source increases the

bulk partition coefficients of the elements. Furthermore,

decreases of these coefficients with increased degrees of mel-

ting would indicate that muscovite and less biotite would

become unstable phases during partial melting of the source.

Considering more incompatible elements such as La, Ce,

and Sm and compatible element Cr indicates that relatively

moderate degrees (between 20 and 30 %) of partial melting

are permissible (Table S8). Concentrations of LREEs such as

La, Ce, and Nd and Cr in geochemical modelling of the

migmatitic xenoliths (C

) demonstrate that degrees of partial

Fig. 9. Schematic model of the most important processes described in the Chah-Bazargan pluton. a — Schematic Figure which graphically

summarizes the relationships between paleosome, melanosome, and neosome. b — Schematic relationships in the metatexites including

representations of patch dilation, net, and stromatic structures. c — Schematic relationships in the diatexite including nebulitic, schollen, and

schlieren structures. Figures (b) and (c) were plotted base on Figure 2.

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melting between 20 and 30 % cause contents of these elements

to be similar to the average of the observed concentrations of

the elements (Table 2).

Partial melting of pelitic metasediments around the south-

west contact of the Chah-Bazargan complex is a possible indi-

cation of advective heating as well as conductive transfer of

heat by quartz diorite (Fig. 9). Balanced in situ crystallization,

reactions between restite (mesosome) and melt (leucosome),

and the adhesion force between melt (leucosome) and crystal

(melanosome) prevent the melt separating from migmatitic

xenoliths (Figs. 2, 3). Additionally, high viscosity of the magma

and low temperature of the partial melting in the source were

other important factors inhibiting melt extraction. It should be

noted that mingling of some parts of peraluminious melt with

quartz dioritic magma is possible (Fig. 9).

The volumes of peraluminous granite patches within the the

Chah-Bazargan quartz-diorite intrusion are between several

tens of centimetres to several tens of cubic metres. The patches

are near or adjacent to the swarms of the migmatitic xenoliths.

The aggregated migmatitic xenoliths are between several tens

of centimetres to several metres across. Therefore, the maxi-

mum temperature of Chah-Bazargan intrusion has easily

spread to the all parts of the xenoliths. Continuous injections

of new quartz-dioritic magma to the chamber may also have

served to maintain the high temperature. Convection and

movement of the quartz-dioritic magma were important fac-

tors in aiding the separation and exhaustion of the leucosome

components. As a result of processes, it is possible that only

20–30 vol. % of the melt could have left the migmatitic xeno-

liths and, so small patches of Chah-Bazargan peraluminous

granites could be produced (Fig. 9a). Because the thermal and

chemical composition of the melt was much different from the

quartz-dioritic melt, the felsic melt remained as patches and

did not mix into the quartz diorite.

Conclusion

Partial melting in the Chah-Bazargan metapelitic xenoliths,

which are incorporated into the Chah-Bazargan quartz dioritic

batholith (Fig. 9a) at 173 Ma, occurred at P and T conditions

higher than the minimum melting curve of granite

(ca. 4.5±1.0 kbar and 760±35 °C). A considerable volume of

leucosome was generated, mostly as a stromatic type (Fig. 9b).

Although these amounts of leucosomes do not represent

pure melts, but contain entrained solid (residual, i.e.

peritectic phases) material, textures and field relationships

suggesting that the melt fraction was substantial. Melting

reactions involved the incongruent breakdown of biotite.

A portion of the leucosome (appro ximately 20–30 vol. %)

was segregated from the diate

xitic migmatitic xenoliths

(Fig. 9c) during contact metamorphism and these amal-

gamated to produce small patches of the Chah-Bazargan

per aluminous granites. A large part of the partial melts

from migmatitic xenoliths could not be extracted due to

a combi nation of situ crystallization, the adhesion force

between melt and remaining crystal, and high viscosity of

the magma.

