Lithos 308–309 (2018) 364–380

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Lithos

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The Late Jurassic Panjeh submarine volcano in the northern Sanandaj-Sirjan Zone, northwest Iran: Mantle plume or active margin?

Hossein Azizi a,⁎, Federico Lucci b,RobertJ.Sternc, Shima Hasannejad d, Yoshihiro Asahara e a Mining Department, Faculty of Engineering, University of Kurdistan, Sanandaj, Iran b Dipartimento di Scienze, Sez. Scienze Geologiche, Università Roma Tre, Largo S. L. Murialdo 1, 00146 Roma, Italy c Geosciences Department, University of Texas at Dallas, Richardson, TX 75083-0688, USA d Earth Sciences Department, Faculty of Basic Sciences, University of Kurdistan, Sanandaj, Iran e Department of Earth and Environmental Sciences, Graduate School of Environmental Studies, Nagoya University, Nagoya 464-8601, Japan article info abstract

Article history: The tectonic setting in which Jurassic igneous rocks of the Sanandaj-Sirjan Zone (SaSZ) of Iran formed is contro- Received 3 January 2018 versial. SaSZ igneous rocks are mainly intrusive granodiorite to gabbroic bodies, which intrude Early to Middle Accepted 17 March 2018 Jurassic metamorphic basement; Jurassic volcanic rocks are rare. Here, we report the age and petrology of volca- Available online 28 March 2018 nic rocks from the Panjeh basaltic-andesitic rocks complex in the northern SaSZ, southwest of Ghorveh city. The Panjeh magmatic complex consists of pillowed and massive basalts, andesites and microdioritic dykes and is as- Keywords: sociated with intrusive gabbros; the overall sequence and relations with surrounding sediments indicate that this Intra-oceanic arc system Ocean island basalt is an unusually well preserved submarine volcanic complex. Igneous rocks belong to a metaluminous sub-alka- fi – Supra-subduction zone line, medium-K to high-K calc-alkaline ma c suite characterized by moderate Al2O3 (13.7 17.6 wt%) and variable Sanandaj Sirjan Zone Fe2O3 (6.0–12.6 wt%) and MgO (0.9–11.1 wt%) contents. Zircon U-Pb ages (145–149 Ma) define a Late Jurassic Neo-Tethys realm (Tithonian) age for magma crystallization and emplacement. Whole rock compositions are enriched in Th, U and light rare earth elements (LREEs) and are slightly depleted in Nb, Ta and Ti. The initial ratios of 87Sr/86Sr (0.7039–0.7076) and εNd(t) values (−1.8 to +4.3) lie along the mantle array in the field of ocean island basalts and subcontinental metasomatized mantle. Immobile trace element (Ti, V, Zr, Y, Nb, Yb, Th and Co) behavior sug- gests that the mantle source was enriched by fluids released from a subducting slab (i.e. deep-crustal recycling) with some contribution from continental crust for andesitic rocks. Based the chemical composition of Panjeh mafic and intermediate rocks in combination with data for other gabbroic to dioritic bodies in the Ghorveh area we offer two interpretations for these (and other Jurassic igneous rocks of the SaSZ) as reflecting melts from a) subduction-modified OIB-type source above a Neo-Tethys subduction zone or b) plume or rift tectonics involving upwelling metasomatized mantle (mostly reflecting the ~550 Ma Cadomian crust-forming event). © 2018 Elsevier B.V. All rights reserved.

1. Introduction time (e.g. Aliani et al., 2012; Berberian et al., 1982; Berberian and Berberian, 1981; Davoudian et al., 2008; Ghasemi and Talbot, 2006; Understanding the tectonic setting and timing of Jurassic igneous ac- Mahmoudi et al., 2011; Mohajjel et al., 2003; Mohajjel and Fergusson, tivity in the Sanandaj-Sirjan Zone (SaSZ) is key for reconstructing the 2014; Moinevaziri et al., 2015; Nadimi and Konon, 2012; Shahbazi et tectonomagmatic evolution of SW Eurasia. This occurred from 143 to al., 2010, 2014; Stöcklin and Nabavi, 1973). This study is focused on 187 Ma (Fig. 1) with a peak of igneous activity in Middle Jurassic time, the heretofore-unstudied Panjeh mafic complex in the northern SaSZ ~165 Ma (Bayati et al., 2017). Most SaSZ igneous rocks are gabbro to sy- (Fig. 2a, b). In this paper U-Pb zircon ages, whole-rock geochemistry enite intrusions emplaced between 160 and 180 Ma, but younger intru- and Sr-Nd isotopic ratios are used to constrain Panjeh complex sions (144–156 Ma) are found in the far NW SaSZ (e.g., Suffi Abad magma genesis and its possible geodynamic implications. Specifically, granite, Ghorveh plutonic complex, Almagholagh diorite, and granitoids we focus on the controversy about the tectonic setting in which these of the Alvand plutonic complex; Bayati et al., 2017). However, Jurassic magmas formed, volcanic arc environment or rift/mantle-plume tec- volcanic rocks in the SaSZ are rare and still poorly studied. Here we re- tonic setting. port results of a first study of Jurassic volcanic rocks and use these re- sults to better understand the evolution of the SaSZ, considered to mark the start of a Neo-Tethys convergent margin in Middle Jurassic 2. Geological setting

⁎ Corresponding author. The SaSZ extends for 1500 km along the Zagros orogen from south- E-mail address: [email protected] (H. Azizi). east to northwest Iran (Fig. 1). The term was first introduced by Stöcklin

https://doi.org/10.1016/j.lithos.2018.03.019 0024-4937/© 2018 Elsevier B.V. All rights reserved. H. Azizi et al. / Lithos 308–309 (2018) 364–380 365

