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, OCTOBER 2015, 66, 5, 361—374 doi: 10.1515/geoca-2015-0031
Introduction
Significant volumes of magma-derived rocks in the continen-
tal crust are represented by granite. Many different types of
granite have been recognized based on their bulk composi-
tions, their mineral assemblages, and the tectonomagmatic
settings in which they occur (Chappell & White 1984; Bar-
barin 1999; Patiño Douce 1999 and others). One of these
granite types is the peraluminous (corundum-normative) leu-
cocratic granites-granodiorites (leucogranites) which are char-
acterized by primary muscovite and biotite, with minor garnet,
rare cordierite, and very rare andalusite, all of which have
been used as significant indicators of pressure of crystalliza-
tion (Cawthorn et al. 1976; Green 1978; Clark et al. 2005,
2007). Besides muscovite, cordierite, garnet and Al
2
SiO
5
polymorphs or feldspars, biotite is the most important alu-
minium concentrator and in biotite-dominated granitoids it
directly determines the peraluminosity of magma (Zen 1988;
Shabani et al. 2003; Bonova et al. 2010). Several possible
mechanisms have been proposed for the formation of these
rocks including amphibole fractionation from less siliceous
melt (Cawthorn et al. 1976), partial melting of pelitic metased-
iments (Green 1978), vapour phase transport of alkalies (Luth
et al. 1964), secondary alteration (Heming Carmichael 1973)
and magma contamination (Ewart Stipp 1968). Among these,
partial melting of pelitic metasedimentary rocks has attracted
significant attention. According to several workers (i.e. Miller
1985; Le Fort et al. 1987; White & Chappell 1988; Sylvester
1998; Searle et al. 2010), these rocks are believed to be de-
rived wholly or dominantly from the partial melting of
metasedimentary rocks, including pelitic rocks (meta-shales)
and quartzofeldspathic psammitic rocks (meta-greywackes)
Petrology and mineral chemistry of peraluminous Marziyan
granites, Sanandaj-Sirjan metamorphic belt (NW Iran)
ESMAIEL DARVISHI
1!
, MAHMOUD KHALILI
2
, ROY BEAVERS
3
and MOHAMMAD SAYARI
2
1
Department of Geology, Islamic Azad University, Aligoodarz branch, Aligoodarz, Iran;
!
geo.edarvishi@gmail.com
2
Department of Geology, University of Isfahan, Isfahan, Iran; mahmoudkhalili@yahoo.com; m.sayari@gmail.com
3
Department of Geological Sciences, Southern Methodist University, Dallas, USA; rbeavers@smu.edu
(Manuscript received November 7, 2014; accepted in revised form June 23, 2015)
Abstract: The Marziyan granites are located in the north of Azna and crop out in the Sanandaj-Sirjan metamorphic belt.
These rocks contain minerals such as quartz, K-feldspars, plagioclase, biotite, muscovite, garnet, tourmaline and minor
sillimanite. The mineral chemistry of biotite indicates Fe-rich (siderophyllite), low TiO
2
, high Al
2
O
3
, and low MgO nature,
suggesting considerable Al concentration in the source magma. These biotites crystallized from peraluminous S-type
granite magma belonging to the ilmenite series. The white mica is rich in alumina and has muscovite composition. The
peraluminous nature of these rocks is manifested by their remarkably high SiO
2
, Al
2
O
3
and high molar A/CNK ( > 1.1)
ratio. The latter feature is reflected by the presence of garnet and muscovite. All field observations, petrography, mineral
chemistry and petrology evidence indicate a peraluminous, S-type nature of the Marziyan granitic rocks that formed by
partial melting of metapelite rocks in the mid to upper crust possibly under vapour-absent conditions. These rocks display
geochemical characteristics that span the medium to high-K and calc-alkaline nature and profound chemical features
typical of syn-collisional magmatism during collision of the Afro-Arabian continental plate and the Central Iranian microplate.
Key words: Marziyan S-type granites, peraluminous mineral chemistry, partial crustal melting.
by the incongruent melting of muscovite and biotite in a pro-
cess called vapour-absent melting (Watt Harley 1993; Stevens
et al. 1997; Waters 2001; Taylor et al. 2010). In evolved conti-
nental crust, generated melts are felsic owing to derivation
from mainly meta-pelitic source rocks or extensive melt evolu-
tion during ascent. In some orogens there is evidence for either
wet melting (Harrison et al. 1998; Patiño Douce & Harris
1998; Guo & Wilson 2012) or input of mantle melts (Barbarin
1999; Soesoo 2000). In the Sanandaj-Sirjan metamorphic belt
of west Iran, many granitoid bodies intruded from Jurassic to
Cenozoic (e.g. Takin 1972; Berberian et al. 1982; Mohajjel et
al. 2003; Agard et al. 2011; Chiu et al. 2013; Sepahi et al.
2014). Among the intrusive complexes of the central SSZ, the
Marziyan granites (Fig. 1) are very poorly studied and mineral
chemistry, petrologic and geochemical data on these rocks are
scarce. The purpose of the work presented here is to describe
the field relationships, petrography, mineral chemistry and
geochemistry of the Marziyan granites, as well as discussing
their petrogenetic and tectonic significance in the light of the
regional framework of the Sanandaj-Sirjan Zone. The data
from this study will shed light on the petrogenesis of these
rocks and the mode of their emplacement.