Geochemical modelling indicates that in REEs plots, per-

aluminous melts are excessively depleted in trace elements

such as REEs (La to Lu), HFSE (Ti, Zr, Ta, Nb, Th, U, Hf, Y),

Ba, Pb, and Sr in comparison with xenoliths of migmatite.

Furthermore, the modelling demonstrates that these elements

are very sensitive to source enrichment and the amounts of

major minerals such as garnet, biotite, muscovite, K-feldspar,

plagioclase, and ilmenite, and accessory minerals, such as

apatite, monazite, and zircon, in the residue of the diatexite

migmatites. Hence, a portion of these elements were hosted by

non-melted part of the mineral assemblage minerals consi-

dered before in the source (migmatitic xenoliths).

Acknowledgements: The authors would like to thank

Prof. Dr. Volker Schenk, Dr. Peter Appel, Mrs. Barbara Mader,

and Mrs. Astrid Weinkauf for their support during EMP and

XRF analyses at Kiel University. Financial support from the

Iranian Ministry of Science, Research and Technology, and

Universities of Kerman and Urmia (Iran) and Institute für

Geowissenschaften, Christian-Albechts-Universität zu Kiel

(Germany) are gratefully acknowledged. Last but not the least,

I would like to thank Prof. Robert J. Stern from the University

of Texas at Dallas for English and scientific editing the article.

This paper is dedicated to Afzalipour who founded Kerman

University.

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Supplementum

Fig. S1. Chemical compositions of garnet grains of metapelitic

xenoliths and peraluminous granites. a — Migmatitic xenolith;

b — Metapelitic xenolith without bands, pods and patches of

leucocratic quartzo-feldspathic melt (leucosome); c — peraluminous

granite patch in the Chah-Bazargan batholith.

Fig. S2. Discriminating diagram of biotite. Plot of Ti (per 11 oxygens)

asafunctionofFe/(Fe+Mg)forbiotitegrains(Robinson1991)from

different rock types. Number 187 is garnet-bearing peraluminous

granite. Numbers 264 and 272 are cordierite-bearing peraluminous

granite. Numbers 182-E2 and 189-E are migmatitic xenoliths.

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Fig. S3. Chemical composition of different rock types plagioclase. a — Quartz-diorite (Chah-Bazargan batholith); b — Contaminated quartz-

diorite. This picture suggests that magma mixing has occurred between quartz dioritic and peraluminous granitic melts; c — Migmatitic

xenolith; d — Peraluminous granite. Core of the grain is presumably a relic of the quartz-diorite and rim has been crystallized from the peralu-

minous granitic melt. Outer rim of the grain suggests that magma mixing has occurred between quartz dioritic and peraluminous granitic melts.

Fig. S4.ZirconiumcontentsagainstMindexdefinedascationratio(Na + K + 2Ca) /(Al * Si)fortheperaluminousgraniteoftheChah-Bazargan

batholith. Lines indicate zirconium saturation isotherms calculated following Watson & Harrison (1983).

iii

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Fig. S5. Continental crust normalized REE and multi-element plots for averages of samples of Chah-Bazargan batholith. a — Normalized REE

diagram; b — Normalized multi-element diagram. Normalization values after Taylor & McLennan (1985).

Table S1: Mineralogy and detailed mineral assemblage of all rock types of Chah-Bazargan, Talle-Pahlevani gabbroic intrusions and Qori
Barrovian-type metamorphic complex.

Minerals

Rock type

Metapelites

Metabasites

Qori Barrovian-type metamorphic

complex (QMC)