Fig. 1. Simplified geology map of the Sanandaj-Sirjan zone (SaSZ), which shows the intrusive bodies that are extend parallel to the Zagros thrust fault in western Iran (modified from Bayati et al., 2017). Inset map is a simplified geological structural map of Iran (Stöcklin and Nabavi, 1973). in 1968 and it is to be considered as the southwestern part of the Iranian Volcanic rocks provide especially important insights because these micro-continent (Azizi et al., 2016; Hassanzadeh et al., 2008; Hosseini et better approximate magma compositions than do plutonic rocks, al., 2015). The SaSZ is 50–100 km wide and is delimited by the Zagros which are more affected by crystal accumulation and because struc- suture zone in the west and the Urumieh-Dokhtar magmatic arc tures such as pillows and interbedded marine sediments reveal de- (UDMA) in the east (Falcon, 1974; Stöcklin, 1968; Stöcklin and position in a marine environment. The Panjeh magmatic complex, Nabavi, 1973). It also separates Late Cretaceous ophiolites into Inner the object of this study, provides especially useful insights into this and Outer Belts (Moghadam and Stern, 2015). The SaSZ has been Jurassic SaSZ igneous activity because it is a well-preserved volcanic subdivided into northern and southern sectors (Eftekharnejad, 1981). complex. The southern part is dominated by Middle to Late Triassic metamorphic The Panjeh study area is located near the village of Kangareh in the rocks with minor Jurassic igneous rocks but Jurassic igneous rocks are northern SaSZ of northwestern Iran (Fig. 2a, b). The local basement con- more common in the northern SaSZ (Fig. 1). Jurassic igneous rocks of sists of the Songhor-Ghorveh metamorphic complex composed of mar- the SaSZ are generally interpreted as having formed at an active margin ble, greenschist and amphibolite (Azizi et al., 2015a). Fossils in the (e.g. Agard et al., 2005; Azizi et al., 2011, 2013; Azizi and Asahara, 2013; Songhor-Ghorveh metasedimentary rocks define a depositional age Berberian et al., 1982; Berberian and Berberian, 1981; Davoudian et al., from Late Triassic to Middle Jurassic (Hosseiny, 1999) in a marine 2008; Ghasemi and Talbot, 2006; Mahmoudi et al., 2011; Mohajjel et al., basin environment. Metamorphic basement in the study area is covered 2003; Mohajjel and Fergusson, 2014; Moinevaziri et al., 2015; Nadimi by unmetamorphosed Cretaceous sedimentary rocks (Hosseiny, 1999) and Konon, 2012; Shahbazi et al., 2010, 2014; Stöcklin and Nabavi, indicating metamorphism in Middle to Late Jurassic time (Azizi et al., 1973). However, this paradigm has been challenged by Hunziker et al. 2015a; Hosseiny, 1999). Considering the absence of Precambrian base- (2015) who infer formation in a Jurassic rift of some sort. One of the ob- ment, Azizi et al. (2015a) interpreted the Songhor-Ghorveh complex jectives of the present study is to shed light on this controversy. as an oceanic island arc remnant, metamorphosed during the Late Cim- An interesting feature of SaSZ Jurassic igneous rocks is that there is a merian orogeny. In Middle to Late Jurassic times (180–140 Ma), the progression of ages, from ~175 Ma in the SE to ~145 Ma in the NW Songhor-Ghorveh basement was intruded by magmatic complexes (Bayati et al., 2017). This progression is difficult to reconcile with forma- such as the 143.5 ± 1.3 to 147.5 ± 1.3 Ma Suffi Abad granite (Azizi et tion at a convergent plate margin, where igneous activity would be ex- al., 2011), as well as the Mobarak-Abad (Azizi and Asahara, 2013), pected to occur all along the margin at the same time, and to continue Ghalaylan (Azizi et al., 2015b) and Kangareh-Taghiabad gabbroic bodies for several millions or tens of millions of years. Such a protracted mag- (Azizi et al., 2015a). Many of these magmatic complexes are also cov- matic history along a well-defined magmatic front like those of modern ered by unmetamorphosed Cretaceous sedimentary rocks (see Azizi et magmatic arcs is not seen in the distribution of SaSZ igneous rocks. al., 2015a; Hosseiny, 1999). 366 H. Azizi et al. / Lithos 308–309 (2018) 364–380

Fig. 2. (a) Distribution of intrusive bodies in southwest of Ghorveh, which cut the metamorphic basement (after Hosseiny, 1999). (b) Simplified geological map of the Panjeh area (after Hosseiny, 1999; Azizi and Asahara, 2013; Azizi et al., 2015a) showing the distribution of Late Jurassic igneous rocks relative to Songhor-Ghorveh basement and the Kangareh-Taghiabad gabbroic complex.

The Panjeh volcanic complex is composed of basalts and andesites possible shear zone is beyond the scope of this paper and will be pre- and, together with the nearby 158 ± 10 Ma Taghiabad maficbody(to sented elsewhere. the NE), is intruded by the 148 ± 3 Ma Kangareh gabbroic complex Three main magmatic units can be recognized in the Panjeh volcanic (Fig. 2; Azizi et al., 2015a). The composite Panjeh-Kangareh-Taghiabad complex (Fig. 3): i) pillow lavas and associated autobreccias and tuff massif thus overlies and intrudes the local Songhor-Ghorveh metamor- (Fig. 4a, b, c), ii) columnarly jointed basalts (Fig. 4d) and iii) andesites phic basement (Azizi et al., 2015a). The contact between and microdolerites with massive structure (Fig. 4e). Panjeh complex pil- metasediments to the SE and Panjeh complex lavas is characterized by low lavas with autobreccias, hyaloclastite tuffs and highly vesiculated marbles interbedded with metabasites, schists and volcanic breccia. basaltic lava flows indicate submarine eruption. Columnarly-jointed ba- Low-grade metamorphism together with pervasive S-L tectonite fabric salts, as well as the overlying andesitic rocks, are locally zeolitized and is here preliminarily interpreted as evidence that the original deposi- otherwise affected by ocean-floor hydrothermal metamorphism. Only tional contact was modified by shearing. Further assessment of this the upper andesites show massive textures. The entire complex was H. Azizi et al. / Lithos 308–309 (2018) 364–380 367

Fig. 3. The Panjeh complex (view from ESE) is composed by pillow lavas and hyaloclastic materials (P + H), basalts with columnar-like jointing (CB) and massive andesitic rocks (A). Magmatic rocks overlie the metasediment tectonites (marbles and schists, M + S). The Panjeh Complex is intruded in the NNW by the Late Jurassic Kangarehgabbro. intruded by the 158 ± 10 Ma Taghiabad mafic body and by the 148 ± clinopyroxene, with magnetite and titanite as accessory minerals. Both 3 Ma Kangareh gabbroic complex. The overall sense of the Panjeh- clinopyroxene and hornblende are locally altered to chlorite and actin- Kangareh-Taghiabad massif is an unusually well preserved submarine olite. Groundmass is microcrystalline, shows mineral phases compara- volcano of Late Jurassic age. ble to phenocrysts and is altered to chlorite and actinolite. Andesites (Fig. 5c) show mineral assemblages comparable to those 3. Petrography of basalts plus minor quartz and sanidine, with textures characterized by few phenocrysts. Groundmass is microcrystalline with a mineral as- The Panjeh magmatic suite is composed by basaltic and andesitic semblage similar to phenocrysts. Local chlorite-actinolite alteration of volcanic rocks associated with minor andesitic/dioritic hypabyssal both phenocrysts and groundmass is observed. Microdiorite and doler- dykes (Fig. 5). Basalts show porphyritic textures (Fig. 5a, b) dominated itic dykes (Fig. 5d) are also reported from the Panjeh complex. These by plagioclase phenocrysts. Mafic minerals are hornblende and augitic- dykes present holocrystalline micro- to meso-crystalline ophitic

Fig. 4. Field photographs of mafic magmatic rocks from the Panjeh Complex: (a) outcrops of basaltic pillow and mega-pillow; (b) zeolitized hyaloclastic breccia from pillow lavas; (c) stratified and metamorphosed fine hyaloclastic material (meta-tuff layers); (d) example of columnar-like jointing in basalts with evidence of hydrothermal alteration and zeolitization; (e) massive andesite body constituting the upper part of the Panjeh complex. 368 H. Azizi et al. / Lithos 308–309 (2018) 364–380

