Arab J Geosci (2016) 9:287 DOI 10.1007/s12517-015-2124-9
ORIGINAL PAPER
Calk-alkaline magmatism of Jebal-e-Barez plutonic complex, SE Iran: implication for subduction-related magmatic arc Jamal Rasouli 1 & Mansour Ghorbani 1 & Vahid Ahadnejad 2 & Giampiero Poli 3
Received: 15 March 2015 / Accepted: 10 September 2015 # Saudi Society for Geosciences 2016
Abstract The Uromia–Dokhtar Magmatic Arc (UDMA) is a northwest–southeast trending magmatic belt which is formed due to oblique subduction of Neotethys underneath Central Iran and dominantly comprises magmatic rocks. The Jebal-e-Barez Plutonic Complex (JBPC) is located southeast of the UDMA and composed of quartz diorite, granodiorite, granite, and alkali granite. Magmatic enclaves, ranging in composition from felsic to mafic, are abundant in the studied rocks. Based on the whole rock and mineral chemistry study, the granitoids are typically medium-high K calc-alkaline and metaluminous to peraluminous that show characteristics of I-type granitoids. The high field strength (HFS) and large ionic radius lithophile (LIL) element geochemistry suggests fractional crystallization as a major process in the evolution of the JBPC. The tectonomagmatic setting of the granitoids is compatible with the arc-related granitic suite, a pre-plate collision granitic suite, and a syncollision granitic suite. Field observations and petrographic and geochemical studies suggest that the rocks in this area are I-type granitoids and continental collision granitoids (CCG), continental arc granitoids (CAG), and island arc granitoid (IAG) subsections. The geothermobarometry based on the electron probe microanalysis of amphibole, feldspars, and * Jamal Rasouli
[email protected] 1
Faculty of Geology, Department of Earth Sciences, Shahid Beheshti University, Tehran, Iran
2
Department of Geology, Payame Noor University, P.O Box 19395-3697, Tehran, Iran
3
Department of Earth Sciences, University of Perugia, Perugia, Italy
biotite from selected rocks of JBPC implies that the complex formed at high-level depths (i.e., 9–12 km; upper continental crust) and at temperatures ranging from 650 to 750 °C under oxidation conditions. It seems that JBPC is located within a shear zone period, and structural setting of JBPC is extensional shear fractures which are product of transpression tectonic regime. All available data suggested that these granitoids may be derived from a magmatic arc that was formed by northeastern ward subduction of the Neotethyan oceanic crust beneath the Central Iran in Paleogene and subsequent collision between the Arabian and Iranian plates in Miocene. Keywords Uromia–Dokhtar Magmatic Arc . Central Iran . Neotethys . Magmatic arc . Jebal-e-Barez
Introduction The spreading and consequent subduction of the Neotethyan oceanic crust underneath Central Iran Block (CIB) have formed the first magmatic arc, which is the so-called Sanandaj–Sirjan Magmatic Arc (SSMA). The initiation of subduction dates back to Late Triassic– Early Jurassic (Berberian and Berberian 1981, Berberian and King, 1981). Subsequent closure of the ocean caused an oblique collision between two continental plates of the Neotethyan plate boundaries: Afro-Arabia (Gondwana) and CIB which are located in the south– southwest and north–northeast, respectively (Omrani et al, 2008). There are voluminous plutons intruded in the SSMA due to Neotethys subduction and later collision with ages ranging from 300 to 35 Ma (Sepahi et al. 2014). The recent studies show two intense magmatism
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periods of 180–140 and 60–35 Ma (Mazhari et al. 2009; Shahbazi et al. 2010; Ahadnejad et al. 2011; EsnaAashari 2012; Sepahi et al. 2014; Shahbazi et al. 2015). They consist of many granitoid intrusions that typically show calc-alkaline affinity. Compared with SSMA, the Urmia–Dokhtar magmatic arc (UDMA) is still poorly understood. The continued northward subduction of the Neotethyan crust beneath CIB induced a continental collision and produced the Andean-type UDMA (Dewey et al. 1973). There is no confirmed reason for dating collision between Arabia and Eurasia (McQuarrie et al. 2003); however, Agard et al (2011) report a resorption of the oceanic domain and collision after 35 Ma and before 25 Ma, respectively. McQuarrie and van Hinsbergen (2013) assessed the magnitude and locations of continental consumption which concluded ca. 27 Ma as an inception of collision age. The continuous calc-alkaline magmatism in the UDMA lasts from Eocene to the present (e.g., Berberian and King 1981; Bina et al. 1986) with peaks of Eocene and Upper Miocene to Plio-Quaternary (Agard et al. 2011). Despite the distribution of voluminous magmatic rocks in the UMDA, their tectonomagmatism characteristics remained poorly understood. Also, field observations revealed that more than 98 % of the known copper mineralization occurs within the interpreted alteration areas (Shahabpour 2007). Based on Cu mineralization and tertiary magmatic activity in the southeastern part of UDMA, the so-called Kerman Cenozoic Magmatic arc (KCM), Shafiei et al. (2009) reported two types of igneous rocks: (a) Barren rocks of pre-collisional Eocene–Oligocene arc diorites, quartz diorites, granodiorites, and their volcanic equivalents and b) collisional middle-late Miocene adakite-like porphyritic granodiorites without volcanic equivalents that are fertile and host some large copper ore deposits in Iran. They ascribe Cu mineralization to the underplating of Cu and sulfur-rich melts from fertile peridotite. These Cu deposits are believed to be generated from metal-rich magmas with high oxidation state and high H2O contents, which leads to the development of porphyry Cu systems in the Kerman Cenozoic arc segment (Asadi et al. 2014) and the great potential of ASTER and ETM+ data for mapping of the distribution of alteration and exploring for copper mineralization in areas with a similar climate and geological setting (Honarmand et al 2012). The igneous rocks of UMDA are mostly volcanic; however, plutonic rocks gradually increase eastward across the zone. In this paper, based on the combined data from field mapping and petrographic and geochemical (both mineral and whole rock) features, we focused on the Oligo-Miocene rocks of the Jebal-e-Barez plutonic complex (JBPC) in the southeastern part of UMDA
to establish tighter constraints on the petrogenetic processes and determine the tectonomagmatic evolution of the JBPC and subduction geometry and its relationship to arc magmatism at the UMDA to depict better constraints of the Neotethyan oceanic slab subduction underneath Central Iran and its related magmatism.