Biotite+Garnet+Kyanite+Plagioclase+

K-felspare+Quartz+Opaqueminerals

Hornblande+Garnet+Plasioclase+Quartz+

Biotite+Titanite

Rock type

Chah-Bazargan intrusions

Talle-Pahlevani intrusions

Chah-Bazargan quartz-dioritic and

Talle-Pahlevani gabbroic intrusions

Plagioclase, Quartz, Clinopyroxene, Titanite,

Opaque minerals

Plagioclase, Olivine, Clinopyroxene,

Hornblande, Biotite, Titanite,

Opaque minerals

Rock type

Peraluminous granites

Migmatitic xenoliths

Chah-Bazargan migmatitic xenoliths

and peraluminous granitic patches

Biotite, Muscovite, Plagioclase, K-felspare,

Quartz, Cordierite, Opaque minerals,

Sillimanite, Tourmaline

Biotite+Plagioclase+K-felspare+Quartz+

Cordierite+Garnet+Opaqueminerals+

Sillimanite

Biotite, Muscovite, Plagioclase, K-felspare,

Quartz, Opaque minerals, Garnet, Sillimanite,

Tourmaline, ±Cordierite,

Biotite+Plagioclase+K-felspare+Quartz+

Cordierite+Opaqueminerals+

Sillimanite+Spinel±Garnet

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Table S2: Detailed petrographic observations of all rock types in the Chah-Bazargan intrusion.

Mineral

phase

Qtz

Chl

Grt

Sil

And Crd

Hbl Cpx Tou

Ilm Ore

Sample

Enclave

AF-180-E1

N 29 42 07 E 54 37 08

A I

AF-180-E2

29 42 07

54 37 08

A I

AF-180-E3

29 42 07

54 37 08

A I

AF-180-E4

29 42 07

54 37 08

A I

AF-181-E2

29 30 17

54 37 33

A I

X S

AF-181-E4

29 30 17

54 37 33

X I

A I

X I

AF-182-E1

29 38 45

54 38 51

A I

AF-182-E2

29 38 45

54 38 51

X I

A I

X S I

AF-184-E1

29 38 15

54 40 53

A I

A S I

AF-184-E2

29 38 15

54 40 53

A I

AF-185-E1

29 38 14

54 44 05

A I

AF-185-E2

29 38 14

54 44 05

A I

X I

AF-185-E3

29 38 14

54 44 05

A I

X I

AF-188-E1

29 38 49

54 39 01

A I

AF-188-E2

29 38 49

54 39 01

A I

AF-188-E3

29 38 49

54 39 01

A I

AF-188-E3

Xenocryst in enclave

AF-188-E4

29 38 49

54 39 01

A I

AF-189-E1

29 38 46

54 39 03

A I

AF-191-E

29 42 50

54 42 07

A I

AF-B-7-a

29 42 29

54 44 16

X I

A I

X I

AF-B-7-b

29 42 29

54 44 16

X I

A I

AF-B-7-c

29 42 29

54 44 16

A I

AF-B-10

29 41 55

54 43 27

A I

AF-B-7-e

29 42 29

54 44 16

A I

AF-269-f

29 38 43

54 39 07

A I

A S

AF-B-7

29 42 29

54 44 16

A I

AF-B-4

Uneqilibrium enclave

A I

29 42 08

54 45 23

AF-6

Dioritic enclave

A I

29 42 14

54 42 59

Chah-Bazargan intrusion

AF-B-8-a

29 42 27

54 44 14

A I

AF-B-1-b

29 42 11

54 45 33

AF-269-a

29 40 14

54 38 48

AF-265

29 39 46

54 39 17

A I

A S

AF-269-c

29 38 43

54 39 06

X I

A I

A S

AF-269-e

29 38 43

54 39 06

A I

X S

AF-271

29 38 47

54 38 25

X I

A I

X S

AF-194-d

29 39 38

54 42 26

A I

A S

Peraluminous granite from Chah-Bazargan intrusion

AF-140-1

29 42 18

54 39 47

A I

AF-187

29 41 08

54 41 04

A I

AF-190-B

29 42 49

54 42 08

A I

AF-189-E

29 38 46

54 39 03

A I

AF-260

29 39 49

54 39 21

A I

AF-264

29 39 50

54 38 14

A I

AF-272

29 38 48

54 38 26

A I

Mineral Abbreviations: are from Kretz 1983.
Marked Abbreviations are: A — accessory and minor phase in matrix phase, I — inclusion in one mineral, R — relict phase, S — secondary phase, X — matrix phase.