Fig. 5. Photomicrographs of the Panjeh magmatic complex: (a–b) altered plagioclase-hornblende phenocrysts in a groundmass composed of plagioclase, hornblende, clinopyroxene, and opaque minerals in basalts; (c) clinopyroxene-plagioclase micro-phenocrysts in locally altered andesitic groundmass; (d) micro-diorite dyke with holocrystalline ophitic texture and pseudofluidal fabric locally highlighted by elongated plagioclase crystals. Abbreviations; Hbl = hornblende, Pl = plagioclase, Kf = alkali feldspars, Cpx = clinopyroxene. texture. Clinopyroxene is subordinate to plagioclase. However, inter- columns with cation-exchange resin (BioRad AG50W-X8, 200–400 growth and granophyric textures indicate cotectic crystallization of pla- mesh). gioclase and clinopyroxene for these dikes. Plagioclase crystals are Trace element concentrations were analyzed using the ICP-MS locally oriented, thus indicating the magmatic anisotropy of these intru- (Agilent 7700x) at Nagoya University. Isotope ratios of Sr and Nd were sive dykes. measured by thermal ionization mass spectrometers (TIMS; a VG-Sec- tor 54-30 and a GVI IsoProbe) at Nagoya University. Measured Nd and Sr isotope ratios were corrected for fractionation based on 4. Analytical techniques 146Nd/144Nd = 0.7219 and 86Sr/88Sr = 0.1194, respectively. NIST- SRM987 and JNdi-1 (Tanaka et al., 2000) were adopted as standards Thirteen andesites, seven basalts and three andesitic/micro-dioritic for 87Sr/86Sr and 143Nd/144Nd ratios, respectively. Averages and 1SE for dikes were selected for whole-rock chemical analyses and zircon U-Pb isotope ratio standards, JNdi-1 and NIST-SRM987, were 143Nd/144Nd dating that was carried out at Nagoya University. Analyses were carried = 0.512113 ± 0.00006 (n = 9), for 87Sr/86Sr = 0.710244 ± 0.000009 out following the procedures and workflow presented in Azizi et al. (n = 11). (2015a). Zircons for U-Pb dating were isolated from two Panjeh andesitic Major element concentrations of 23 samples were measured by X- rocks (SP15, SP17). Because of the low amount of zircons in these ray fluorescence (XRF) method using a ZSX Primus II (Rigaku Co., mafic rocks, up to 2 kg of each sample was crushed. After sieve selection Japan) at Nagoya University, Japan. Glass-beads for XRF analyses were (b250 μm) and pure water washing and drying, a magnetic separator prepared mixing 0.5 g of sampled powder with 5.0 g of lithium (equipped with neodymium magnet) was used to separate magnetic tetraborate. This mixture was then melted at 1200 °C for 15 min with minerals. Heavy minerals were then concentrated using bromoform a high-frequency bead sampler (Rigaku Co., Japan). (CHBr3) heavy liquid. Additional andesitic samples (4) were analyzed by XRF only for Zircons were selected by handpicking under microscope and then major and selected trace elements, their glass-beads were prepared placed in resin on a glass side. After polishing the glass slide, back- with a mixture of 1.5 g of sample powder and 6.0 g of lithium scattered electron (BSE) and cathodoluminescence (CL) images of zir- tetraborate. The loss on ignition (LOI) of the sample was measured con grains were obtained with a scanning electron microscope (JEOL from the sample powder weight in a quartz glass beaker in the oven JSM-6510LV) equipped with cathodoluminescence system (GATAN at 950 °C for 5 h. MiniCL) at Nagoya University. Prismatic crystals with no flaws or alter- 100 mg of rock powder for each sample was decomposed in a cov- ation textures/domains and shooting point for dating, were selected ered PTFE beaker using 3 ml of HF (50%) and 0.5–1mlHClO4 (70%) at based on BSE and CL observations. U-Pb dating was obtained with a 120–140 on a hotplate for 3 days until the powder was completely dis- laser ablation (LA, NWR213 Electro Scientific Industries) - inductively solved. After removing the PTFE cover, dissolved samples were dried at coupled plasma mass spectrometer (ICP-MS Agilent 7700x) at Nagoya 140 °C on a hotplate with infrared lamps up to 2 days. After this proce- University, Japan. A detailed description of the LA-ICP-MS analysis is dure, samples were dissolved in 10 ml of 2 to 4 M HCl and the resulting provided in Kouchi et al. (2015) and Orihashi et al. (2008). The ISOPLOT solution was analyzed for determination of trace element contents and v.4.15 program (Ludwig, 2012) was used for calculations of the Sr-Nd isotope ratios. Sr and Nd separation was carried out using cascade Concordia and ages, statistics, and for constructing plots. H. Azizi et al. / Lithos 308–309 (2018) 364–380 369

5. Results Zircons present prismatic bipyramidal elongated shape with oscilla- tory zoning typical of magmatic crystallization (Fig. 6), confirmed also 5.1. Zircon U-Pb dating by Th/U ratio always higher than 0.3. Mean ages obtained for zircons from SP15, SP17-1 and SP17-2 sam- Three andesitic samples (SP15, SP17-1 and SP17-2) were chosen for ples are 142.4 ± 6.8 Ma, 143.6 ± 2.8 Ma and 147.0 ± 3.7 Ma, respec- age determination. Approximately 100 zircon grains were separated for tively (Fig. 7a–i). Zircons from SP15 sample, furthermore, show two each sample. Representative CL images of zircon grains from the three comparable clusters of ages as highlighted by the concordia diagram: samples are shown in Fig. 6. Results of U-Pb dating of zircon grains are a first population with a mean age of 136.3 ± 2.0 Ma and an older one listed in Table 1. at 151.3 ± 4.5 Ma, respectively (Fig. 7a–c). A minor cluster of analyzed

Fig. 6. Cathodoluminescence (CL) images of selected zircons for samples SP-15 (a), SP-17-1 (b) and SP-17-2 (c). Zircons are characterized by prismatic bipyramidal elongated shapes, and show oscillatory zoning typical of a magmatic origin and crystallization. A minor sub-population of zircon grains contain inherited cores. Location of the LA-ICPMS laser spots (red circles) are indicated. (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.) 370 H. Azizi et al. / Lithos 308–309 (2018) 364–380

Table 1 LA-ICP-MS data of zircon grains from the Panjeh igneous rocks.