Geological setting The JBPC is the largest pluton (∼500 km2) in the UMDA that morphologically is a NW–SE trend; high mountains and streams of this area have cut deep valleys (Aale-Taha 2003). It is located at the E–NE of Jiroft (Fig. 1). Previously, the JBPC was separated into three plutonic phases by Ghorbani (2014). The first plutonic phase is the main body of complex with composition of quartz diorite to granodiorite. After differentiation of magma with the process of magmatic differentiation by fractional crystallization in the magmatic chamber, the porphyric and not fully consolidated magmas have been intruded into the main body. Their composition was dominantly granodiorite and granite in composition that is defined as the second plutonic phase. Finally, the last phase is started by an intrusion of the holo leucogranite into the previous bodies. This plutonic activity is pursued by the minor quaternary basaltic volcanism that shows metamorphic haloes in the contacts. Furthermore, the emplacement of subsequent homogenous plutonic rocks is common. They are dominantly porphyric leucogranites; however, some bodies show dendritic texture that may imply existence of silicic fluids in the latest crystallization stages (Ghorbani 2014). The abundance of microfractures and joints may imply cold and viscous magma. There are three types of joints in the studied rocks: (1) synmagmatic joints that form aplitic dykes; (2) cooling joints that caused hydrothermal alteration; and (3) post-crystallization joints. The contacts between igneous bodies and their country rocks are mainly sharp, although somewhere the continuous contacts were seen. The crystallization of magma released heat, in which magma passed into the country rock where it partially melted and became incorporated into the evolving magma.
Analytical methods A total of 200 samples of the various granitoids have been selected for common thin section study. Among them, 44 representative samples from the different granitic rocks were petrographically selected for whole rock chemical analysis. After agate mortar crushing, analysis of both major and trace elements were performed at the Department of Earth Sciences,
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Fig. 1 a The distribution of Cenozoic volcanic and plutonic rocks of UDMA in relation to the Sanandaj–Sirjan arc and Central Iran. Modified after Alavi 1994; Mohajjel et al. 2003; b Simplified geological map of the studied area
University of Perugia, Italy. The analysis for major elements was carried out by an X-ray fluorescence spectrometry (XRF) using a tube completed with Rn and W anodes under conditions with acceleration voltage of 40–45 kV and an electric current range of I = 30– 35 mA. For radiation separation in working regime without vacuum, a LiF-200 crystal analysis and scintillating detector were used. After calcination of powdered samples and full matrix correction after Franzini et al (1972), the sum of all major oxides is equal to about 100 wt.%. Precision is better than 10 % for V, Cr, Ni, Y, Zr, and Ba and better than 5 % for all the other elements. The concentration of trace elements in the selected samples has been performed by inductively coupled plasma mass spectrometry (ICP-MS). The uncertainty is 230 ppm) and Nd (>15 ppm) imply a long-lived mature arc setting for JBPC. The field, petrography, and geochemical studies indicated that the JPBC originated from both crustal and mantle-derived magmas. Some field and petrographic features such as the occurrence of MME, antirapakivi and cumulative textures, presence of green hornblende, magnetite, intergranular K-feldspar, automorph sphene, apatite inclusions in the amphibole
Fig. 18 Amphibole compositions imply that in the JBPC rocks display high fO2 and have been formed in oxidation conditions
Arab J Geosci (2016) 9:287
and biotite crystals, and absence of metamorphic minerals (e.g., garnet and andalusite) indicate involvement of upper mantle-originated magma in formation of the studied rocks. The increase in temperature and excess fluid pressure caused by subduction triggered melting of mantle edge and formation of basaltic magma and its ascent and introduction into crust followed by partial melting. The juxtaposed series of mafic–felsic pulses formed a mixed magma. Finally, this magma is emplaced at broad, shallow magma chamber (9– 12 km), where the differentiation took place by fractional crystallization and produced a wide variety of rocks from quartz diorite to alkali granite. In such shallow magma reservoirs, the emplacement of magma took place as sill (Lipman 1984; Fridrich et al 1991). Combined field observations and petrofabric studies with classified remote sensing data (not shown) displayed a deep caldera as a feeder zone for Eocene volcanic rocks (Rasouli 2015). The trend and plunge of lineations and direction and dip of foliations are changed slightly indicating injection and deformation of magma in low-changed strain conditions. The lithostatic pressure allows aplitic apophyses to be intruded into country rocks. Following a model proposed by Bray and Pallister (1991) and Fridrich et al (1991), resurgent intrusions initially spread as sill-like bodies near the base of the caldera and developed into stocklike plutons as continued emplacement of intrusive material gravitationally loads caldera-floor rocks and encourages block stoping. Sills generally share the country rock fabric, fed by vertical dikes, and the injected magma partially melted the country rocks. Mechanism of pluton emplacement at shallow-crustal levels in caldera has mostly been considered in sill form (Fridrich et al. 1991; Bray and Pallister 1991). The space problem has been a major focus of research in magma emplacement (e.g., Castro 1986; Brun and Pons 1981; Guineberteau et al 1987; Hutton 1996; Fernandez and Castro 1999; Petford and Gallagher 2001). In orogenic belt such as UDMA, transpressional tectonic regime is often associated with extensional shear fractures which generated spaces that allowed emplacement of magma. The decompression situation due to oblique subduction of Neotethyan oceanic crust beneath CIB permits emplacement of melted magma in appropriate spaces in the UDMA in its current NW–SE direction. The transpressional tectonic regime is general in shear zones (i.e., UDMA). The JBPC is located in a shear zone, and multiple magmatic pulses were injected as sills. The syntectonic JBPC is spatially associated with a major dextral transpressional shear
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Fig. 19 a Na2O versus SiO2 variation diagram showing alkali feldspar role in fractionation process; b the fractional evolution of the plagioclase and alkali feldspar in Rb versus Sr diagram (after Arth 1976). Symbols as in Fig. 4
zone (Fig. 21). The microstructural fabrics (magmatic, submagmatic, and mylonitic) imply that the shear zone was active during magma emplacement (Rasouli et al. 2014). Furthermore, the field studies show abundant fractures and joints in rocks which are characteristics of transpressional tectonics. These fractures caused extensive alteration in JBPC, especially in the late stock bodies (Shahabpour 2007; Honarmand et al. 2012). As
b
1
2
200
3
Y/Nb 4
5
K/Rb 400 600
6
1000
7
a
shown in Fig. 15, the microstructural signatures indicate dextral sense of shearing parallel to the direction UDMA of NW–SE. The fault system in the study area is North–South-striking, and magma was injected into the rotated shear fractures. The JBPC intruded parallel to the regional fabric as a sill into created spaces, and this progressive rotational opening allowed voluminous bodies of magma to injection and emplacement. The
2
5
10 20 Rb
50
100 200
0
10
20 Zr/Nb
30
40
Fig. 20 a The K/Rb versus Rb; b Zr/Nb versus Y/Nb for evaluating degree of crustal contamination (after Wilson 1989). FC fractional crystallization, CC crustal contamination. Symbols as in Fig. 4
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Arab J Geosci (2016) 9:287
Fig. 21 Schematic shape of the transpressional tectonic regime for emplacement of magmatism of Jebal-e-Barez plutonic complex
progressive deformation and folding of volcanic rocks associated with shearing in transpressional tectonic regime are followed by segregation and emplacement of granitic magmas.