FAZLNIA

GEOLOGICA CARPATHICA

, 2017, 68, 5, 445–463

Table S3: Chemical compositions of plagioclase, biotite, muscovite, garnet, K-feldspar, cordierite and spinel. Notes: Granite: Per-aluminous

granite; Xeno: xenolith; Inn R: Inner rim; Out R: Outer rim; Anor: anorthosite; Cont: contaminated leuco-quartz diorite-anorthosite; Mat: matrix

Sample

269-f 269-f B-7-b B-7-b

272

273

273 B-1-b B-1-b

Mineral

Type of rock Xeno Xeno Xeno Xeno Granite Granite Granite Cont Cont Anor Anor

Rim Core Rim Core Out r Inn r

Core

Rim Core Rim Core

SiO

64.56 59.74 59.56 55.09 62.49

66.33

61.17 63.65 56.42 58.33 55.96

22.66 25.90 25.63 28.37 23.42

20.43

24.09 23.25 28.47 25.92 27.32

0.09

0.17

0.04

0.00

0.18

0.00

0.11

0.06

CaO

3.11

6.75

6.37

9.83

4.50

1.36

5.76

3.99

9.83

7.78 10.01

9.72

7.54

7.72

5.82

8.78

10.82

8.23

9.46

5.96

6.99

5.79

0.08

0.17

0.09

0.32

0.15

0.25

0.18

0.12

0.20

0.12

BaO

0.03

0.02

0.04

0.00

0.01

0.05

0.02

0.00

Total

100.25 100.13 99.66 99.24 99.55

99.10

99.55 100.73 100.82 99.33 99.25

2.84

2.66

2.50

2.78

2.94

2.73

2.80

2.51

2.62

2.53

1.17

1.36

1.35

1.52

1.23

1.07

1.27

1.20

1.50

1.37

1.46

Total

4.01

4.00

4.01

4.00

3.99

0.00

0.01

0.00

0.01

0.00

0.15

0.32

0.31

0.48

0.21

0.06

0.28

0.19

0.47

0.38

0.49

0.83

0.65

0.67

0.51

0.76

0.93

0.71

0.81

0.52

0.61

0.51

0.00

0.01

0.02

0.01

0.00

Total

0.98

0.99

1.00

1.01

0.99

1.00

0.15

0.33

0.31

0.48

0.22

0.06

0.28

0.19

0.47

0.38

0.48

0.85

0.67

0.68

0.51

0.77

0.93

0.71

0.80

0.52

0.61

0.51

Kfs

0.00

0.01

0.02

0.01

Sample

269-f

B-7-b

182-E2

Mineral

Grt

Type of rock

Xeno

Rim

Core

Rim

Core

Rim

SiO

37.21

37.12

36.41

36.49

37.55

TiO

0.03

0.01

0.03

0.04

21.00

20.92

20.99

21.18

21.08

FeO

33.68

36.72

28.35

29.97

35.33

MgO

2.26

2.67

1.64

2.03

3.02

MnO

5.34

1.85

10.89

8.36

2.53

CaO

1.02

0.90

1.09

1.26

1.28

Total

100.54

100.22

99.38

99.33

100.83

Structural formulae on a basis of 12 oxygens

3.00

2.98

3.00

2.00

1.99

2.03

2.04

1.99

0.00

2.27

2.48

1.94

2.05

2.36

0.27

0.32

0.20

0.25

0.36

0.37

0.13

0.76

0.58

0.17

0.09

0.08

0.10

0.11

Total

8.00

Alm

0.76

0.83

0.65

0.69

0.79

Prp

0.09

0.11

0.07

0.08

0.12

Sps

0.12

0.04

0.25

0.19

0.06

Grs

0.03

0.04

0.89

0.91

0.89

0.87

Sample

187

264

272

182-E2

Mineral

Kfs

Type of rock

Granite

Xeno

SiO

64.94

65.18

64.98

64.57

19.26

18.87

18.48

18.98

0.07

0.00

0.05

CaO

0.05

0.00

0.04

0.02

1.78

1.67

1.50

1.37

14.48

15.09

14.91