206 a 207 206 206 238 207 235 238 206 235 207 Sample name Th/U Pbc Pb/ Pb Error Pb/ U Error Pb/ U Error U- Pb age Error U- Pb age Error (%) ±2σ ±2σ ±2σ (Ma) ±2σ (Ma) ±2σ

a: SP15 SP15–01 1.69 0.95 0.0470 0.0035 0.0570 0.0015 0.369 0.029 357.1 9.2 319.1 25.2 SP15–02 1.29 n.d. 0.0576 0.0055 0.0640 0.0019 0.508 0.051 399.7 11.8 416.9 41.5 SP15–03b 0.28 n.d. 0.0453 0.0054 0.0239 0.0008 0.149 0.018 152.1 4.8 141.1 17.5 SP15–04 1.12 n.d. 0.0634 0.0120 0.0234 0.0012 0.205 0.040 149.1 7.4 189.0 36.8 SP15–05 0.45 0.02 0.0590 0.0037 0.0570 0.0014 0.464 0.032 357.2 8.7 386.8 26.3 SP15–06b 0.55 3.01 0.0385 0.0045 0.0239 0.0008 0.127 0.016 152.2 5.2 121.3 14.9 SP15–07 1.04 4.69 0.0283 0.0030 0.0231 0.0008 0.090 0.010 146.9 4.8 87.3 9.7 SP15–10 1.43 2.23 0.0300 0.0035 0.0208 0.0006 0.086 0.010 132.9 3.9 84.0 10.1 SP15–11b 0.26 n.d. 0.0496 0.0065 0.0211 0.0007 0.144 0.019 134.5 4.3 136.8 18.3 SP15–13b 0.95 0.96 0.0445 0.0052 0.0214 0.0006 0.131 0.016 136.6 4.1 125.4 15.2 SP15–14b 0.81 n.d. 0.0511 0.0061 0.0212 0.0006 0.149 0.018 135.2 4.1 141.3 17.5 SP15–16b 1.28 0.59 0.0473 0.0069 0.0243 0.0009 0.159 0.024 155.0 5.5 149.4 22.4 SP15–17 1.07 n.d. 0.0738 0.0119 0.0227 0.0010 0.231 0.039 144.8 6.5 211.1 35.4 SP15–19 0.37 n.d. 0.0508 0.0048 0.0364 0.0009 0.255 0.025 230.5 5.4 230.7 22.6 SP15–20 0.54 1.29 0.0650 0.0038 0.1116 0.0021 1.000 0.062 682.3 12.6 704.0 43.6 SP15–22 1.51 1.77 0.0333 0.0064 0.0215 0.0009 0.099 0.020 137.3 5.7 95.7 18.9 SP15–24 0.71 n.d. 0.0598 0.0046 0.0644 0.0014 0.531 0.042 402.4 8.5 432.4 34.5 SP15–25 0.72 4.83 0.0250 0.0057 0.0209 0.0012 0.072 0.017 133.6 7.4 70.8 16.7 SP15–27b 0.79 1.46 0.0492 0.0056 0.0233 0.0007 0.158 0.018 148.2 4.3 148.7 17.4 SP15–32b 1.75 1.49 0.0408 0.0036 0.0217 0.0006 0.122 0.011 138.2 3.6 116.8 10.9

b: SP 17–1 SP17–1-01 0.63 n.d. 0.0592 0.0114 0.0247 0.0012 0.201 0.040 157.1 7.5 186.2 37.0 SP17–1-02b 0.68 0.39 0.0458 0.0035 0.0223 0.0005 0.141 0.011 142.3 3.1 133.8 10.7 SP17–1-03 0.74 0.13 0.0573 0.0034 0.0798 0.0016 0.630 0.040 495.1 9.7 496.2 31.2 SP17–1-04b 1.10 n.d. 0.0481 0.0116 0.0223 0.0012 0.148 0.037 142.5 7.6 140.3 34.7 SP17–1-05b 0.99 n.d. 0.0519 0.0065 0.0221 0.0007 0.158 0.021 140.7 4.4 148.9 19.3 SP17–1-06b 1.14 0.46 0.0552 0.0088 0.0229 0.0009 0.174 0.029 145.7 5.9 162.8 26.9 SP17–1-08b 0.88 0.61 0.0504 0.0061 0.0228 0.0007 0.158 0.020 145.1 4.5 149.2 18.6 SP17–1-09 0.78 3.51 0.0236 0.0038 0.0227 0.0009 0.074 0.012 144.6 5.6 72.3 12.0 SP17–1-10b 0.89 1.31 0.0569 0.0041 0.0229 0.0006 0.180 0.014 146.1 3.6 167.8 12.7 SP17–1-11b 0.95 0.14 0.0572 0.0044 0.0216 0.0005 0.170 0.014 137.7 3.4 159.6 12.8 SP17–1-13 0.87 8.51 0.0258 0.0016 0.0214 0.0005 0.076 0.005 136.2 3.3 74.4 4.9 SP17–1-14b 2.01 2.11 0.0431 0.0047 0.0225 0.0007 0.133 0.015 143.3 4.4 127.2 14.4 SP17–1-17 0.95 n.d. 0.0659 0.0132 0.0247 0.0013 0.225 0.047 157.6 8.3 205.9 42.8 SP17–1-18b 0.70 n.d. 0.0515 0.0076 0.0238 0.0009 0.169 0.026 151.7 5.6 158.5 24.2 SP17–1-19 1.22 0.64 0.0463 0.0066 0.0244 0.0009 0.156 0.023 155.6 5.6 147.1 21.6 SP17–1-21 0.51 4.22 0.0125 0.0014 0.0214 0.0006 0.037 0.004 136.4 4.1 36.7 4.2 SP17–1-22 0.39 2.75 0.0286 0.0033 0.0238 0.0007 0.094 0.011 151.5 4.7 90.9 10.9 SP17–1-23 0.52 2.85 0.0283 0.0027 0.0240 0.0007 0.094 0.009 152.8 4.2 90.9 8.9 SP17–1-24b 3.25 2.02 0.0491 0.0030 0.0221 0.0005 0.150 0.010 141.0 3.3 141.7 9.2 SP17–1-25b 0.80 0.33 0.0499 0.0036 0.0226 0.0006 0.155 0.012 144.2 3.5 146.7 11.2 SP17–1-26b 0.56 0.43 0.0483 0.0055 0.0243 0.0008 0.162 0.019 155.0 4.8 152.4 17.9 SP17–1-27 1.36 2.48 0.0359 0.0053 0.0248 0.0009 0.123 0.019 158.1 6.0 117.5 17.8 SP17–1-29 3.48 19.66 0.0294 0.0016 0.0223 0.0006 0.090 0.006 142.1 3.7 88.0 5.4 SP17–1-30 0.71 2.34 0.0601 0.0068 0.0241 0.0008 0.200 0.023 153.5 5.2 184.8 21.7 SP17–1-31 0.50 3.42 0.0368 0.0040 0.0227 0.0007 0.115 0.013 144.7 4.4 110.7 12.4 SP17–1-32 0.54 0.27 0.0522 0.0052 0.0281 0.0008 0.202 0.021 178.7 4.9 187.1 19.3 SP17–1-33 3.04 4.66 0.0302 0.0021 0.0217 0.0005 0.090 0.007 138.1 3.2 87.7 6.4 SP17–1-35 1.47 6.30 0.0037 0.0004 0.0223 0.0006 0.011 0.001 142.0 4.1 11.3 1.3 SP17–1-36 0.88 n.d. 0.0627 0.0080 0.0236 0.0008 0.204 0.027 150.5 5.2 188.5 24.9 SP17–1-37 0.83 n.d. 0.0682 0.0122 0.0252 0.0014 0.237 0.044 160.6 8.6 216.0 40.3 SP17–1-38 0.61 0.33 0.0626 0.0043 0.0888 0.0030 0.766 0.059 548.2 18.6 577.5 44.1 SP17–1-39 0.78 n.d. 0.0584 0.0078 0.0249 0.0011 0.201 0.028 158.7 6.8 185.8 25.9 SP17–1-40 0.20 0.88 0.0506 0.0032 0.0538 0.0018 0.376 0.027 338.0 11.2 324.0 23.1 SP17–1-41b 0.95 0.03 0.0495 0.0032 0.0218 0.0007 0.149 0.011 139.0 4.6 140.9 10.2 SP17–1-42 0.76 0.25 0.0597 0.0093 0.0250 0.0012 0.206 0.033 159.1 7.5 189.9 30.8 SP17–1-43b 0.97 0.60 0.0510 0.0049 0.0216 0.0008 0.152 0.016 137.5 5.1 143.2 14.8 SP17–1-44b 1.31 n.d. 0.0472 0.0038 0.0242 0.0008 0.158 0.014 154.4 5.3 148.6 13.1 SP17–1-45 1.61 3.10 0.0321 0.0039 0.0235 0.0010 0.104 0.013 149.7 6.1 100.6 12.9