Conclusions Based on a combined petrographic, field, mineral, and whole rock geochemical investigation of the JBPC, we propose the following evolutionary model: 1. The JBPC is a calk-alkaline complex that is located SE of the UDMA. This arc is formed by oblique subduction of Neotethys underneath Central Iran and contains voluminous volcanic and plutonic rocks. The geochemical signatures of studied rocks (e.g., high-K calk-alkaline) are characteristic of mature island arcs that have been evolved into active continental margin. 2. The abundant biotite in the granitoids, MMEs, and mineral assemblages of titanite + magnetite ± quartz indicate high oxygen buffer (above the quartz–fayalite–magnetite-QFM) that is typical for compressional tectonic regime.
3. The basaltic magma produced by partial melting of mantle wedge materials segregated and ascended to the base of the crust. The conductive heating from the underplating magma triggered of the melting and generation of granitic magma. At the same time, the crystallization occurred in the convicting interior produced rocks ranging in composition from intermediate (quartz diorite) through felsic (granite) at the study area. 5. The progressive heating of the country rocks melts and incorporates surrounding country rock into crystallizing magma. The shape and size of microgranular enclaves may indicate contemporaneous flow and mingling of partly crystalline felsic–mafic magmas. Furthermore, the elongated shapes of enclaves at the margins of igneous bodies may also imply magmatic flow. 6. Geothermobarometry study indicates that the magmas were emplaced at high-level depths (i.e., 9–12 km; upper continental crust) with low temperatures (650–750 °C). 7. The field, microstructural, and geochemical data implies synkinematic emplacement of the complex into an old caldera as a sill in a dextral transpressional shear zone.
65.98 0.41
70.01 0.33
70.65 0.19
JB91 71.65 0.22
JB94
67.43 0.40
JB97
66.93 0.41 12.45 9.73 0.01 0.27 0.19 1.20 4.31 0.15 372.4 105.1 34.0 4.0 2.5 1.0 7.0 4.0 20.0 31.0 3.7 13.9 2.8 0.6 1.8 0.3 1.3 0.3 0.8 0.1 0.8 0.1 6.7 1.7 0.3 0.1
72.54 0.22
JB100
63.85 0.53 16.01 4.92 0.11 2.28 5.45 3.89 1.86 0.10 302.1 72.5 377.8 163.0 4.4 11.8 15.4 32.6 13.8 32.6 3.9 16.3 4.1 0.9 3.4 0.7 3.7 0.9 2.3 0.3 2.1 0.4 22.4 3.1 0.4 4.3
68.11 0.31
71.43 0.26 14.46 3.23 0.10 0.67 2.48 3.62 3.34 0.08 451.5 95.5 166.2 5.0 8.5 4.0 4.0 4.0 30.0 53.1 6.3 22.3 4.6 0.8 4.0 0.7 4.2 1.0 2.7 0.4 3.2 0.4 26.7 2.5 0.8 0.2
JB27
62.75 0.49
JB116
0.07 0.98 2.63 5.41 0.03 461.5 109.1 113.1 4.0 5.5 2.0 2.4 8.0 30.0 55.1 6.1 19.6 3.3 0.5 2.4 0.3 1.5 0.3 0.9 0.1 0.8 0.1 8.3 1.1 0.7 0.1
76.52 0.09 12.95 0.87
JB26
JB112
70.25 0.19 14.88 2.47 0.10 0.95 3.00 3.98 1.99 0.04 608.5 51.7 376.6 68.7 2.7 8.7 2.9 0.0 10.2 21.3 2.2 7.9 1.6 0.5 1.3 0.2 1.4 0.4 1.0 0.2 1.0 0.2 9.5 1.2 0.3 1.9
JB21
68.25 0.37
JB85
0.30 0.94 2.75 5.10 0.04 638.6 113.1 121.1 4.0 3.0 4.0 1.6 6.0 20.0 34.0 3.8 12.7 2.4 0.5 2.0 0.3 1.7 0.4 1.1 0.1 1.0 0.1 9.7 2.4 0.2 0.1
75.62 0.20 13.05 1.39
JB19
SiO2 TiO2
JB81
0.71 4.01 6.00 0.25 0.13 59.7 1.8 213.2 4.0 3.0 4.0 0.8 4.0 9.0 11.0 1.5 7.0 1.9 0.6 2.0 0.4 2.3 0.5 1.6 0.2 1.8 0.2 15.2 0.4 0.3 0.2
0.53 3.13 5.62 0.15 0.09 43.2 1.8 160.2 5.0 5.0 4.0 0.8 4.0 8.0 11.5 1.7 8.0 2.6 0.5 3.0 0.7 4.0 0.9 2.7 0.4 3.0 0.3 26.5 0.5 0.5 0.2
72.83 0.31 13.86 2.39 0.02 0.64 2.45 4.00 2.58 0.07 320.3 43.1 147.1 5.0 3.0 4.0 3.0 4.0 10.0 29.0 3.6 13.5 3.0 0.7 2.8 0.5 3.1 0.7 2.2 0.3 2.4 0.3 20.5 0.7 0.3 0.2
JB14
JB63
70.53 0.39 16.16 0.80
74.52 0.33 14.16 0.74
JB13
Sample
70.63 0.30 14.86 3.53 0.08 0.68 2.79 3.40 2.52 0.09 479.5 74.8 274.3 10.0 7.0 4.0 4.0 4.0 20.0 42.0 5.1 19.1 3.8 0.9 3.4 0.6 3.4 0.7 2.0 0.3 1.9 0.2 20.3 2.4 0.6 0.2
JB11
70.93 0.30 14.96 3.28 0.06 0.57 3.26 4.17 1.47 0.09 375.4 38.6 301.3 15.0 7.5 4.0 6.6 8.0 20.0 45.0 5.4 19.9 3.8 0.9 3.4 0.6 3.3 0.7 2.0 0.3 2.1 0.2 20.8 0.8 0.5 0.4
JB10
SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 Ba Rb Sr Zr Nb Ni Co Cr La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Y Cs Ta Hf
JB6
JB3
Sample
JB4
The whole-rock major (wt %) and trace (ppm) chemical compositions of the JBPC rocks
Table 1
Appendix
72.01 0.22
JB118
60.34 0.70 16.26 7.17 0.13 2.66 6.08 2.37 2.57 0.16 346.3 61.7 302.3 10.0 10.0 6.0 18.4 8.0 30.0 53.1 6.6 25.5 5.2 1.1 4.6 0.8 4.7 1.1 2.9 0.4 3.1 0.4 28.2 0.8 0.7 0.6
JB28
76.27 0.04
JB128
72.23 0.23 14.26 2.85 0.08 0.56 2.24 3.63 3.42 0.07 434.4 107.1 149.1 10.0 9.5 2.0 3.6 4.0 20.0 47.0 5.7 20.2 4.1 0.8 3.8 0.7 4.2 1.0 2.8 0.5 3.3 0.4 27.6 1.7 1.1 0.6
JB29
76.02 0.06
JB137
76.02 0.14 13.35 1.54 0.05 0.43 2.06 4.59 1.28 0.05 235.2 33.8 159.2 4.0 6.0 2.0 1.6 4.0 10.0 25.0 2.7 9.3 1.8 0.5 1.6 0.3 1.7 0.4 1.2 0.2 1.3 0.2 11.1 0.3 0.7 0.1
JB30 75.12 0.10 13.55 1.96 0.04 0.25 1.77 3.34 3.60 0.03 420.4 117.1 145.1 5.0 7.0 4.0 1.6 10.0 30.0 57.6 6.2 20.5 3.4 0.6 2.6 0.4 1.9 0.4 1.1 0.1 1.1 0.1 11.1 2.7 0.7 0.2
JB32
72.11 0.18
JB138
76.52 0.11 12.85 1.60 0.03 0.15 1.40 3.16 3.69 0.03 538.5 86.3 176.2 4.0 7.5 4.0 1.8 6.0 30.0 57.1 6.3 20.8 3.7 0.6 2.8 0.4 2.0 0.4 1.1 0.1 1.1 0.1 10.5 1.5 0.8 0.1
JB31
75.98 0.02
JB143
75.92 0.07 12.75 1.77 0.04 0.19 0.84 2.84 4.76 0.02 474.5 98.9 89.1 5.0 4.0 2.0 2.2 4.0 30.0 54.6 6.2 20.4 3.8 0.5 3.2 0.5 2.5 0.5 1.5 0.2 1.7 0.2 15.9 1.8 0.6 0.1
JB33
71.25 0.28
JB149
54.79 0.86 17.65 8.75 0.18 3.54 7.35 4.13 0.80 0.15 100.6 20.7 379.1 140.9 4.4 11.2 20.2 25.1 12.9 33.6 4.7 21.0 5.6 1.4 5.0 0.9 5.2 1.2 3.1 0.4 2.7 0.5 29.5 0.5 0.3 3.7
JB40
59.12 0.69
JB156
2.0 0.1 1.0 10.0 27.0 2.8 8.8 1.5 0.4 0.8 0.1 0.4 0.1 0.3 0.0 0.3 0.0 1.7 1.3 0.1 0.4
0.48 0.09 0.17 3.33 0.04 909.9 75.8 113.1 15.0
81.52 0.38 11.55 0.57
JB48
55.24 0.56
72.15 0.27 14.35 2.18 0.01 0.76 1.88 4.35 2.81 0.05 481.6 95.0 217.2 145.2 8.4 7.2 4.3 29.9 17.1 35.2 3.6 12.7 2.7 0.6 2.2 0.4 2.3 0.6 1.6 0.3 1.7 0.3 15.5 2.1 0.8 3.9
JB59
71.78 0.28
JB163
69.89 0.31 14.84 2.82 0.10 0.89 2.88 5.11 2.42 0.07 1125 83.9 295.2 132.6 7.4 7.9 7.0 7.4 19.8 40.5 4.0 13.9 2.9 0.7 2.4 0.4 2.5 0.6 1.6 0.3 1.7 0.3 15.6 1.5 0.6 3.2
JB54
JB163
67.01 0.34 15.48 3.07 0.11 0.88 2.99 4.85 3.05 0.07 566.3 89.0 289.8 176.2 6.3 11.3 6.9 81.5 18.0 38.1 4.2 16.4 3.7 0.8 3.1 0.6 3.3 0.8 2.1 0.3 2.0 0.4 21.2 0.6 0.5 4.1
JB53
65.32 0.29
JB181
70.25 0.25 15.09 3.18 0.05 1.25 2.97 2.84 1.82 0.06 534.3 46.3 343.9 74.9 3.1 7.1 7.6 31.3 12.0 24.6 2.5 9.0 2.2 0.6 2.0 0.4 2.3 0.6 1.4 0.2 1.4 0.3 15.2 1.2 0.3 2.1
JB61
Arab J Geosci (2016) 9:287 Page 17 of 22 287
JB63
15.09 3.16
0.09 1.70 3.98 3.91 2.40 0.05 355.1 94.3 305.8 104.1 3.9 10.0 9.4 28.7 14.3 30.3 3.2 11.8
2.6 0.7 2.1 0.4 2.1 0.5 1.2 0.2 1.2 0.2 13.1 4.7 0.4 3.0
Sample
Al2O3 Fe2O3
MnO MgO CaO Na2O K2O P2O5 Ba Rb Sr Zr Nb Ni Co Cr La Ce Pr Nd
Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Y Cs Ta Hf
Table 1 (continued)
2.0 0.6 1.7 0.3 1.8 0.4 1.1 0.2 1.1 0.2 11.5 4.5 0.6 3.0
0.07 1.40 3.60 4.01 2.21 0.05 220.4 116.7 293.6 103.1 5.0 12.4 8.6 27.5 9.3 20.9 2.2 8.7
14.86 2.69
JB85
1.7 0.5 1.3 0.2 1.0 0.2 0.6 0.1 0.7 0.1 6.2 6.7 0.4 2.8
0.06 0.75 2.26 3.75 3.35 0.03 370.1 163.3 199.5 98.9 4.3 12.6 5.1 31.5 20.6 37.9 3.2 9.9
14.37 1.61
JB91
1.8 0.5 1.4 0.2 1.3 0.3 0.9 0.1 0.9 0.2 8.0 5.4 0.6 2.8
0.07 0.93 2.51 3.78 3.11 0.03 401.6 156.7 239.7 96.3 4.5 9.5 6.0 18.9 16.2 33.2 3.1 10.6
14.09 1.95
JB94
2.5 0.7 2.2 0.4 2.3 0.5 1.3 0.2 1.4 0.2 14.1 6.2 0.4 3.0
0.09 1.98 4.36 3.75 2.24 0.05 331.1 89.9 327.2 115.0 4.2 10.6 11.4 11.4 13.0 28.4 3.0 11.7
14.96 3.62
JB97
1.6 0.4 1.4 0.2 1.2 0.3 0.8 0.1 0.9 0.2 8.6 4.3 0.7 2.6
0.08 0.83 2.48 3.97 3.05 0.03 323.1 141.8 208.6 92.6 4.8 16.7 5.7 144.4 16.6 30.4 2.7 8.9
13.95 1.93
JB100
2.5 0.8 2.1 0.4 2.1 0.5 1.3 0.2 1.4 0.2 13.5 3.2 0.5 2.5
0.13 1.13 3.69 3.76 2.09 0.08 419.6 87.1 353.0 98.9 5.5 8.3 6.8 14.5 17.4 35.9 3.5 12.4
15.27 3.49
JB112
2.8 0.9 2.4 0.4 2.5 0.6 1.5 0.3 1.5 0.3 15.5 2.4 0.3 2.5