Geological setting
The Marziyan granites are located in the north of Azna and
crop out in an area between the Marziyan and the Kolbor vil-
lages which cover an area of approximately 30 km
2
, between
N 33°312—33°382 and E 49°242—49°322. The Sanandaj-Sir-
jan Zone, in terms of structural framework, is known as an ac-
tive geological zone in Iran (Mohajjel et al. 2003) which has
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experienced different deformations, metamorphic and mag-
matic events since the Cenozoic time. Detailed geological data
from the area under study are scarce and are mainly limited to
reconnaissance reports. The Sanandaj-Sirjan Zone in the Azna
area is characterized by the predominance of metamorphic
rocks and the presence of several granite and leucogranitic
bodies. The metamorphic rocks are composed of various
meta-sedimentary assemblages from low to high metamor-
phic grade. The basement of the area (Fig. 1) is dominated
by the pre-Jurassic, low- to very low-grade metamorphic
rocks (June Complex – Mohajjel et al. 2003), such as meta-
volcanic and tuffs, meta-cherty limestone, meta-sandstone,
slates and phyllites (Hamedan Phyllites: Fig. 1). The intru-
sion of the Marziyan granites into the Hamedan Phyllites in
the Late Cretaceous-Eocene (Sahandi et al. 2007) gave rise
to low-grade thermal aureole (up to albite-epidote to horn-
blende-hornfels facies) (Fig. 2). Contact metamorphic rocks,
consisting of spotted schist, andalusite-garnet schist and
cordierite schist (hornfelses), are exposed only in the southern
portions of the pluton. The northern margin of the complex is
controlled by a fault system parallel to the contact where the
granite thrust over metamorphic rocks. Thus, the traces of
contact metamorphism have been obliterated. The presence of
mantle-derived materials emplaced as diabasic dykes into the
granites and metamorphic rocks contributed to the heat source
for the partial melting of the country rocks. From a tectonic
perspective, the deformational features (i.e. fault, joints, my-
lonitization, schistosity and veins of the Marziyan granites)
were exposed with two different trends: (a) the NW-SE trend;
a compressional trend, running parallel to the main Sanandaj-
Sirjan belt trend, (b) and the NE-SW trend: shear stresses after
collision (Mohajjel et al. 2003). The trend of elongation in the
granites studied is very similar to that of the faults and joints
in the country rocks. Therefore, the Marziyan granites were
likely emplaced during the major deformational event in the
area. The direction of mylonitization and elongated veins is
parallel to the direction of the schistosity in country rocks and
corresponding roughly to the main trend of the Sanandaj-Sir-
jan Zone. The feature infers a syn-deformational (syn-colli-
sion) emplacement of the Marziyan granites.
Analytical methods
About two hundred rock samples were collected from local-
ities scattered over the area of investigation. One-hundred and
fifty thin sections were studied by optical microscope. For
chemical analysis, approximately 1 kg of each sample was
crushed into smaller chips in a steel jaw crusher. Then chips
of the samples were pulverized below 200 mesh with a soft
iron shatter box. Bulk major, minor and trace element analy-
ses were conducted on 12 representative granitic samples
Fig. 1. Simplified geological map of the Marziyan granites (modified from Sahandi et
al. 2007).
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PETROLOGY OF PERALUMINOUS MARZIYAN GRANITES, SANANDAJ-SIRJAN BELT (NW IRAN)
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(Table 1). Whole-rock major oxides were analysed by using
X-ray fluorescence (XRF) spectrometry at the Southern Metho-
dist University, Dallas (USA) and trace elements including
rare earth elements (REE) data were acquired by Inductively
Coupled Plasma-Mass Spectrometry (ICP-MS) at the Labwest
Minerals Analysis Pty Ltd in Western Australia. The analy-
ses were carried out with a detection limit of 0.01—10 ppm
following lithium metaborate fusion method, using high
pressure digestion in microwave apparatus including HF.
The results are presented in Table 2. Major-element compo-
sitions of the biotite and muscovite minerals in selected
leucogranites were determined by wave length-dispersive
spectrometry using the Cameca JXA-8800 (WDS) microprobe
JEOL at Russian Government University. The operational
conditions were 20 kV, 12 nA specimen current. The analyti-
cal spot diameter was set between 3 and 5 mm, keeping the
same current conditions. Representative mineral analyses of
leucogranites are presented in Tables 3 and 4.
Petrography and field relations
Based on field studies as well as petrographic characteris-
tics, the Marziyan granites are mainly dominated by leuco-
granite to granite. The most abundant and characteristic rock
type of the Marziyan pluton is leucogranite which is scattered
in portions throughout the area and intruded into the
metapelites (Fig. 2a,b). Small volumes of mylonitized granite
are commonly present in the shear zones. The granites are
mainly coarse to medium grained, white to light grey and hyp-
idiomorphic granular (Figs. 2, 3). Mineralogically these rocks
are composed of quartz, K-feldspar, and plagioclase as well as
muscovite, biotite, garnet, tourmaline, minor sillimanite, apa-
tite and small amounts of zircon and monazite (Table 1). Al-
teration of biotite to chlorite and of feldspar to sericite is
dispersed throughout the rocks. These rocks have been vari-
ably subjected to deformation. The most deformed parts of the
granite are characterized by mineral orientation and quartz re-
crystallization, while the undeformed parts have poikilitic
K-feldspar and quartz enclosing biotite and plagioclase. Sub-
hedral granular texture with perthitic microcline are the com-
mon petrographic features of the rocks studied. The prevailing
textures of the rocks are granular porphyric, (with relatively
larger K-feldspar, tourmaline and garnet crystals), and cata-
clastic texture (crushed minerals such as tourmaline and gar-
net). Most of the coarse-grained granites show subsolvus
recrystallization, in terms of two separate feldspar crystalliza-
tions, containing both plagioclase and K-feldspar. Small shear
zones were well developed in some portions. They are a re-
sponse to regionally imposed stress. Field observations and
Fig. 2. Photographs showing field geological features of Marziyan granites that intruded in the metapelite rocks.