15.11

BaO

0.22

0.04

0.37

Total

100.81

100.85

100.01

100.46

Structural formulae on a basis of 8 oxygens

2.97

2.98

2.99

2.97

1.04

1.02

1.00

1.03

Total

4.00

0.00

0.16

0.15

0.13

0.12

0.84

0.88

0.89

0.00

0.01

Total

1.01

1.03

1.01

5.02

0.00

0.16

0.14

0.13

0.12

Kfs

0.84

0.86

0.87

0.88

Sample

269-f

B-7-b 182-E2

269-f

B-7-b

Mineral

Type of rock Xeno

Xeno

Mat

SiO

34.61

35.03

34.18

46.22

45.23

TiO

1.96

2.93

3.03

0.43

0.41

19.62

19.41

19.80

36.21

35.83

FeO

22.05

20.43

23.57

0.76

0.92

MgO

7.35

7.14

6.49

0.42

0.55

MnO

0.12

0.34

0.19

0.03

0.00

0.11

0.18

0.10

1.22

0.71

9.36

9.74

9.65

9.86

11.09

Total

95.18

95.19

97.00

95.15

94.74

5.35

5.38

5.23

6.13

6.08

2.66

2.62

2.77

1.87

1.92

0.92

0.90

0.81

3.79

3.75

0.23

0.34

0.35

0.04

2.85

2.63

3.02

0.08

0.10

1.69

1.64

1.48

0.08

0.11

0.02

0.04

0.02

0.00

0.03

0.05

0.03

0.31

0.18

1.85

1.91

1.88

1.67

1.90

Total

15.58

15.50

15.59

13.99

14.09

0.63

0.62

0.67

0.50

0.49

THE CHAH-BAZARGAN PERALUMINOUS GRANITES — PETROLOGICAL CONDITIONS

GEOLOGICA CARPATHICA

, 2017, 68, 5, 445–463

Table S3 continuation: Chemical compositions of plagioclase, biotite, muscovite, garnet, K-feldspar, cordierite and spinel. Notes: Granite:

Per-aluminous granite; Xeno: xenolith; Inn R: Inner rim; Out R: Outer rim; Anor: anorthosite; Cont: contaminated leuco-quartz diorite-

anorthosite; Mat: matrix

Sample

181-E

182-E2

264

Mineral

Crd

Type of rock

Xeno

Granite

SiO

48.31

48.18

48.21

TiO

0.00

33.05

33.12

33.16

FeO

10.39

11.92

11.89

MgO

6.36

6.08

5.97

MnO

0.31

0.36

CaO

0.02

0.03

0.00

0.34

0.13

0.15

0.00

0.01

Total

98.77

99.82

99.75

basis of 18 oxygens

5.00

4.97

4.98

1.00

1.03

1.02

3.04

3.00

3.01

0.00

Total

3.04

3.00

3.01

0.90

1.03

0.98

0.94

0.92

0.03

Total

1.91

2.00

1.98

0.00

0.07

0.03

0.00

Total

0.07

0.03

0.48

0.52

0.53

Sample

182-E2

187

Mineral

Spl

Type of rock

Xeno

Granite

SiO

0.05

0.01

TiO

0.02

0.01

58.34

58.77

59.34

0.40

0.35

0.12

1.34

0.58

0.02

FeO

35.81

35.49

35.73

MgO

1.64

1.93

2.12

MnO

0.44

0.39

0.25

ZnO

3.28

3.02

2.45

Total

101.30

100.60

100.06

basis of 32 oxygens

0.01

0.00

15.67

15.81

15.97

0.07

0.06

0.02

0.23

0.10

0.00

Total

15.99

16.00

6.82

6.77

6.82

0.56

0.66

0.72

0.08

0.05

0.55

0.51

0.41

Total

8.01

8.00

0.93

0.91

0.90

0.00

Table S4: Temperatures estimated from different thermometers. Abbreviations are: B92-HW and B92-GS: Bhattacharya et al. (1992);