0.17 2.36 5.86 3.21 1.68 0.10 256.0 55.8 449.7 94.0 3.6 6.1 13.3 15.0 13.0 27.0 3.1 11.9
15.98 6.08
JB116
4.1 0.8 3.7 0.7 4.0 0.9 2.6 0.4 2.5 0.4 25.6 2.4 0.7 4.0
0.09 0.63 2.33 4.16 2.81 0.04 390.8 110.9 193.5 147.7 7.9 6.2 3.7 0.0 25.0 51.8 5.6 20.4
14.26 2.33
JB118
3.4 0.3 2.9 0.6 3.7 0.9 2.5 0.4 2.7 0.5 24.7 1.9 1.2 2.0
0.10 0.10 0.82 4.16 3.95 0.00 403.1 179.6 74.5 50.2 10.4 16.6 3.0 106.1 18.0 41.2 3.9 14.6
13.40 0.85
JB128
2.7 0.3 2.3 0.4 2.1 0.5 1.5 0.2 1.7 0.3 14.0 2.6 0.8 2.1
0.03 0.10 0.70 4.11 4.21 0.00 226.9 253.2 52.8 65.4 8.2 3.0 1.5 16.3 36.7 72.3 6.0 19.3
13.28 0.70
JB137
4.3 0.8 3.6 0.6 3.6 0.9 2.4 0.4 2.4 0.4 23.3 1.5 0.8 3.8
0.32 0.55 2.11 4.34 2.55 0.04 490.7 93.7 225.8 134.5 8.4 5.1 4.8 37.0 28.2 61.9 6.1 22.1
14.43 2.10
JB138
4.2 0.1 4.5 1.0 7.1 1.8 5.2 0.8 5.5 1.0 50.6 1.4 3.1 3.7
0.01 0.04 0.62 3.88 4.71 0.00 96.7 231.6 32.2 74.3 17.6 7.4 1.0 14.4 13.0 33.9 3.5 14.1
13.54 0.53
JB143
6.0 0.8 5.2 1.0 5.7 1.4 3.6 0.6 3.7 0.6 36.0 2.3 1.2 5.6
0.12 0.75 2.33 4.01 2.85 0.05 437.8 137.0 192.2 200.1 13.0 8.0 5.3 0.0 32.4 75.0 7.7 28.3
14.26 3.09
JB149
4.2 1.1 3.8 0.7 4.3 1.0 2.6 0.4 2.4 0.4 26.6 1.8 0.3 3.2
0.15 3.02 6.98 3.57 1.37 0.09 201.9 48.5 403.5 121.4 3.8 10.2 17.3 30.3 11.4 27.3 3.5 15.5
16.57 6.80
JB156
4.6 1.0 4.2 0.8 4.5 1.1 2.7 0.4 2.5 0.4 27.3 1.4 0.5 3.8
0.16 2.77 4.69 2.37 1.95 0.09 302.4 68.2 309.2 142.1 6.4 13.6 16.2 44.5 19.1 43.2 5.1 19.7
14.35 6.85
JB163
1.9 0.5 1.5 0.3 1.5 0.3 0.9 0.1 0.9 0.2 9.1 6.4 0.6 3.1
0.07 1.09 2.91 4.01 2.56 0.04 352.9 132.2 263.0 106.2 4.9 7.9 6.4 2.7 13.6 27.2 2.6 9.3
14.24 2.22
JB163
3.1 0.8 2.6 0.5 2.7 0.6 1.7 0.3 1.7 0.3 16.8 4.2 0.5 3.1
0.15 1.49 4.33 3.48 1.68 0.07 445.2 55.6 397.0 123.0 5.8 7.1 9.1 5.9 19.0 39.8 4.0 14.8
15.36 4.52
JB181
Page 18 of 22
2.7 0.7 2.3 0.4 2.4 0.6 1.5 0.2 1.4 0.2 15.0 2.2 0.3 2.9
0.10 1.93 4.39 3.64 2.17 0.06 348.1 71.6 298.6 108.0 3.4 13.6 11.5 34.0 10.4 24.7 2.8 11.3
14.85 3.90
JB81
287 Arab J Geosci (2016) 9:287
Arab J Geosci (2016) 9:287 Table 2
Page 19 of 22 287
The electron probe microanalysis for minerals of selected samples
Amphibole SiO2 TiO2 Al2O3 FeO MnO MgO CaO Na2O K2O Total No. of O2 Si Al iv Al vi AlTotal Ti Fe3+ Fe2+ Mn Mg Ca K Mg/(Mg+Fe2)
JB76_4 53.09 1.37 5.52 10.32 0.30
JB76_5 52.80 1.44 5.12 10.50 0.29
JBT6_13 53.50 0.55 4.28 11.14 0.95
JBT6_14 54.11 0.89 5.79 10.42 0.54
JBT6_15 51.57 1.51 6.83 10.00 0.69
JB25_19 53.24 1.39 5.91 11.09 0.44
JB25_20 54.05 1.44 6.70 9.13 0.32
JB25_21 54.21 1.33 5.53 9.39 0.50
JB135_31 44.02 0.19 9.55 22.83 0.77
JB135_32 44.05 0.84 9.42 22.37 0.49
13.46 10.67 0.00 0.41 97.21 23.00 7.70 0.30 0.64 0.94 0.15 0.00 1.25 0.04 2.91 1.66 0.08 0.70
13.53 10.75 0.00 0.50 96.99 23.00 7.69 0.31 0.57 0.87 0.16 0.00 1.28 0.04 2.94 1.68 0.09 0.70
12.48 10.46 0.00 0.43 95.82 23.00 7.91 0.09 0.65 0.74 0.06 0.00 1.38 0.12 2.75 1.66 0.08 0.67
12.09 9.97 0.00 0.28 96.15 23.00 7.88 0.12 0.88 0.99 0.10 0.00 1.27 0.07 2.63 1.56 0.05 0.67
13.48 9.65 0.00 0.31 96.59 23.00 7.47 0.53 0.63 1.17 0.16 0.52 0.69 0.08 2.91 1.50 0.06 0.81
11.58 10.86 0.00 0.43 97.00 23.00 7.76 0.24 0.77 1.05 0.15 0.00 1.35 0.05 2.52 1.70 0.08 0.65
12.89 10.40 0.00 0.33 97.35 23.00 7.74 0.26 0.87 1.13 0.16 0.00 1.09 0.04 2.75 1.60 0.06 0.72
11.88 10.84 0.00 0.56 96.30 23.00 7.88 0.12 0.83 0.94 0.15 0.00 1.14 0.06 2.58 1.69 0.10 0.69
10.98 4.47 0.00 0.22 95.34 23.00 6.86 1.14 0.61 1.77 0.02 0.45 2.52 0.10 2.55 0.75 0.04 0.50
10.16 5.30 0.00 0.35 95.05 23.00 6.90 1.10 0.64 1.74 0.10 0.19 2.74 0.07 2.37 0.89 0.07 0.46
0.00
0.00
0.00
0.45
0.00
0.00
0.00
0.42
0.23
JB76-1 39.65 3.29 12.77 17.11 0.23 12.86 0.00 0.00 8.04
JB76-2 40.88 3.50 12.77 16.95 0.19 11.95 0.00 0.00 7.71
JB76-3 41.39 3.14 13.69 16.46 0.20 11.23 0.42 0.00 7.48
JB25-25 42.21 3.72 12.25 15.42 0.34 10.81 0.79 0.00 7.84
JB25-26 42.05 3.68 13.16 15.29 0.29 10.32 0.25 0.00 8.43
JB25-27 43.11 3.78 13.52 12.08 0.25 11.44 1.08 0.00 8.42
95.85 22.00 5.99 2.27 1.74 0.64 0.39 2.16 0.03 3.03 0.00 1.62 0.57