c: SP 17–2 SP17–2-01 1.01 7.06 0.0441 0.0031 0.0241 0.0008 0.147 0.011 153.7 4.9 139.2 10.7 SP17–2-02b 1.08 0.41 0.0425 0.0034 0.0240 0.0007 0.141 0.012 152.6 4.5 133.6 11.4 SP17–2-04b 0.65 n.d. 0.0569 0.0072 0.0243 0.0009 0.191 0.025 155.0 5.9 177.3 23.4 SP17–2-05b 1.42 n.d. 0.0544 0.0054 0.0219 0.0007 0.164 0.017 139.4 4.6 154.1 16.2 SP17–2-06 0.33 1.57 0.0616 0.0035 0.1466 0.0041 1.246 0.079 881.9 24.8 821.6 52.4 SP17–2-07 0.48 0.57 0.0722 0.0038 0.1665 0.0046 1.657 0.098 992.9 27.4 992.3 58.6 SP17–2-08 2.77 17.00 0.1644 0.0160 0.0247 0.0013 0.560 0.062 157.4 8.0 451.7 49.6 SP17–2-10 0.51 1.63 0.0447 0.0049 0.0831 0.0040 0.512 0.061 514.4 24.7 419.5 50.1 SP17–2-12 1.02 3.12 0.0234 0.0040 0.0245 0.0013 0.079 0.014 155.7 8.5 77.0 13.8 SP17–2-13b 0.89 0.67 0.0507 0.0044 0.0244 0.0011 0.170 0.017 155.2 7.0 159.8 15.7 SP17–2-14 0.48 0.82 0.0532 0.0088 0.0293 0.0016 0.215 0.037 186.2 10.4 197.6 34.4 H. Azizi et al. / Lithos 308–309 (2018) 364–380 371

Table 1 (continued)

206 a 207 206 206 238 207 235 238 206 235 207 Sample name Th/U Pbc Pb/ Pb Error Pb/ U Error Pb/ U Error U- Pb age Error U- Pb age Error (%) ±2σ ±2σ ±2σ (Ma) ±2σ (Ma) ±2σ

SP17–2-15 0.64 0.96 0.0665 0.0071 0.0238 0.0012 0.218 0.026 151.6 7.4 200.5 23.4 SP17–2-16 0.26 0.64 0.0549 0.0028 0.0917 0.0039 0.694 0.046 565.4 24.0 534.9 35.7 SP17–2-17b 0.77 n.d. 0.0519 0.0051 0.0238 0.0011 0.170 0.018 151.7 7.0 159.7 17.3 SP17–2-18b 0.71 n.d. 0.0529 0.0066 0.0236 0.0012 0.172 0.023 150.5 7.4 161.5 21.6 SP17–2-22 0.99 4.50 0.0327 0.0055 0.0231 0.0011 0.104 0.018 147.0 7.3 100.3 17.7 SP17–2-23 0.85 3.54 0.0457 0.0081 0.0226 0.0012 0.143 0.026 144.2 7.6 135.3 25.0 SP17–2-24 1.50 1.05 0.0490 0.0039 0.0254 0.0008 0.172 0.015 161.8 5.2 160.9 13.7 SP17–2-25 1.14 12.40 0.0101 0.0007 0.0207 0.0007 0.029 0.002 132.2 4.4 28.8 2.2 SP17–2-26 1.71 3.52 0.0195 0.0025 0.0228 0.0009 0.061 0.008 145.1 5.5 60.4 8.1 SP17–2-27 0.92 14.80 0.0269 0.0033 0.0240 0.0012 0.089 0.012 153.1 7.7 86.7 11.4 SP17–2-28b 0.96 0.74 0.0485 0.0035 0.0231 0.0006 0.155 0.012 147.5 4.0 146.0 11.3 SP17–2-29 0.70 3.09 0.0339 0.0041 0.0232 0.0008 0.108 0.014 147.7 5.2 104.3 13.2 SP17–2-30b 0.69 1.55 0.0447 0.0046 0.0228 0.0007 0.141 0.015 145.6 4.6 133.7 14.3 SP17–2-31 0.44 1.51 0.0518 0.0066 0.1000 0.0037 0.714 0.094 614.4 22.9 547.2 72.2 SP17–2-32 0.26 n.d. 0.0575 0.0037 0.0647 0.0017 0.513 0.035 404.2 10.5 420.3 29.1 SP17–2-33b 1.13 0.75 0.0442 0.0034 0.0226 0.0006 0.137 0.011 143.9 3.9 130.8 10.7 SP17–2-35b 2.20 2.15 0.0425 0.0036 0.0224 0.0007 0.131 0.012 142.5 4.2 124.9 11.2 SP17–2-36 1.02 2.83 0.0341 0.0036 0.0234 0.0008 0.110 0.012 149.2 4.8 106.0 11.8

a Percentage of 206Pb contributed by common Pb is on the basis of 204Pb. Value of common Pb was assumed by Stacey and Kramers (1975) model. n.d. = not detection of 206Pb. b Points which are used for Concordia diagram.

Fig. 7. Concordia, average and histogram of ages for samples SP-15 (a–c), SP-17-1 (d–f) and SP-17-2 (g–i). 372

Table 2 Major and trace element concentrations of the Panjeh igneous rocks.