Sample Qz
Kfs
Pl Bt
Ms
Grt
Tur
Sill
Ap
Zr
Opq
S-20
33.2 28.5 27.2 3.9 4.2 0.8 – 0.8 0.9 0.3 0.5
M-4
32.4 33.1 24.1 1.9 2.7 2.6 –
– 0.6 0.2 0.4
M-13
31.3 27.2 32.3 3.4 2.1 0.2 –
– 0.8 0.8 0.7
M-40
38.1
21.4
31.4
0.2
2.4
–
4.6
–
1
0.2
0.4
Az-2
37.2 29.2 22.4 2.5 1.7 0.4 –
– 0.4 0.3 0.6
Az-8
39.2 29.1 27.2 2.1 2.2 0.5 –
– 0.5 0.2 0.3
Az-9
39.2 22.5 27.4 4.6 1.5 – 0.4 – 0.6 0.5 0.5
Az-10
38.8 28.5 25.2 3.2 2.3 0.5 –
– 0.6 0.2 0.8
Az-24
37.8 22.6 25.1 5.1 4.4 0.9 – 0.5 0.8 0.5 0.5
Sh-4
39.2 29.6 22.2 4.4 7.5 0.7 –
– 0.7 0.4 0.9
Sh-5
41.3 30.1 24.2 3.5 2.3 – 0.2 – 0.7 0.2 0.7
Sh-9
43.2 21.1 23.2 1.4 4.5 – 0.5 – 0.8 0.4 0.5
Table 1: Modal analyses of representative Marziyan granites (in vol. %).
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petrographic evidence such as the occurrence of muscovite
and garnet and the absence of hornblende and primary sphene,
strongly support the peraluminous (S-type) nature of the
Marziyan granites and an origin for these rocks derived from
partial melting of crustal protolith.
Discussion
Mineral chemistry
To determine the chemical composition of biotite and
muscovite in the studied samples, three fresh and representa-
tive samples from the granites under discussion were selected.
Table 2: Representative major element (wt. %) and trace element including REE (ppm) compositions of the Marziyan granites.
Sample
no.
S-20 M-4 M-13 M-40 Az-2 Az-8 Az-9 Az-10
Az-24 Sh-4 Sh-5 Sh-9
SiO
2
69.85 71.05 70.75 71.36 73.41 74.5
71.78 72.81 70.4
72.92 73.42 77.5
Al
2
O
3
18.5
16.03 15.46 17.52 15.05 14.05 17.12 15.12 18.4
15.08 15.17 14.64
CaO
0.75 1.05 1.4
0.9
0.38 0.4
0.35 0.6
0.83 0.51 0.4
0.3
K
2
O
4.38 5.98 4.6
2.9
4.5
5.12 3.1
5
3.6
5.3
5.8
3.83
Na
2
O
4.2
2.96 3.9
5
4.3
3.95 3.9
3.5
3.9
4.1
3.1
2.74
MgO
0.26 0.2
0.7
0.26 0.3
0.2
0.98 0.45 0.4
0.25 0.2
0.45
(Fe
2
O
3
)
tot
0.7
0.62 1.8
0.7
1.02 1
1.01 1.3
1.2
1.01 0.6
1.1
MnO
0.05 0.08 0.02 0.02 0.02 0.03 0.01 0.04 0.02 0.02 0.04 0.02
P
2
O
5
0.76 0.06 0.2
0.99 0.06 0.04 0.05 0.11 0.8
0.13 0.1
0.07
TiO
2
0.02 0.02 0.2
0.02 0.08 0.04 0.08 0.14 0.042 0.1
0.07 0.06
L.O.I.
1.05 0.96 0.98 1
0.75 0.63 0.92 0.93 0.86 0.8
0.8
0.5
Total
100.5
99.06 100.01 100.7
99.87 99.96 99.3
100
100.5
100.2
99.76 100.98
A/CNK
1.36 1.22 1.19 1.46 1.14 1.11 1.5
1.24 1.47 1.13 1.15 1.35
A/NK
1.5
1.4
1.35 1.69 1.21 1.15 1.57 1.34 1.67 1.3
1.2
1.62
Corundum
2.4
2.1
1.2
2.1
1.8
1.1
2.8
2.1
2.9
1.4
2.1
2.6
Ba
313
527
353
332
454
342
417
475
382
428
352
338
Sr
35
187
122
47
63
32
47
90
58
58
45
35
Rb
108
198
118
148
159
341
105
188
111
213
321
216
Cs
18
12
38
45
27
25
39
24
41
36
23
36
Zr
28
40
105
35
64
76
98
86
57
81
75
71
Y
19
25
29
8
18
21
26
15
18
27
16
14
Th
14
23
24
10
25
16
12
24
11
16
12
18
Ta
1.33 0.91 3
5.36 1.99 5.6
3.1
2.5
1.92 6.3
4.04 2.55
Ga
13
13.9
16
20
19
17
20
16
15
17
19
18.5
Nb
10
15
22
21
16
20
21
19
16
24
19
21
Ni
4
4
5
4
7
4
7
5
4
4
5
4
Pb
40
20.5
16.5
24
16.7
23.9
26
19
27
29
32
21
Hf
0.44 0.87 0.55 0.35 0.77 0.55 0.88 0.86 0.57 0.94 0.82 0.97
La
12.4
23
41.5
11
15
12.9
30
18
12
23.3
33
22
Ce
22.6
45
75.6
19
27.3
21.8
56.4
34.6
20.5
41.1
62
41.2
Pr
4
4.3
7.75 3.2
9.2
5.3
9.7
7.2
5.4
4.7
4.9
5
Nd
14.2
12.2
25
13.2
16.9
17
22.4
14.5
16.3
16.4
16.6
15.4
Sm
3.4
2.92 4.2
3.1
4.32 3.42 3.3
4.6
4.9
4.64 3.1
3.55
Eu
0.17 0.76 0.9
0.18 0.39 0.44 0.56 0.26 0.29 0.21 0.47 0.36
Gd
1.67 2.99 3.56 1.9
1.9
3.1
2.2
3.4
2.98 3.5
2.3
2.68
Tb
0.38 0.81 0.79 0.34 0.55 0.36 0.29 0.46 0.59 0.66 0.59 0.58
Dy
2.1
5.28 4.9
1.9
2.86 2.55 2.6
2.9
2.21 4.8
2.24 3.4
Ho
0.47 0.98 0.88 0.44 0.52 0.46 0.51 0.49 0.54 0.91 0.58 0.54
Er
1.43 2.9
2.1
0.95 0.69 0.63 0.72 0.79 0.66 2.5
0.99 0.81
Tm
0.39 0.71 0.55 0.27 0.44 0.28 0.35 0.26 0.5
0.6
0.34 0.32
Yb
1.8
4.1
3.2
1.5
2.8
2.56 1.98 2.4
2.42 4.2