95.86 22.00 6.13 2.26 1.59 0.77 0.41 2.13 0.03 2.79 0.00 1.54 0.56
95.93 22.00 6.17 2.41 1.55 0.96 0.37 2.05 0.03 2.61 0.07 1.49 0.55
95.38 22.00 6.32 2.16 1.68 0.49 0.42 1.93 0.04 2.41 0.13 1.50 0.56
95.47 22.00 6.29 2.32 1.71 0.62 0.41 1.91 0.04 2.30 0.04 1.61 0.55
95.72 22.00 6.34 2.34 1.66 0.68 0.42 1.48 0.03 2.51 0.17 1.58 0.63
Fe3/(Fe3+Alvi) 0.00 Biotite SiO2 TiO2 Al2O3 FeO MnO MgO CaO Na2O K2O Total No. of O2 Si Al Al iv Al vi Ti Fe Mn Mg Ca K Mg/(Mg+Fe2)
287
Arab J Geosci (2016) 9:287
Page 20 of 22
Table 2 (continued) Alkali feldspar SiO2 Al2O3 Fe2O3 FeO CaO Na2O K2O total Si Al Fe3+ Fe2+ Ca Na K XAn XAb XOr
1 71.15 16.09 0.09 0.10 0.00 2.81 9.85 100.09 3.16 0.84 0.00 0.00 0 0.24 0.56 0.00 30.24 69.76
2 70.61 15.75 0.09 0.10 0.22 1.47 11.85 100.09 3.17 0.83 0.00 0.00 0.01 0.13 0.68 1.29 15.66 83.05
2 71.24 16.67 0.09 0.10 0.48 0.60 10.91 100.09 3.16 0.87 0.00 0.00 0.02 0.05 0.62 3.30 7.46 89.24
4 72.02 15.09 0.09 0.10 0.00 2.79 9.88 99.97 3.20 0.79 0.00 0.00 0.00 0.24 0.56 0.00 30.03 69.97
5 70.63 15.40 0.09 0.10 0.29 1.54 11.96 100.01 3.17 0.82 0.00 0.00 0.01 0.13 0.69 1.67 16.09 82.23
6 71.09 16.23 0.09 0.10 0.27 1.00 10.67 99.45 3.18 0.85 0.00 0.00 0.01 0.09 0.61 1.83 12.24 85.93
7 71.19 15.98 0.09 0.10 0.00 2.72 9.60 99.68 3.17 0.84 0.00 0.00 0.00 0.23 0.55 0.00 30.10 69.90
8 71.19 15.98 0.09 0.10 0.00 2.72 9.60 99.68 3.17 0.84 0.00 0.00 0.00 0.23 0.55 0.00 30.10 69.90
9 71.23 14.67 0.09 0.10 0.22 1.50 12.21 100.02 3.20 0.78 0.00 0.00 0.01 0.13 0.70 1.26 15.54 83.21
10 71.02 16.01 0.09 0.10 0.19 1.61 10.98 100.00 3.17 0.84 0.00 0.00 0.01 0.14 0.62 1.17 18.01 80.82
Plagioclase SiO2 TiO2 Al2O3 Cr2O3 Fe2O3 FeO MnO MgO CaO BaO Na2O K2O total Si Ti Al Cr Fe3 Fe2 Mn Mg Ca Ba Na K XAn XAb XOr
JB90_6 59.86 0 23.68 0.29 0.25 0.22 0 0 8.74 0 6.66 0.22 99.92 2.685 0.000 1.252 0.010 0.008 0.008 0.000 0.000 0.420 0.000 0.579 0.013 41.51 57.24 1.24
JB90_7 60.01 0 24.38 0 0.35 0.31 0 0 10.56 0 3.41 0.45 99.47 2.687 0.000 1.286 0.000 0.012 0.012 0.000 0.000 0.507 0.000 0.296 0.026 61.16 35.74 3.10
JB90_8 60.02 0 24.34 0 0.25 0.22 0 0 9.98 0 4.84 0.24 99.89 2.681 0.000 1.282 0.000 0.008 0.008 0.000 0.000 0.478 0.000 0.419 0.014 52.46 46.04 1.50
JB90_9 66.74 0 21.06 0 0.19 0.17 0 0 5.84 0 5.85 0.31 100.16 2.915 0.000 1.084 0.000 0.006 0.006 0.000 0.000 0.273 0.000 0.495 0.017 34.77 63.03 2.20
JB90_10 62.46 0 23.58 0 0.21 0.19 0 0 8.49 0 4.99 0.27 100.19 2.759 0.000 1.228 0.000 0.007 0.007 0.000 0.000 0.402 0.000 0.427 0.015 47.59 50.61 1.80
JB90_11 61.12 0 24.7 0 0.25 0.22 0 0 10.34 0 3.01 0.23 99.87 2.709 0.000 1.290 0.000 0.008 0.008 0.000 0.000 0.491 0.000 0.259 0.013 64.38 33.91 1.71
JB90_12 60.31 0 25.26 0 0.35 0.31 0 0 10.05 0 3.57 0.34 100.19 2.675 0.000 1.320 0.000 0.012 0.011 0.000 0.000 0.478 0.000 0.307 0.019 59.41 38.19 2.39
JB25_23 93.94 0.03 2.84 0 0.09 0.08 0 0 1.41 0 1.03 0.36 99.78 3.837 0.001 0.137 0.000 0.003 0.003 0.000 0.000 0.062 0.000 0.082 0.019 38.08 50.34 11.58
JB25-24 80.71 0 9.01 0 0.1 0.04 0 0.04 5.88 0 2.11 0.11 98.00 3.472 0.000 0.457 0.000 0.003 0.001 0.000 0.003 0.271 0.000 0.176 0.006 59.82 38.85 1.33
JBT6_17 65.96 0 23.55 0 0.16 0.14 0 0 7.37 0 2.78 0.19 100.15 2.859 0.000 1.203 0.000 0.005 0.005 0.000 0.000 0.342 0.000 0.234 0.011 58.37 39.84 1.79
11 70.75 15.79 0.09 0.10 0.12 1.54 11.93 100.32 3.17 0.83 0.00 0.00 0.01 0.13 0.68 0.70 16.29 83.01
12 71.18 16.14 0.09 0.10 0.17 1.24 11.06 99.98 3.17 0.85 0.00 0.00 0.01 0.11 0.63 1.09 14.40 84.51
Arab J Geosci (2016) 9:287 Acknowledgments This paper is a part of the first author’s PhD thesis. Parts of the research expenses were funded by a Shahid Beheshti University research grant which is gratefully acknowledged. It is also supported by Payam-e-Noor University’s grant. We thank the University of Perugia for ICP-MS analyses, with particular thanks to Mr. Fabio Lazar for technical assistance during the first author’s sabbatical.