Rock Andesitic group Basaltic group Dioritic dike type

Sample Unit IR-P1 IR-P4 IR-P7 IR-P9 IR-P13 IR-P14 IR-P15 IR-P23 IR-P24 SP-15a SP-16a SP-17a SP-18a IR-P11 IR-P16 IR-P21 IR-P27 IR-P28 IR-P29 IR-P30 IR-P10 IR-P25 IR-P26

Latitude (N) 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 35° 06′ 25.2″ 37.2″ 36.0″ 34.2″ 43.1″ 13.0″ 09.0″ 27.2″ 29.4″ 04.1″ 06.3″ 09.3 10.4″ 31.2″ 58.9″ 28.7″ 43.3″ 44.7″ 43.7″ 43.3″ 46.2″ 34.2″ 43.0″

Longitude (E) 47° 31′ 47° 31′ 47° 31′ 47° 31′ 47° 32′ 47° 32′ 47° 32′ 47° 32′ 47° 32′ 47° 32′ 47° 32′ 47° 32′ 47° 32′ 47° 31′ 47° 32′ 47° 32′ 47° 34′ 47° 34′ 47° 34′ 47° 34′ 47° 31′ 47° 32′ 47° 32′ 27.6″ 48.0″ 56.4″ 59.4″ 29.1″ 24.0″ 28.0″ 25.9″ 23.4″ 12.5″ 06.7″ 02.0″ 0.4 46.8″ 40.0″ 44.6″ 28.0″ 29.7″ 36.2″ 28.5″ 59.4″ 26.0″ 25.1″

SiO2 % 62.8 57.9 54.0 53.9 64.3 52.6 56.3 54.6 56.2 55.9 60.9 56.5 57.6 51.9 47.7 46.9 43.4 46.8 44.8 50.9 60.3 56.8 56.9 TiO2 % 0.82 1.14 0.97 1.01 1.00 0.77 1.23 1.47 0.97 1.30 0.97 1.19 1.05 1.22 1.35 1.23 1.63 1.84 1.75 2.78 1.18 1.34 1.05 Al2O3 % 16.5 15.4 13.7 16.8 14.8 16.9 16.0 14.8 17.0 15.6 14.0 15.0 15.1 16.4 17.6 15.7 15.9 14.8 14.1 15.6 15.7 15.8 16.8 Fe2O3 % 7.32 7.34 6.67 6.94 6.63 7.29 7.76 8.45 8.07 8.03 5.43 7.49 5.76 8.91 9.66 10.6 14.0 13.8 13.9 13.0 7.16 7.58 6.74 MnO % 0.14 0.15 0.20 0.12 0.06 0.17 0.17 0.13 0.13 0.15 0.12 0.14 0.13 0.14 0.14 0.16 0.19 0.20 0.19 0.20 0.12 0.15 0.14 MgO % 1.97 2.31 2.55 4.42 2.26 6.93 2.38 3.74 0.93 2.23 2.28 1.60 2.11 6.08 7.61 9.20 11.0 11.13 11.1 5.13 3.27 2.43 2.40 CaO % 3.26 7.82 15.9 6.90 2.69 6.90 6.63 6.77 6.23 4.87 6.80 5.52 8.58 8.92 10.8 10.9 9.55 8.29 7.45 8.82 4.78 5.37 4.34 Na2O % 1.92 3.76 0.44 3.01 2.20 4.48 4.89 4.76 5.57 5.03 3.46 5.54 2.45 3.62 2.53 1.53 1.65 1.74 2.63 3.66 4.71 5.97 5.5 K2O % 2.69 2.25 2.61 2.54 4.26 1.14 2.30 3.01 2.28 3.24 3.02 2.50 3.59 1.15 0.85 1.4 0.12 0.16 0.33 1.03 2.14 2.56 3.71 P2O5 % 0.17 0.34 0.27 0.24 0.17 0.20 0.37 0.61 0.39 0.38 0.28 0.41 0.32 0.22 0.16 0.15 0.20 0.25 0.21 0.69 0.30 0.41 0.34 .Aiie l ihs308 Lithos / al. et Azizi H. LOI % 0.92 2.91 1.50 1.05 1.62 1.76 1.00 3.82 1.25 2.65 1.61 2.03 1.38 1.58 1.86 2.27 2.79 3.66 2.00 1.25 1.22 Total % 97.7 99.3 100.2 97.4 99.4 99.0 99.7 99.3 101.7 98.0 99.9 97.5 98.7 99.9 100.0 99.7 99.9 101.8 100.2 103.8 101.0 99.6 97.8 Mg# 34.7 38.3 43.0 55.7 40.2 65.2 37.7 46.6 18.5 35.3 45.3 29.6 42.0 57.4 60.8 63.1 60.7 61.4 61.1 43.9 47.4 38.7 41.2 V ppm 131 134 128 165 135 155 133 155 117 172 204 205 210 134 236 274 131 146 231 Cr ppm 134 79.0 173 139 132 491 550 98.2 49.1 130 146 108 148 226 309 552 563 91.4 492 93 63.7 58.4 485 Co ppm 17.1 16.1 15.9 20.6 18.2 22.9 13.9 19.2 9.33 15 12 11 11 31.9 42.2 48.7 61.9 14.1 61.4 33.4 13.5 15.3 54.2 Ni ppm 50.5 29.5 34.4 38.8 58.7 45.5 32.1 29.8 13.7 14 16 11 24 54.1 112 237 209 32.5 282 33.8 23.5 16.3 240 Cu ppm 9.1 32.3 33.5 40.8 6.6 4.5 22.8 3.7 21.7 2 9 42 5 51.8 64.2 10.2 75.2 8.49 82.2 52.4 3.58 6.58 18.1 – Zn ppm 68.7 86.5 185 89.0 173 124 106 89.9 97.2 96 82 90 71 71.8 78.2 109 98.7 84.1 103 114 102 80.7 109 364 (2018) 309 Ga ppm 21.7 24.7 21.7 19.1 19.7 17.0 25.8 23.1 25.6 24 18 21 21 17.3 18.9 16.8 18.2 28.8 19 24.9 25.8 26.1 18.3 Rb ppm 143 67.2 100 111 140 41.5 70.6 62.9 70.9 81 104 65 113 33.1 40.0 92.8 2.94 88.7 9.41 36.3 78.0 54.5 9.01 Sr ppm 180 717 1147 535 212 1470 1166 806 1112 1004 582 1551 788 326 784 876 322 1167 195 385 915 731 169 Y ppm 22.1 25.3 21.1 20.2 17.7 15.7 24.0 19.5 22.7 25 23 24 25 22.3 13.8 12.9 15.7 26.0 18.4 39.3 26.1 24.7 19.5 –