Dasg91: Dasgupta et al. (1991); FS78: Ferry & Spear (1978); HS82: Hodges & Spear (1982); PL83: Perchuk & Lavrent’eva (1983); T76:

Thompson (1976); HL77: Holdway & Lee (1977); GS97: Gessmann et al. (1997); KM04-Bt-Grt and KM04-Crd-Grt: Kaneko & Miyano

(2004).

Sample

kbar

B92-HW B92-GS

Dasg91

FS78

HS82

PL83

T76

HL77

GS97 KM04-Bt-

Grt

KM04-

Crd-Grt

269-f

624

623

540

659

670

626

662

633

640

645

625

B-7-b

560

522

521

613

628

602

627

603

605

590

−

182-E2

706

701

658

827

842

705

782

734

785

780

745

269-f

623

622

535

655

666

624

654

629

636

643

620

B-7-b

559

521

516

609

624

600

619

599

601

588

−

182-E2

706

700

652

822

837

702

774

730

778

740

269-f

622

621

530

651

661

621

647

626

632

641

615

B-7-b

558

520

511

605

620

597

612

596

595

586

−

182-E2

705

699

646

817

833

698

765

726

773

786

735

269-f

622

620

525

647

657

618

639

622

628

639

610

B-7-b

558

519

507

601

616

594

605

592

590

584

−

182-E2

704

698

640

812

828

695

756

722

770

784

730

269-f

621

620

520

642

653

615

631

619

624

637

605

B-7-b

557

518

502

597

612

591

597

589

585

582

−

182-E2

703

697

634

807

823

692

748

718

767

782

725

vii

FAZLNIA

GEOLOGICA CARPATHICA

, 2017, 68, 5, 445–463

Table S5: Pressures estimated from different baro-

meters. Abbreviations are, HS82: Hodges & Spear

(1982); WU04: Wu et al. (2004); Ave: average of

pressure.

Sample

ºC

HS82

WU04

Ave

269-f

~640

1.6

2.5

2.1

B-7-b

~590

1.4

1.9

1.7

182-E2

~760

4.5

5.0

4.8

Average of

metapelites and

xenoliths

Average of

migmatitic

xenoliths

n=10

n=3

Table 2

210.27

214.13

65.21

96.25

67.10

75.24

2.42

1.94

12.71

16.19

26.70

23.77

190.30

256.33

53.82

38.45

30.02

40.65

56.65

80.54

7.37

9.98

27.67

36.35

6.62

6.74

1.10

0.76

7.53

6.49

1.56

1.13

10.20

7.54

2.22

1.60

6.42

4.36

0.96

0.66

6.38

4.35

0.94

0.66

69.61

109.16

31.37

67.53

1007

611

8773

17647

101.97

196.88

13.47

21.34

7.55

7.06

2.20

2.18

21.57

16.06

Table S6: Geochemical averages for selected

metapelites and xenoliths without migmatitic texture

and migmatitic xenoliths from the Chah-Bazargan

batholith listed in Table 2.

Table S7: Calculated bulk partition coefficients (Kd) with 1 %, 5 %, 10 %,

20 %, 30 %, 40 %, and 50 % partial melting for selected Chah-Bazargan

migmatitic xenoliths.

Source Tables 1 and 2.