References Aale-Taha B (2003) Petrography and petrology of igneous rocks and related Cu mineralization at the Southeast of Bam (Jebal-e-Barez). PhD thesis, Azad University (Olom-o-Tahghighat), Tehran, 388 p (In persian) Abdel-Rahman A (1994) Nature of biotites from alkaline, calcalkaline, and peraluminous Magmas. J Petrol 35(2):525–541 Ahadnejad V, Valizadeh MV, Deevsalar R, Rezaei-Kahkhaei M (2011) Age and geotectonic position of the Malayer granitoids: implication for plutonism in the Sanandaj-Sirjan Zone, W Iran. N Jb Geol Palaontol Abh 261:61–75 Agard P, Omrani J, Jolivet L, Whitechurch H, Vrielynck B, Spakman W, Monié P, Meyer B, Wortel R (2011) Zagros orogeny: a subductiondominated process. In: Lacombe O, Grasemann B, Simpson G (Eds). Geodynamic Evolution of the Zagros: geological magazine. 134:692–725. doi: 10.1017/S001675681100046X Alavi M (1994) Tectonics of the Zagros orogenic belt of Iran: new data and interpretations. Tectonophysics 220:211–238 Anderson JL (1983) Proterozoic anorogenic granite plutonism of North America. Geol Soc Am Mem 161:133–154 Anderson JL, Smith DR (1995) The effects of temperature and fO2 on the Al-in-hornblende barometer. Am Mineral 80:549–559 Arth JG (1976) Behaviour of trace elements during magmatic process summary of theoretical models and their applica-tions. Rev Geophys Space Phys 15:96–104 Asadi S, Moore F, Zarasvandi A (2014) Discriminating productive and barren porphyry copper deposits in the Southeastern part of the central Iranian volcano-plutonic belt, Kerman region, Iran: a review. Earth Sci Rev 138:25–46 Berberian F, Berberian M (1981) Tectono-plutonic episodes in Iran. In: Gupta HK, Delany FM (eds) Zagros Hindu Kush Himalaya geodynamic evolution. American Geophysical Union, Washington DC, pp 5–32 Berberian M, King GCP (1981) Towards a paleogeography and tectonic evolution of Iran. Can J Earth Sci 18:210–226 Bina MM, Bucur I, Prevot M, Meyerfeld Y, Daly L, Cantagrel JM, Mergoil J (1986) Palaeomagnetism petrology and geochronology of Tertiary magmatic and sedimentary units from Iran. Tectonophysics 121:303–329 Brun JP, Pons J (1981) Strain pattern of pluton emplacement in a crust undergoing non-coaxial deformation, Sierra Morena, Southern Spain. J Struct Geol 3:219–229 Castro A (1986) Structural pattern ascent model in the central extremadura batholith, Hercynian belt, Spain. J Struct Geol 8:633–645 Chappell BW, White AJR (1992) I and S-type granites in the Lachlan fold belt. Trans R Soc Edinb Earth Sci 83:1–26 Coleman RG, Peterman ZE (1975) Oceanic plagiogranites. J Geophys Res 80:1099–1108 De Souza ZS, Martin H, Peucat JJ, Jardim De Sá EF, De Freitas Macedo MH (2007) Calc-alkaline magmatism at the archean–proterozoic transition: the caicó complex basement (NE Brazil). J Petrol 48: 2149–2185 Dewey JF, Pitman WC III, Ryan WBF, Bonnin J (1973) Plate tectonics and the evolution of the alpine system. Geol Soc Am Bull 84:3137–3318 Du Bray EA, Pallister JS (1991) An ash flow caldera in cross section: ongoing field and geochemical studies of the mid tertiary Turkey
Page 21 of 22 287 Creek caldera, Chiricahua Mountains, SE Arizona. J Geophys Res 96: doi: 10.1029/91JB00067. issn: 0148-0227 Esna-Ashari A, Tiepolo M, Valizadeh MV, Hassanzadeh J, Sepahi AA (2012) Geochemistry and zircon U-Pb geochronology of Aligoodarz granitoid complex, Sanandaj-Sirjan zone, Iran. J Asian Earth Sci 43:11–22 Ewart A (1979) A review of the mineralogy and chemistry of tertiaryrecent dacitic, latitic, rhyolitic and related salic volcanic rocks. In: Barker F (ed). Trondhjemites, dacites, and related rocks. SpringerVerlag, 12-101 Fernandez C, Castro A (1999) Pluton accommodation at high strain rates in the upper continental crust. The example of the central extremadura batholith, Spain. J Struct Geol 21:1143–1149 Floyd PA, Winchester JA (1975) Magma type and tectonic setting discrimination using immobile elements. Earth Planet Sci Lett 27:211– 218 Franzini M, Leoni M, Saitta M (1972) A simple method to evaluate the matrix effects in X-ray fluorescence analysis. X-Ray Spectrom 1: 151–154 Fridrich CJ, Smith RP, DeWitt E, McKee EH (1991) Structural, eruptive, and intrusive evolution of the Grizzly Peak caldera, Sawatch Range, Colorado. Geol Soc Am Bull 103:1160–1177 Ghorbani M (2014) Geology of Iran (Book). Arian Zamin Publications, 488 p (In persian) Goswami B, Bhattacharyya C (2014) Petrogenesis of shoshonitic granitoids, eastern India: implications for the late Grenvillian postcollisional magmatism. Geosci Front 5:821–843 Guineberteau B, Bouchez JL, Vigneresse JL (1987) The Mortagne granite pluton (France) emplaced by pull-apart along a shear zone: structural and gravimetric arguments and regional implication. Geol Soc Am Bull 99:763–770 Hall A (1987) Igneous petrology Longman, London, 573 P Harris NBW, Pearce JA, Tindle AG (1986) Geochemical characteristics of collision-zone magmatism. In: Coward MP, Alison C (eds) Collision tectonics. Geological Society London Special Publications 19: 67–81 Henry DJ, Guidotti CV, Thomson JA (2005) The Ti-saturation surface for low-to-medium pressure metapeliticbiotite: implications for geothermometry and Ti-substitution mechanisms. Am Mineral 90: 316–328 Honarmand M, Ranjbar H, Shahabpour J (2012) Application of principal component analysis and spectral angle mapper in the mapping of hydrothermal alteration in the Jebal–Barez area, Southeastern Iran. Resour Geol 62(2):119–139 Hutton DHW (1996) The space problem in the emplacement granite. Episodes 19(4):114–119 Irvine TN, Baragar WRA (1971) A guide to the classification of the common volcanic rocks. Can J Earth Sci No. 8 Kroll H, Evangelakakis C, Voll G (1993) Two-feldspar geothermometry: a review and revision for slowly cooled rocks. Contrib Mineral Petrol 114:510–518 Leake BE (1997) Nomenclature of amphiboles of the subcommittee on amphiboles of the international mineralogical association commission on new minerals and mineral names. Eur J Mineral 9:623–651 Lipman PW (1984) The roots of ash-flow calderas in North America: windows into the tops of granitic batholiths. J Geophys Res 89(1): 8801–8841 Maniar PD, Piccoli PM (1989) Tectonic discrimination of granitoids. Geol Soc Am Bull 101:635–643 Mazhari SA, Bea F, Amini S, Ghalamghash J, Molina JF, Montero P, Scarrow JH, Williams IS (2009) The Eocene bimodal Piranshahr massif of the Sanandaj-Sirjan Zone, NW Iran: a marker of the end of the collision in the Zagros Orogen. J Geol Soc 166:53–69 McQuarrie N, van Hinsbergen DJJ (2013) Retrodeforming the ArabiaEurasia collision zone: age of collision versus magnitude of continental subduction. Geology 41(3):315–318