Zr ppm 187 18.0 132 12.4 17.6 81.8 272 29.2 26.2 264 213 246 230 44.4 12.8 66.7 14.5 267 8.7 21.4 9.56 25.0 103 380 Nb ppm 15.5 31.1 23.3 16.2 19.7 8.02 33.1 17.4 19.9 23 22 19 22 10.2 9.70 7.79 12.8 37.2 14.0 29.1 27.9 36.6 15.8 Cs ppm 10.4 3.06 2.30 8.64 8.29 9.34 2.53 2.93 1.84 1.44 11.2 23.7 0.24 1.82 1.35 1.36 15.0 0.710 0.21 Ba ppm 318 507 401 470 403 404 572 1060 910 920 493 695 596 135 88.8 134 47.0 1285 87.4 229 593 711 24.9 Hf ppm 5.31 0.81 3.64 0.55 0.61 2.48 6.88 1.47 1.63 1.64 0.570 1.92 1.08 7.20 0.825 1.61 0.35 1.32 2.87 Ta ppm 1.07 2.01 1.29 1.05 1.32 0.47 1.93 1.10 1.29 0.75 0.78 0.56 0.95 3.30 1.06 2.04 1.80 2.44 1.29 Pb ppm 9.39 10.8 21.7 18.3 13.9 23.0 16.1 8.05 9.53 248 220 145 26 5.87 6.300 3.04 2.14 12.8 3.18 4.5 11.4 10.5 7.47 Th ppm 11.7 9.32 9.02 6.44 11.3 5.05 8.99 9.14 10.2 13 8 8 10 5.96 0.89 0.87 1.09 10.0 1.05 2.93 8.53 8.16 1.32 U ppm 2.37 1.83 2.52 0.96 1.58 1.11 3.08 2.35 2.53 1.04 0.15 0.22 0.21 2.71 0.20 0.680 1.35 2.91 0.44 La ppm 32.4 51.4 40.8 26.9 32.3 21.1 50.2 42.3 41.9 14.9 8.32 7.67 11.2 49.3 11.6 34.0 58.3 42.4 14.6 Ce ppm 68.2 97.1 73.7 53.1 66.2 40.8 100 89.9 85.1 31.4 19.4 17.8 24.3 96.5 26.6 72.7 105 85.9 31.7 Pr ppm 7.53 10.9 8.28 6.0 7.51 4.65 11.6 11.3 10.5 3.83 2.59 2.36 3.09 10.9 3.51 8.86 11.8 10.0 4.02 Nd ppm 28.7 41.7 31.5 23.3 28.8 18.2 45.1 47.3 40.2 16.0 11.7 10.4 13.5 41.6 15.6 36.8 44.9 39.1 17.7 Sm ppm 5.54 7.36 5.70 4.54 5.48 3.47 7.87 8.28 6.86 3.64 2.78 2.57 2.98 7.39 3.73 7.89 7.94 6.65 4.02 Eu ppm 1.34 2.19 1.62 1.34 1.10 1.07 2.43 2.41 1.90 1.17 1.01 1.01 1.28 2.08 1.35 2.41 2.75 2.16 1.15 Gd ppm 5.04 6.32 5.09 4.38 4.83 3.32 6.49 6.31 5.71 4.05 3.10 2.79 3.39 6.35 4.19 8.24 6.86 5.96 4.40 Tb ppm 0.739 0.868 0.692 0.65 0.680 0.484 0.86 0.778 0.785 0.656 0.484 0.438 0.538 0.883 0.643 1.271 0.921 0.838 0.661 Dy ppm 4.41 5.06 4.07 3.99 3.93 2.98 4.90 4.15 4.70 4.25 2.92 2.70 3.31 5.17 4.02 7.76 5.33 5.02 4.04 Ho ppm 0.875 0.975 0.805 0.795 0.725 0.624 0.911 0.761 0.903 0.874 0.554 0.538 0.649 0.98 0.739 1.54 1.02 0.942 0.793 Er ppm 2.42 2.64 2.19 2.23 1.98 1.74 2.56 1.98 2.53 2.49 1.49 1.44 1.72 2.82 1.97 4.26 2.79 2.595 2.14 Tm ppm 0.354 0.371 0.305 0.303 0.265 0.246 0.359 0.261 0.343 0.358 0.191 0.201 0.231 0.397 0.264 0.600 0.367 0.363 0.290 Yb ppm 2.37 2.31 2.00 1.93 1.61 1.54 2.37 1.59 2.30 2.33 1.14 1.25 1.37 2.65 1.50 3.67 2.44 2.25 1.83 Lu ppm 0.331 0.316 0.285 0.269 0.218 0.225 0.355 0.207 0.305 0.339 0.146 0.173 0.182 0.373 0.197 0.509 0.347 0.305 0.252

a Samples only measured by XRF for major and trace elements. H. Azizi et al. / Lithos 308–309 (2018) 364–380 373

Fig. 8. (a) Total alkalis versus SiO2 diagram (after LeMaitre et al., 2002), compared with available data from the nearby Late Jurassic complexes (references in text). All the major elements data have been recalculated to 100 wt% on anhydrous basis with FeO* as total FeO; (b) plot of K2O vs. SiO2 (Peccerillo and Taylor, 1976) with subdivision of volcanic series in low-K, medium-K, high-K and shoshonite.

zircons present inherited structured cores with rounded shape showing ranging 13.7–17.6 wt%, and Mg# (molar Mg/[Mg + Fetot]=18–65) ages from 500 to 330 Ma. with Na2O+K2O up 9.2 wt% (Na2O is generally higher than K2Owith No zircons were obtained from basaltic lava samples. However, fos- average values of 3.5 wt% and 2.1 wt%, respectively). sils in interlayered sediments for the Ghorveh and Songor area confirm We note that less-evolved basalt (SiO2 b 47 wt%, in Table 2) show the Jurassic ages. In addition, Panjeh basalts show petrological and geo- high contents of MgO (9.7–13.14 wt%) suggesting that there are some chemical features overlapping those of layered basalts from nearby primitive melts. However, the high TiO2 (1.22–2.78 wt%) contents and Taghiabad basaltic complex, with a similar age (Azizi et al., 2015a). the low Al2O3/TiO2 (9.75–13.1) ratios exclude any relationship to komatiite (e.g. Arndt and Jenner, 1986; Gao and Zhou, 2013; Redman 5.2. Geochemistry and Keays, 1985). On the total alkali versus silica (TAS) diagram (LeMaitre et al., 2002), The chemical compositions of 23 basaltic and andesitic samples from Panjeh Complex samples straddle the subalkaline-alkaline field bound- the Panjeh mafic complex were investigated for major and trace ele- ary spanning from basalts to trachyandesites and dacites (Fig. 8a). In the ment compositions. Data are shown in Table 2 and are graphically com- K2O vs. SiO2 diagram (Peccerillo and Taylor, 1976)samplesvaryinaffin- pared to recent analyses of nearby Jurassic magmatic complexes (Fig. 2) ities according to silica content from low-K basalts (tholeiites) to of Kangareh-Taghiabad (Azizi et al., 2015a), Ghalaylan (Azizi et al., shoshonitic andesite, with many samples plotting in the medium-K 2015b), Ebrahim-Attar granite (Azizi et al., 2016) and Mobarak-Abad and high-K fields (Fig. 8b). (Azizi and Asahara, 2013). Harker diagrams for both major (Fig. 9) and selected trace (Fig. 10) All the studied samples show basic to intermediate compositions elements, with SiO2 content as differentiation index, negatively corre-

(SiO2 ranging 43.4–64.3 wt%, with a mean value of 54.3 wt%), Al2O3 late with TiO2, Mg#, MnO and CaO, whereas Na2O and K2O correlate

Fig. 9. Major element Harker diagrams for the Panjeh and nearby Jurassic magmatic complex. 374 H. Azizi et al. / Lithos 308–309 (2018) 364–380

Fig. 10. Trace element Harker diagrams for the Panjeh and nearby Jurassic magmatic complex.