1.9
1.87
Lu
0.27 0.68 0.56 0.24 0.48 0.45 0.19 0.46 0.63 0.58 0.33 0.29
ΣREE
65.28 106.96 171.49 57.22 83.35 71.25 131.2
90.32 69.92 108.1
129.34 97.94
Rb/Sr
3.3
1.1
0.97 3.2
2.6
10.7
2.2
2.1
1.9
3.7
7.1
6.2
Rb/Ba
0.35 0.38 0.33 0.45 0.35 1
0.25 0.6
0.3
0.5
0.91 0.64
Rb/Zr
3.9
4.95 0.99 4.3
2.5
4.5
0.97 2.2
1.95 2.63 4.3
3.1
Sr/Ba
0.11 0.36 0.35 0.14 0.14 0.1
0.11 0.19 0.15 0.14 0.13 0.11
Eu/Eu*
0.22 0.79 0.71 0.23 0.34 0.41 0.64 0.20 0.23 0.16 0.54 0.36
T
Zr
(
0
c)
671
688
753
684
723
731
779
748
730
735
740
755
Biotite
Biotite is a significant ferromagnesian mineral in most in-
termediate and felsic igneous rocks, and occurs, as a minor
phase in some mafic rocks. In the Marziyan granitic rocks,
biotite is the dominant ferromagnesian phase. Other mafic
minerals such as garnet, tourmaline, chlorite and ilmenite
may occur, but only in trace amounts. Petrographically, bio-
tites from the Marziyan granites differ in their pleochroic
scheme, some being pleochroic in shades of reddish brown
and some in bright fire-red (Fig. 3a,b). Representative elec-
tron microprobe analyses of the biotites from the studied
rocks are displayed in Table 3. The value of Fe
3+
is estimated
by the approach of Dymek (1983). According to classifica-
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tion of Deer’s (1996, 2001) diagram, the biotites of the
Marziyan pluton are classified as Fe-rich biotite (siderophyl-
litic) (Fig. 4). The Fe/(Fe + Mg) ratio in these phases is about
0.68. Nachit (1986) used mica composition in granitoids to
relate the magma types in which biotite crystallized. In the
Al (total) vs. Mg classification diagram, the nature of granitic
magmas was grouped into four types such as peraluminous,
calc-alkaline, sub-alkaline, and alkaline-peralkaline (Fig. 5a).
Biotites from the Marziyan granites are clustered in the pera-
luminous field (Fig. 5a). Igneous biotites can also provide
valuable petrogenetic information. Three general reviews on
Table 3: Representative electron microprobe analyses and the structural formula of biotites based on 11 atoms of oxygen.
Sample
no.
Sh-4 Sh-4 Sh-4 Sh-4 S-20 S-20 S-20 S-20 Az-24
Az-24
Az-24
Az-24
SiO
2
34.85
35.31
34.35 34.65
35.2
34.5
35.9
35.2
34.98
36.02
34.78
35.4
TiO
2
2.15
1.98
2.35 2.23
1.3
1.9
0.95
1.5
1.95
0.35
2.2
1.8
Al
2
O
3
17.97
18.22
17.86
18.2
18.6
18.3
19
18.1
18.1
20.46
17.36
17.53
FeO
tot
24.65
24.44
24.75
25.12
24.2
24
24.5
25
24.96
23.39
24.67
25.31
MnO
0.75 0.54 0.68 0.66 0.37 0.35 0.39 0.45 0.62 0.22 0.63 0.63
MgO
6.18
6.12
6.24
6.52
6.2
6.1
6.2
5.9
6.38
6.3
6.34
6.47
CaO
0.15 0.21 0.13 0.14 0.22 0.24 0.21 0.14 0.14 0.33 0.13 0.13
Na
2
O
0.02 0.01 0.07 0.03 0.04 0.02 0.06 0.02 0.05 0.09
0.1 0.01
K
2
O
9.64
9.15
9.35
9.58
9.2
9.65
8.9
9.45
9.51
6.4
9.47
9.55
Total oxide
96.36 95.98 95.75 97.13 95.33 95.06 96.11 95.76 96.69 93.56 95.68 96.83
Si
2.68 2.71 2.66 2.65 2.71 2.68 2.74 2.72 2.68 2.75 2.70 2.71
Al
iv
1.32 1.29 1.34 1.35 1.29 1.32 1.26 1.28 1.32 1.25 1.30 1.29
Al
vi
0.31 0.36 0.29 0.29 0.41 0.36 0.44 0.36 0.32 0.60 0.28 0.30
Ti
0.12 0.11 0.14 0.13 0.08 0.11 0.05 0.09 0.11 0.02 0.13 0.10
Fe
2+
1.55 1.56 1.51 1.51 1.51 1.51 1.52 1.56 1.56 1.45 1.55 1.59
Fe
3+
0.03 0.00 0.09 0.09 0.05 0.05 0.05 0.05 0.04 0.04 0.05 0.03
Mn
0.05 0.04 0.04 0.04 0.02 0.02 0.03 0.03 0.04 0.01 0.04 0.04
Mg
0.71 0.70 0.72 0.74 0.71 0.71 0.70 0.68 0.73 0.72 0.73 0.74
Ca
0.01 0.02 0.01 0.01 0.02 0.02 0.02 0.01 0.01 0.03 0.01 0.01
Na
0.00 0.00 0.01 0.00 0.01 0.00 0.01 0.00 0.01 0.01 0.02 0.00
K
0.95 0.90 0.92 0.93 0.90 0.96 0.87 0.93 0.93 0.62 0.94 0.93
Total
9.73 9.67 9.73 9.75 9.69 9.72 9.67 9.71 9.73 9.51 9.73 9.73
Mg/Mg+Fe
0.31 0.31 0.31 0.32 0.31 0.31 0.31 0.30 0.31 0.32 0.31 0.31
Sample
no.