0.5

0.05

Value

0.05

0.1

0.2

0.3

0.4

0.5

1.56

1.22

1.10

1.06

1.05

1.04

0.66

−0.18

−0.45

−1.63

−13.33

5.16

2.82

−15.35

−0.86

−12.33

2.18

1.56

1.37

1.28

−1.48

0.17

0.29

0.45

0.55

0.62

0.67

3.95

−0.30

−0.87

−13.22

3.53

2.16

1.76

−5.80

0.29

0.45

0.62

0.71

0.76

0.80

2.78

−0.24

−0.63

−3.47

7.07

2.81

2.06

−8.56

0.11

0.20

0.33

0.43

0.50

0.56

5.00

−0.24

−0.62

−3.26

7.76

2.88

2.10

−8.86

−0.20

−0.51

−2.07

71.09

3.87

2.46

−12.13

−0.24

−0.62

−3.22

7.91

2.90

2.10

−8.91

−0.26

−0.72

−5.16

4.90

2.48

1.91

−7.22

1.57

1.22

1.10

1.06

1.05

1.04

0.66

0.10

0.18

0.31

0.40

0.47

0.52

5.28

0.24

0.38

0.55

0.65

0.71

0.76

3.19

0.12

0.21

0.35

0.45

0.52

0.57

4.84

0.12

0.22

0.36

0.46

0.53

0.59

4.73

0.11

0.20

0.34

0.43

0.51

0.56

4.94

0.10

0.17

0.30

0.39

0.46

0.51

5.38

0.10

0.18

0.30

0.40

0.47

0.52

5.30

0.10

0.18

0.30

0.39

0.46

0.52

5.34

0.10

0.19

0.32

0.41

0.48

0.54

5.15

−0.16

−0.38

−1.23

−4.81

10.63

3.63

−22.69

−0.10

−0.23

−0.60

−1.27

−2.95

−14.09

136.81

0.07

0.13

0.24

0.32

0.38

0.43

6.09

−0.11

−0.25

−0.66

−1.48

−3.89

−176.25

1596.25

−0.12

−0.26

−0.71

−1.65

−4.87

27.92

−241.25

−0.16

−0.37

−1.18

−4.34

12.94

3.82

−24.37

0.42

0.59

0.74

0.81

0.85

0.88

2.09

0.84

0.91

0.95

0.97

0.98

1.17

0.13

0.23

0.37

0.47

0.54

0.59

4.66

viii

THE CHAH-BAZARGAN PERALUMINOUS GRANITES — PETROLOGICAL CONDITIONS

GEOLOGICA CARPATHICA

, 2017, 68, 5, 445–463

Table S8: Calculated bulk partition coefficients (Kd) for each mineral based on partition coefficients (mineral/granitic peraluminous melt) after

Nash & Crecraft (1985), Sisson & Bacon (1992), Bea et al. (1994), and Keskin' software (2002).

Element

=D × C

/(ƒ+D(1-ƒ))

(Grt) (Bt-Ms) (Kfs)

(Pl)

(Crd)

(Ap)

(Zr)

(Ilm)