287
Page 22 of 22
McQuarrie N, Stock JM, Verdel C, Wernicke BP (2003) Cenozoic evolution of Neotethys and implications for the causes of plate motions. Geophys Res Lett 30:2036. doi:10.1029/2003GL017992 Middlemost EAK (1994) Naming materials in the magma/igneous system. Earth Sci Rev 37:215–224 Mohajjel M, Fergusson CL, Sahandi MR (2003) Cretaceous-Tertiary convergence and continental collision, Sanandaj-Sirjan zone, western Iran. J Asian Earth Sci 21:397–412 Nachit H, Ibhi A, Abia EH, Ohoud MB (2005) Discrimination between primary magmatic biotites, reequilibrated biotites and neoformed biotites. Compt Rendus Geosci 337:1415–1420 Nakamura N (1974) Determination of REE, Ba, Fe, Mg, Na, and K in carbonaceous and ordinary chondrites. Geochim Cosmochim Acta 38:757–775 Omrani J, Agard PH, Whitechurch H, Benoit M, Prouteau Gand Jolivet L (2008) Arc magmatism and subduction history beneath the Zagros Mountains, Iran: a new report of adakites and geodynamic consequences. Lithos 106:380–398 Patiño Douce AE (1999) What do experiments tell us about the relative contributions of crust and mantle to the origin of granitic magmas? In: Castro A, Fernandez C, Vigneresse JL (Eds). Understanding granites: integrating new and classical techniques. Geol Soc London Spec Publ 168, 55–75 Patiño Douce AE (2005) Vapor-absent melting of tonalite at 15-32 kbar. J Petrol 46:275–290 Pearce JA, Harris NB, Tindle AG (1984) Trace element discrimination diagrams for the tectonic interpretation of granitic rocks. J Petrol 25: 956–983 Peccerillo A, Taylor, SR (1976) Geochemistry of the Eocene calcalkaline volcanic rocks from the Kastamonu area northern Turkey. Contrib Mineral Petrol 58(1):63–81 Peters T (2000) Formation and evolution of the western Indian Ocean as evidenced by the Masirah ophiolite: a review. In: Dilek Y, Moores EM, Elthon D, Nicolas A (eds) Ophiolites and oceanic crust: new insights from field studies and the ocean drilling program. Colorado: Geol Soc Am Sp Paper 525-536 Petford N, Gallagher K (2001) Partial melting of mafic (amphibolitic) lower crust by periodic influx of basaltic magma. Earth Planet Sci Lett 193:483–489 Petrelli M, Perugini D, Poli G, Peccerillo A (2007) Graphite electrode lithium tetraborate fusion for trace element determination in bulk geological samples by laser ablation ICP-MS. Microchim Acta 158:275–282 Putirka KD (2008) Thermometers and barometers for volcanic systems. In: Putirka KD, Tepley FJ III (eds). Minerals, inclusions and volcanic processes. Mineral Soc Am Geochem Soc Rev Mineral Geochem 69: 61–120 Rasouli J (2015) Petrology, geochemistry and reviewing the zoning alteration and copper mineralization in Jabal Barez Granitoid complex
Arab J Geosci (2016) 9:287 (North East Jeroft). Ph.D. Thesis, Shahid Beheshti University, Tehran, Iran, 366 p (In persian) Rasouli J, Ghorbani M, Ahadnejad V (2014) Field observations, Petrography and microstructures study of Jebale Barez Plutonic complex (East–North East Jiroft). J Tethys 2(3):178–195 Ridolfi F, Renzulli A (2012) Calcic amphiboles in calc-alkaline and alkaline magmas: thermobarometric and chemometric empirical equations valid up to 1130 & #xB0;C and 2.2 GPa. Contrib Mineral Petrol 163:877–895 Robert JL (1976) Titanium solubility in synthetic phlogopite solid solutions. Chem Geol 17:213–227 Sakuyama T, Ozawa K, Sumino H, Nagao K (2009) Progressive melt extraction from upwelling mantle constrained by the Kita-Matsuura Basalts in NW Kyushu, SW Japan. J Petrol 50:725–779 Sepahi AA, Shahbazi H, Siebel W, Ranin A (2014) Geochronology of plutonic rocks from the Sanandaj-Sirjan zone, Iran and new zircon and titanite U-Th-Pb ages for granitoids from the Marivan pluton. Geochronometria 41(3):207–215 Shafiei B, Haschke M, Shahabpour J (2009) Recycling of orogenic arc crust triggers porphyry Cu mineralization in Kerman Cenozoic arc rocks, southeastern Iran. Miner Deposita 44:265–283 Shahabpour J (2007) Island-arc affinity of the central Iranian volcanic belt. J Asian Earth Sci 30:652–665 Shahbazi H, Siebel W, Pourmoafee M, Ghorbani M, Sepahi AA, Shang CK, Vousoughi-Abedini M (2010) Geochemistry and U–Pb zircon geochronology of the Alvand plutonic complex in Sanan-daj–Sirjan Zone (Iran): new evidence for Jurassic magmatism. J Asian Earth Sci 39(6):668–683 Shahbazi H, Siebel W, Pourmoafee M, Ghorbani M, Sepahi AA, Vousoughi-Abedini M, Shang CK (2015) The Almogholagh pluton, Sanandaj-Sirjan zone, Iran: geochemistry, U-(Th)-Pb titanite geochronology and implications for its tectonic evolution. J Mineral Geochem 192(1):85–99 Shand SJ (1943) Eruptive rocks. Their genesis, composition, classification, and their relation to ore-deposits with a chapter on meteorite. John Wiley and Sons, New York Sun SS, McDonough WF (1989) Chemical and isotopic systematic of oceanic basalts; implications for mantle composition and processes. In: Saunders AD, Norry MJ (Eds). Magmatism in the Ocean Basins. Geological Society of London, pp. 313–345 (Special Publication No. 42) Tarney J, Jones CE (1994) Trace element geochemistry of orogenic igneous rocks and crustal growth models. J Geol Soc Lond 151:855–868 Taylor SR, McLennan SM (1985) The continental crust: its composition and evolution. Blackwell, Oxford, 312 pp Vynhal CR, McSween HY, Speer JA (1991) Hornblende chemistry in southern Appalachian granitoides: implications for aluminiumhornblende thermobarometry and magmatic epidote stability. Am Mineralogists 76:176–188 Wilson M (1989) Igneous petrogenesis. Unwin Hyman, London, 456 pp