Sh-4 Sh-4 Sh-4 Sh-4 S-20 S-20 S-20 S-20 Az-24
Az-24
SiO
2
45.12
44.89
45.5
46.1
45.8
46.5
47
6.11
45
46.13
TiO
2
1.08
1.12
1.03
1.01
1.05
0.9
0.9
0.02
0.09
0.01
Al
2
O
3
35.05
34.87
35.8
35.9
35.7
35.5
34.2
35.95
38.31
34.61
FeO
tot
1.82
1.76
1.92
1.99
1.89
2.45
1.9
2.61
1.08
2.28
MnO
0.06
0.05
0.07
0.07
0.07
0.09
0.01
0.08
0.01
0.01
MgO
0.36
0.24
0.28
0.35
0.25
0.49
0.49
0.47
0.11
0.98
CaO
0.05
0.05
0.04
0.04
0.04
0.03
0.01
0.09
0.11
0.07
Na
2
O
0.32
0.42
0.39
0.37
0.41
0.3
0.4
0.25
0.29
0.16
K
2
O
11.1
11.08
11.03
11.01
11.05
10.25
10.9
10.38
11.26
11.36
Total oxide
94.96 94.48 96.06 96.84 96.26 96.51 95.81 95.96 96.26 95.61
Si
3.04 3.04 3.03 3.04 3.04 3.07 3.12 3.06 2.97 3.09
Al
iv
0.96 0.96 0.97 0.96 0.96 0.93 0.88 0.94 1.03 0.91
Al
vi
1.82
1.82
1.83
1.83
1.83
1.82
1.80
1.87
1.96
1.82
Ti
0.05 0.06 0.05 0.05 0.05 0.04 0.04 0.00 0.00 0.00
Fe
2+
0.10 0.10 0.11 0.11 0.10 0.14 0.11 0.14 0.06 0.13
Fe
3+
0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00
Mn
0.00 0.00 0.00 0.00 0.00 0.01 0.00 0.00 0.00 0.00
Mg
0.04 0.02 0.03 0.03 0.02 0.05 0.05 0.05 0.01 0.10
Ca
0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.01 0.01 0.01
Na
0.04 0.06 0.05 0.05 0.05 0.04 0.05 0.03 0.04 0.02
K
0.95 0.96 0.94 0.93 0.94 0.86 0.92 0.88 0.95 0.97
Total
9.01
9.02
9.01
9.00
9.01
8.96
8.98
8.99
9.02
9.04
Mg/Mg+Fe
0.26 0.20 0.21 0.24 0.19 0.26 0.31 0.24 0.15 0.43
Table 4: Representative electron microprobe analyses and the structural formula of white micas based on 11 atoms of oxygen.
micas in igneous rocks are provided by Foster (1960) and
Speer (1984). Biotite specimens in granitic rocks show that
the chemical composition and the colour of this mineral
strongly reflect the tectonic origin of its host (Lalonde &
Bernard 1993). In the continental collision- related granites,
biotite is enriched in total Al and Fe and is Fe
3+
-poor, consis-
tent with anatexis or assimilation of a reduced metased-
imentary material. The bright red colour of biotite from
peraluminous collisional granitic plutons reflects a high total
Fe content with low Fe
3+
/(Fe
2+
+ Fe
3+
), and probably also the
presence of Ti
3+
. Trying to use biotite’s capability to deter-
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mine the magmatic series, Abdel-Rahman (1994) introduced
four efficient diagrams discriminating alkaline, calc-alkaline
and peraluminous (including S-type) natures. These diagrams
Fig. 3. Photomicrographs of representative samples from the Marziyan granites, (crossed nicols). a – the granites displaying subhedral
granular quartz with biotites, orthoclase, plagioclase; b – leucogranite containing biotite phenocrysts; c – muscovite granite containing
primary muscovite, quartz, plagioclase and K-feldspar granite; d – secondary muscovite with plagioclase. Qz – quartz, Bt – biotite,
Pl – plagioclase, Ms – muscovite, Kfs – K-feldspar (abbreviations from Whitney & Evans 2010).
Fig. 4. Diagram of Deer et al. (1996) indicates that analysed biotites
are siderophyllite.
identifying magmatic nature based on biotite chemistry for
the Marziyan granitic rocks are presented in Fig. 5b,c,d,e.