0.01

0.05

0.10

0.20

0.30

0.40

0.50

0.001

0.06

1.01

4.61

0.06

456

1.30

7.1

11.4

5.9

30.02 −30.4 −31.9 −34.0 −39.2 −46.2 −56.4 −72.2

0.01

0.05

0.86

3.87

0.07

569

2.04

7.8

13.9

7.1

56.65 −57.3 −60.1 −63.9 −73.4 −86.1 −104.1 −131.8

0.4

0.08

0.51

2.56

0.09

855

3.35

7.6

20.4

10.2

27.67 −28.0 −29.3 −31.1 −35.5 −41.3 −49.4 −61.4

6.4

0.06

0.42

1.45

0.10

1105

3.79

6.9

26.6

13.0

6.62

−6.69 −6.99 −7.41 −8.43 −9.77 −11.62 −14.34

9.3

0.05

2.32

2.99

0.01

23.8

0.45

2.5

2.4

1.1

1.10

−1.13 −1.22 −1.36 −1.78 −2.56 −4.55 −20.68

3.7

0.10

0.60

2.05

0.29

2133

9.21

0.00

50.0

24.0

7.53

−7.61 −7.94 −8.41 −9.51 −10.95 −12.91 −15.72

140

0.12

0.64

0.82

1.77

2216

278

4.1

68.2

30.3

6.38

−6.45 −6.73 −7.11 −8.04 −9.24 −10.87 −13.20

0.2

0.96

1.32

4.43

2981

923

3.6

76.4

37.4

0.94

−0.95 −0.99 −1.04 −1.18 −1.35 −1.59 −1.93

130

0.1

0.5

0.78

0.72

162

71.4

0.20

19.3

6.6

53.82 −54.5 −57.1 −60.8 −69.9 −82.3 −99.8 −127.0

42.3

1.15

0.31

0.92

0.00

119.0

15.8

16.9

69.61 −70.4 −73.5 −77.9 −88.3 −102.0 −120.8 −148.0

0.05

24.50

0.27

0.04

0.01

0.00

11.6

8.8

9.9

26.70 −27.0 −28.2 −30.0 −34.2 −39.9 −47.7 −59.4

Note: D

=11.60%Grt+34.80%Bt-Ms+11.6%Kfs+13.9%Pl+23.2%Crd+2.3%Ap+0.1%Zr+2.3%Ilm;

=3.3%Grt+38%Bt+4.4%Kfs+9.8%Pl+38%Crd+1.1%Ap+0.1%Zr+5.3%Ilm

Element

=D × C

/(ƒ+D(1-ƒ))

(Grt) (Bt-Ms) (Kfs)

(Pl)

(Crd)

(Ap)

(Zr)

(Ilm)

0.01

0.05

0.10

0.20

0.30

0.40

0.50

0.001

0.06

1.01

4.61

0.06

456

1.30

7.1

11.4

5.9

30.02 −30.4 −31.8 −33.7 −38.4 −44.6 −53.1 −65.8

0.01

0.05

0.86

3.87

0.07

569

2.04

7.8

13.9

7.1

56.65 −57.3 −59.9 −63.4 −72.1 −83.5 −99.2 −122.0

0.4

0.08

0.51

2.56

0.09

855

3.35

7.6

20.4

10.2

27.67 −28.0 −29.2 −30.9 −35.0 −40.4 −47.7 −58.2

6.4

0.06

0.42

1.45

0.10

1105

3.79

6.9

26.6

13.0

6.62

−6.68 −6.98 −7.38 −8.35 −9.60 −11.31 −13.75

9.3

0.05

2.32

2.99

0.01

23.8

0.45

2.5

2.4

1.1

1.10

−1.12 −1.19 −1.29 −1.54 −1.92 −2.55 −3.80

3.7

0.10

0.60

2.05

0.29

2133

9.21

0.00

50.0

24.0

7.53

−7.61 −7.94 −8.39 −9.46 −10.85 −12.72 −15.37

140

0.12

0.64

0.82

1.77

2216

278

4.1

68.2

30.3

6.38

−6.45 −6.72 −7.10 −8.00 −9.17 −10.74 −12.95

0.2

0.96

1.32

4.43

2981

923

3.6

76.4

37.4

0.94

−0.95 −0.99 −1.04 −1.18 −1.35 −1.58 −1.90

130

0.1

0.5

0.78

0.72

162

71.4

0.20

19.3

6.6

53.82 −54.4 −56.8 −60.2 −68.2 −78.6 −92.9 −113.5

42.3

1.15

0.31

0.92

0.00

119.0

15.8

16.9

69.61 −70.4 −73.5 −77.9 −88.4 −102.2 −121.1 −148.6

0.05

24.50

0.27

0.04

0.01

0.00

11.6

8.8

9.9

26.70 −27.0 −28.3 −30.0 −34.3 −40.1 −48.1 −60.2

Note: D

=11.60%Grt+34.80%Bt-Ms+11.6%Kfs+13.9%Pl+23.2%Crd+2.3%Ap+0.1%Zr+2.3%Ilm;

=3.3%Grt+38%Bt+4.4%Kfs+9.8%Pl+38%Crd+1.1%Ap+0.1%Zr+5.3%Ilm