These diagrams clearly show that the parent magma of anal-
ysed biotites had peraluminous nature (Fig. 5b,c,d,e). Biotite
is also a very useful and suitable indicator of the oxidation-
reduction state in a melt (Wones & Eugster 1965; Burkhard
1993; Bonova et al. 2010). Biotites from the Marziyan gran-
ites have a FeO*/MgO ratio of 3—4, low TiO
2
and high
Al
2
O
3
(Fig. 6a), on the basis of this diagram all the studied
samples are plotted in ilmenite series (Ishihara 1977) indicat-
ing a reducing environment for the granites under discussion
(Karimpour et al. 2011). The Ti content of biotite is believed
to be dependent on the temperature of crystallization of bio-
tite and the oxygen fugacity (fO
2
) (Henry et al. 2005) and
possibly on the volatile content of the magma. Low Ti con-
tent correlates with low temperature of crystallization and
low oxygen fugacity (Henry et al. 2005). High Al
2
O
3
and
low TiO
2
values in the biotites of the area reflect geochemi-
cal features characteristic of ilmenite series of granites
(Fig. 6a,b). Biotites with high Al concentrations seem to be
characteristic of peraluminous granites (e.g. Clarke et al.
2005; Dahlquist et al. 2007) where they coexist with alumi-
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nous minerals. However, the most commonly invoked pro-
cess, and probably the one responsible for the bulk of peralu-
minous granites, is anatexis or assimilation of pelitic
metasediments (Chappell & White 1987). In the Marziyan
granites, biotites are enriched in total Al and Fe contents and
are consistent with anatexis or assimilation of a reduced
metasedimentary material. In the Fe
2+
-Fe
3+
-Mg diagram of
Wones & Eugster (1965), biotite composition from the
Marziyan granites defines a cluster falling on the quartz-
fayalite-magnetite (QFM) oxygen fugacity buffer (Fig. 6b).
A better evaluation of oxygen fugacity can be made from the
Fe/(Fe+Mg) ratio of the biotite by using the calibrated curves
of Wones & Eugster (1965) and Wones (1989) buffer (il-
menite granites).
Fig. 5. Discrimination magmatic series diagrams based on the bio-
tite
chemistry unanimously confirm the peraluminous nature of the
Marziyan granitic rocks. a – in pfu (Nachit 1986), b—e – in wt. %
(Abdel-Rahman 1994).
White mica
Two types of white mica (muscovite) are distinguished in
the samples studied: large euhedral to subhedral flakes white
mica and small flakes of secondary white mica unevenly dis-
persed in feldspar, rarely in biotite (Fig. 3c,d). The secondary
white mica contains less Mg, Fe, Ti and more Al (Fig. 7a).
The morphology of the primary white mica flakes; their rela-
tionships to other rock-forming minerals, as well as systematic
compositional difference from the secondary white mica sug-
gest a magmatic origin of the primary white mica (Fig. 3c,d).
According to the classification of micas into 6 end-members
(Dymek 1983), the analysed white micas are mostly repre-
sented by muscovite. White mica is the other sheet silicate
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Fig. 6. a – Al
2
O
3
—TiO
2
diagram after Karimpour et al. (2011),
b – Fe
2+
-Fe
3+
-Mg diagram of Wones & Eugster (1965). Biotites
from the Marziyan granites cluster near the QFM and ilmenite series.
Fig. 7. a – Composition of white micas in the triangular diagram
Mg, Ti, Na (data from Table 4). The limit between fields for sec-
ondary and primary micas is from Miller et al. (1981). Main inset
shows representative primary and secondary white micas in Marziyan
granite filled circles; b – Chemical compositions of muscovite
plotted on Mg + Fe- Al diagram showing strongly peraluminous and
muscovite component for Marziyan samples (Zane & Rizzo 1999).
present. Care was taken to determine whether it is of primary
or secondary origin, since primary white mica is widely held
to be an indicator of peraluminous magmas (Speer 1984).
Petrographic observations using the criteria of Miller et al.
(1981) suggest that both types of white mica are present in the
studied samples. Chemical analyses were made of presumed
primary white micas (Table 4), which fall in the appropriate
field of the Mg-Ti-Na diagram (Fig. 7a) according to the divi-
sion established by Miller et al. (1981). The analysed white
mica, according to classification of micas into 6 end-members
(Dymek 1983), are mostly composed of muscovite. As Fig. 7b
(Zane & Rizzo 1999), displays, the Marziyan samples fall in
the strongly peraluminous muscovite component field. They
are also distinctively Fe-rich, similar to those in typical S-type
granite and those reported by Clarke et al. (2005) as coexisting
with aluminous minerals. Thus, both textural and chemical
evidence indicates a primary origin for almost all the studied
white mica. The petrographic and compositional characteris-
tics of the Fe-rich white mica in the Marziyan granites
(Fig. 7b) indicate an origin by crystallization of primary mus-
covite from a peraluminous magma (Miller et al. 1981; Clarke
et al. 2005; Dahlquist et al. 2007).
Whole-rock geochemistry
Major element data
The chemical compositions of the Marziyan granites are
reported in Table 1. The SiO
2
contents of the representative
samples vary from 69.85 to over 77.5 wt. % CaO. The high
alumina content (Al
2
O
3
:
14.05—18.5 %) relative to alkalies
(Na
2
O: 2.7—5 % and K
2
O: 2.9—5.98 %) and calcium (CaO:
0.3—1.44 %) is reflected in a high percentage of normative cor-
undum and a high molecular ratio Al
2
O
3
/(CaO + Na
2
O+ K
2
O)
(A/CNK) (Fig. 8a). These rocks with low TiO
2
+Fe
2
O
3(tot)
+MgO
(0.76—2.53) can be classified as leucogranites. In the ternary
Ab-An-Or normative diagram (Barker 1979), the Marziyan
granitic rocks are classified as granite (Fig. 8b) and on the
MALI (Na
2
O + K
2
O—CaO) vs. SiO
2
diagram (Frost & Frost
2008) they fall in both granite and granodiorite fields
(Fig. 9a). Incidentally, samples with low FeO
tot
display broad-
ly magnesian character (Fig. 9b).
Trace element data
The Rb, Sr and Ba contents vary between 108—341, 32—187
and 313—527 ppm, respectively. The rocks with high Rb but
lower Zr, Sr and Ba are characterized by high Rb/Zr
(about 3), Rb/Ba ( > 0.25) and Rb/Sr (0.97—10.7) ratios. The
Marziyan granites show strong enrichment in alkalies and
!
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Fig. 9. Most of the Marziyan samples are located in the granite and
granodiorite areas on the MALI vs. SiO
2
diagram (a) and all have
magnesian character according to FeO
t ot
/(FeO
tot
+MgO) vs. SiO
2
diagram (b). (Frost & Forst 2008).
Fig. 8. a – A/NK—A/CNK diagram (Maniar & Piccoli 1989).
A/NK = molar ratio of Al
2
O
3
/[K
2
O + Na
2
O]; A/CNK = molar ratio of
Al
2
O
3
/[CaO + K
2
O + Na
2
O]); b – Normative albite (Ab)-anorthite
(An)-orthoclase (Or) contents of the Marziyan granites, compared
with experimentally generated melt compositions from metapelite
from the Himalayan belt (Patiño Douce & Harris 1998). The Ab-An-Or
classification for silicic rocks follows Barker (1979).
depletion in HFS elements (Fig. 10, Table 1). Low Zr values
of the rocks (28—105 ppm) are accompanied by low CaO
contents of the rocks (0.3—1.44). Spider diagrams for the
Marziyan granites, relative to primitive mantle (Fig. 10b),
are characterized by distinct negative anomalies for Nb, Sr, P
and Ti typical for upper crustal compositions (Rollinson
1993). Rb, Ba and Eu concentrations in the granites studied
are variable and suggest variations in the proportions of feld-
spar and mica retained in the residua. La and Ce concentra-
tions vary between 11—41.5 and 19—75.6 ppm, respectively.
The studied samples are enriched in LREE relative to HREE
(Fig. 11a). The Marziyan granites are characterized by nega-
tive Eu anomaly and Eu/Eu*(0.16—0.79) (Fig. 10a). Primi-
tive mantle normalized trace element spider diagrams show
(Fig. 10b) relatively high Cs, Rb, K, Th, U, Ba contents and
low Sr, Ti. The REE content varies between 58.22 and
171.49 ppm. REE-normalized patterns are distinctly more
enriched and fractionated for LREE [(La/Sm)
N
= 2.29—6.70]
than for HREE [(Gd/Yb)
N
= 0.6—1.16].
Petrology
Peraluminous leucocratic granites commonly make up rel-
atively small syn-collision to post-collision plutons (Le Fort
et al. 1987; Nabelek et al. 1992; Inger & Harris 1993). They
include two-mica and muscovite-garnet granites and do not
contain low-pressure, high-temperature mafic aluminous
minerals (e.g. cordierite) and aluminosilicates, which are re-
markable features of strongly peraluminous S-type granites
(Chappell & White 1974). Comparison of the Marziyan
granites with typical peraluminous leucocratic granites dem-
onstrates significant similarities in their geological, mineral-
ogical, mineral-chemistry and chemical properties. The
presence of primary muscovite, siderophyllite biotite, garnet,
tourmaline and minor sillimanite as well as the Na/K rela-
tionship and high molar A/CNK ratio can be used to infer the
S-type character of the Marziyan granites (Fig. 8a). More-
over, the studied rocks with La
N
(68), Yb
N
(9.96) and strong
negative Eu anomaly are clearly consistent with the values of
these elements in S-type leucogranites (La
N
< 100, Yb
N
< 10,
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Eu/Eu* < 0.5) (Williamson et al. 1996). Strong negative Eu
anomaly, as Cullers & Graf (1984) cited, may be related to
early fractionation of feldspar and/or melting of igneous
source rocks with negative Eu anomalies, or vapour-absent
melting masking the uncertainities of the feldspar/melt dis-
tribution coefficient for Eu (Harris & Igner 1992). As the
Marziyan granitic samples on the La/Sm-La diagram exhibit
(Fig. 11), these trace elements are more likely to be con-
trolled by partial melting rather than fractional crystalliza-
tion. On Rb/Ba vs. Rb/Sr diagram (Sylvester 1998), the
majority of the Marziyan samples as well as the Himalayan
granites are plotted in clay-rich sources and the lower plagio-
clase content field (Fig. 12b). High Rb/Sr ( > 0.97), medium
to high Rb/Ba ( > 0.25) and low Sr/Ba ( < 0.36) ratios of the
Marziyan rocks as well as low CaO, high K
2
O and high Rb
abundances imply metapelitic source rock melted in water-
undersaturated conditions as proposed by Harris & Inger
(1992) and McDermott et al. (1996). Due to involvement of
plagioclase, wet melting tends to generate a rather- calcic
melt, whereas melts originated during dehydration melting,
owing to involvement of only micas, have more alkali com-
position (Patiño Douce & Beard 1995). The melting with
added H
2
O will increase the CaO/Na
2
O ratios (0.1—0.36) of
peraluminous granites (Holtz & Johannes 1991). The role of
muscovite (or biotite) -breakdown in the source should be
apparent from strong peraluminosity (Whitney 1988). On
this account, the Hamedan phyllites, in the Sanandaj-Sirjan
metamorphic belt, can be regarded as the potential parental
materials for the Marziyan granites. The low CaO/Na
2
O in
these rocks could be the result of melting without H
2
O in
the parental sediments (e.g. Patiño Douce & Johnston 1991;
Patiño Douce & Beard 1995; Sylvester 1998). According to
Villaseca et al. (2009) the S-type leucogranites, and their
source rocks, are commonly depleted in REE and other “in-
compatible” elements (i.e. Zr, Hf and Y), relative to what
would be predicted from the source composition. The low
CaO and high SiO
2
contents of the Marziyan granitic rocks
accompanied by low Zr values (28—105 ppm) point to the
low degree of partial melting of the source. These data over-
lap with those of Himalayan S-type leucogranites presented
by Harris et al. (1990). S-type granites commonly character-
ized by low Zr content ( < 100 ppm; e.g. Scaillet et al. 1990)
because of low solubility of zircon in peraluminous melts
forming at relatively low ( < 800) temperature (Watson &
Harrison 1983). In the Ab-An-Or normative diagram
(Fig. 8b), the studied granitic samples lie in the granite field
and close to the composition of melts generated by dehydra-
tion melting of muscovite schist at 6 to 10 kbar (Patiño
Douce & Harris 1998). Different reactions have been pro-
posed for melting of continental crust: (a) vapour/fluid
present incongruent melting of muscovite at temperature of
about 700—800 °C (Thompson 1982); (b) vapour absent in-
congruent melting of muscovite at approximately 700—750 °C
(Harris et al. 1995); (c) fluid-absent melting of biotite after
dehydration of muscovite at temperatures >750 °C (Le Bre-
ton & Thompson 1988). All the mineralogical and geochem-
ical criteria are in favour of the generation of Marziyan
granites by fluid-absent melting at temperatures of about
700 °C to 800 °C and 6—10 kbars (Fig. 8b) during adiabatic
Fig. 10. a – Chondrite-normalized whole rock REE patterns for
the Marziyan Granites. The chondrite values are from Boyton (1984);
b – Primitive mantle-normalized trace element diagrams. Normal-
ization factors are from Sun & McDonough (1989).
Fig. 11. La/Sm-La diagrams (Jiang et al. 2005) for the Marziyan
Granites signify the partial melting for the evolution of magma.
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Fig. 12. a – Molar Al
2
O
3
/(MgO+FeOD) vs. molar CaO/(MgO+FeOD)
for determining the composition of partial melts obtained by dehy-
dration melting of various bulk compositions (Patiño Douce 1999);
b – Rb/Ba vs. Rb/Sr diagram from Sylvester (1998). Most Marziyan
samples plot in Clay-rich Sources and lower plagioclase content
field same Himalayan granites field.
decompression or shear heating, and are solely the result of
the breakdown of muscovite or biotite. Goswami et al.
(2009) and Bikramaditya et al. (2011) proposed that about
10 % leucogranite melts can be generated by fluid-absent de-
compression melting of pelitic sediments at a temperature of
around 750 °C and a pressure of 6 to 10 kbar. On the basis of
zircon saturation (Watson & Harrison 1983), the Marziyan
granites should have originated at approximately 750 °C
(Table 1) which is not sufficient to cross the biotite break-
Fig. 13. a – Rb/Zr vs. SiO
2
discrimination diagram (Harris et al. 1986); b – Ta vs. Yb diagram (Pearce et al. 1984) for the Marziyan Gran-
ites. Note that all samples of the Marziyan plot in the Syn-COLG field and same the Himalayan granites. VAG – volcanic arc granite,
WPG – within plate granite, ORG – oceanic related granite, Syn-COLG – syn-collision granite, Post-COLG – post collision granite.
down reaction (Goswami et al. 2009; Bikramaditya et al.
2011), more likely in a continent-continent collision setting
by partial melting of mid to upper crustal sediments
(Figs. 12, 13). In the opinion of Paul et al. (2010) crustal
thickening in the Sanandaj Sirjan Zone was extreme
> 50 km. On this account, thermal gradient has increased
during collision of the Afro-Arabian and Central Iranian
plates and the intrusion of Marziyan granitic rocks probably
occurred by partial melting of mid to upper crustal sediments
and ascended diapirically owing to their lower density and
existence in a compressional environment by a shear zone.
Conclusion
On the basis of field, mineralogical and chemical features
the Marziyan granites are S-type granites. These rocks con-
sist of quartz, K-feldspar, plagioclase, biotite and Al-rich
minerals (such as muscovite, garnet and minor sillimanite).
The biotites from the Marziyan granites are Fe-rich (sidero-
phyllite), with low TiO
2
, high Al
2
O
3
, and low MgO, suggests
considerable Al concentration in the source magma. These
biotites were crystallized from peraluminous S-type granitic
magma belonging to ilmenite series. The white micas are
alumina enriched and have muscovite composition. The per-
aluminous composition of these rocks is shown by their high
content of normative corundum (2.05), their high molar
A/CNK > 1.1 ratio and the occasional presence of Al-silicate
minerals (i.e. garnet, muscovite). The geochemical behav-
iour of some major and trace elements including their re-
markably low CaO contents, CaO/Na
2
O ratios (0.1—0.36)
and negative Eu anomalies (0.44) generally serve as useful
keys to conclude that the melts must have originated under
vapour-absent conditions from a metapelitic source. The
Marziyan granites display geochemical characteristics that
span the medium to high K and calc-alkaline series and the
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principal features of syn-collisional magmatic intrusions re-
lated to an active continental margin. In the light of existing
data and on the basis of our observation, the origin of the
Marziyan granites, might have taken place in the course of
the collision of the Afro-Arabian continental plate and the
Central Iranian microplate.
Acknowledgment: The authors would like to thank Dr Mohs-
sen Tabatbai Manesh for conducting microprobe analyses at
the Russian Government University. Financial support of the
University of Isfahan is highly acknowledged. The authors are
also very grateful to the reviewers for their constructive re-
views and suggestions that greatly improved the manuscript.
References
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