positively; near constant values are observed for Al2O3 (Fig. 9). Incom- diagram (Fig. 12c) Panjeh samples mostly plot above the MORB-OIB patible large ion lithophile elements (LILEs) such as Ba and Rb, together array. In the Th-Co diagram (Fig. 12d), Panjeh samples scatter widely with light rare earth elements (LREEs) such as La, increase with SiO2 across the fields of calc-alkaline (CA) up to the boundary with from mafic to intermediate rocks, whereas high field strength elements shoshonitic (H-K and SHO) series with a main distribution between (HFSEs) such as Nb, Zr, Y and Yb (this last one representing heavy rare OIB-like and back-arc basalts (BABB) fields (Hastie et al., 2007). earth elements, HREEs) scatter with no appreciable correlation (Fig. 10). In Primitive Mantle (PM)-normalized diagrams (Sun and McDonough, 1989)(Fig. 11) Panjeh samples show strongly fractionated 5.3. Sr-Nd isotope ratios

REE patterns (Fig. 11a) enriched in LREE relative to HREE, with (La/Yb)N and (Dy/Yb)N mean values of 10.8 and 1.46, respectively. LREE content The Sr-Nd isotope ratios for 17 samples of Panjeh magmatic rocks increases from basalts to andesitic rocks. The Eu anomaly (Eu* = are given in Table 3. Based on the zircon U-Pb geochronological re- 1/2 [EuN/(SmN ×GdN) ]) is near absent (mean value of 0.97, ranging sults, the data are corrected for 145 Ma of radiogenic growth. The ini- 87 86 0.66–1.23). tial Sr/ Sr(145Ma) ranges from 0.7039 to 0.7061 for the basaltic In the PM-normalized trace-element diagram (Fig. 11b), analyzed rocks and from 0.7044 to 0.7076 for the andesitic lavas and dykes. samples are broadly enriched in incompatible elements such as Th, La, In the εNd(t) vs. 87Sr/86Sr(i) diagram (Fig. 13), Panjeh samples Ce and Nd. Depletion in HFSEs such as Nb, Ta and Ti is recognized in mostly are distributed along the Mantle Array, from the depleted all andesitic bodies (red circles). In contrast, basaltic samples (blue mantle (DM) toward the undepleted bulk silicate Earth (BSE) or squares) show no depletion in Nb-Ta. Andesitic/dioritic dykes (yellow Primitive Mantle (PM; Hofmann, 1988). Several samples plot right triangles) show variable HFSE depletion. Panjeh samples, moreover, of the mantle array, suggesting seawater alteration (Vidal et al., are characterized by a marked negative Zr anomaly (Fig. 11b); the sig- 1984). Nd isotopic signature generally track magma composition; nificance of this strong Zr-anomaly is unclear but may point to an im- in Panjeh complex mafic samples have higher εNd(t) and felsic sam- portant role for residual zircon, as expected to exist in continental ples have lower and negative εNd(t). crustal material.

In the TiO2 vs. V diagram (Fig. 12a; Shervais, 1982; Reagan et al., 2010), Panjeh samples with b1 wt% TiO2 show arc-like Ti/V ~20 whereas 6. Discussion samples with N1 wt% TiO2 show OIB-like Ti/V ~50 (Fig. 12a). In the Nb/Y vs. Zr/Y diagram (Fig. 12b; Fitton et al., 1997) Panjeh (and neighbor- Panjeh geochemical and geochronological data will be discussed hood) samples plot along and left of the MORB-OIB mantle array, hereafter in the light to understand the i) petrogenesis and ii) tectonic away from the field of arc basalts, however in the Th/Yb vs. Nb/Yb settings and implications. H. Azizi et al. / Lithos 308–309 (2018) 364–380 375

2015; Shervais, 2001); or by assimilation of continental crust by man- tle-derived mafic magmas (Pearce, 2008). These two possibilities are captured in Fig. 12c where Panjeh samples plot above the MORB-OIB array, shifted toward the volcanic arc array, in the field of “deep-crustal recycling” or slab recycling (after Pearce, 2008; Buchs et al., 2013; Rossetti et al., 2017). This behavior of Panjeh rocks could be explained as addition of Th or from subducted sediments or interaction with con- tinental crust via couple assimilation-fractional crystallization (AFC) processes (Pearce, 2008). Other evidence consistent with continental crustal assimilation is the transition from low-K mafic magmas (domi- nated by mantle melts) to high-K and shoshonitic evolved magmas (Fig. 8b): this behavior is not seen in intra-oceanic arcs, where all igne- ous rocks – basalt to rhyolite – plot in the same field, apparently con- trolled by fractionation (De Astis et al., 2000). Further indications that assimilation of continental crust contributed to magmatic evolution is provided by the isotopic data, where maficig- neous rocks show a mantle-like Nd signature while felsic igneous rocks demonstrate affinities with continental crust; this behavior cannot be explained by fractionation alone, it requires assimilation of an isotopi- cally evolved component such as the continental crust to produce felsic melts. Finally, round-shaped zircon grains with inherited structured cores with ages from 500 to 330 Ma are interpreted as xenocrysts picked up from underlying crust of this age or terrigenous sediments in the Ghorveh basin, although we note that there are no pre-Jurassic zircons in the nearby Kangareh-Taghiabad gabbroic bodies (Azizi et al., 2015a). The interpretation of continental crust laying beneath the Panjeh complex in the Jurassic time, is also consistent with the presence of Jurassic shallow water sediments beneath the complex. With respect to the mantle magma source, the εNd(t) of mafic Panjeh volcanics and gabbroic dikes are mostly ~+4, similar to the εNd(t) ~3–8 of Kangaraeh-Taghiabad mafic rocks, suggesting a moder- ately depleted mantle source (Fig. 13). Panjeh basalts have positive εNd(t) similar to Kangareh and Mobarak-Abad mafic rocks, although it is noteworthy that significant variations in εNd(t) are observed for some slightly fractionated basalts: IR-P27 and IR-P28 with Mg# ~61 Fig. 11. Primitive-Mantle normalized (after Sun and McDonough, 1989) REE diagram (a) have εNd(t) ~0 whereas other slightly fractionated basalts (IP-R11, fi and multi-element diagram (b) for the ma c samples from the Panjeh magmatic complex. −16, and −21) have εNd(t) ~3 to 4 (Tables 2, 3). This suggests some Petrological group and references: BABB, back arc basalts (Buchs et al., 2013; Pearce et al., 2005); FAB, forearc basalts (Ishizuka et al., 2011; Reagan et al., 2010); MORB, mid-ocean isotopic variability in the mantle source. Andesitic lavas and dioritic ridge basalts (Jenner and O'Neill, 2012); OIB, ocean island basalts (Buchs et al., 2013; dike have generally lower εNd(t) = +1.8 to −1.8; these overlap Willbold and Stracke, 2006). Island arc basalts after Buchs et al. (2013).(For Ebrahim-Attar and Ghalaylan granites and some magmatic rocks from interpretation of the references to color in this figure, the reader is referred to the web Taghiabad. Nd model ages (TDM1; DePaolo and Wasserburg, 1976) version of this article.) point to 0.7–1.0 Ga and 0.5–0.9 Ga for basalts and andesites (lavas and dykes) respectively, as expected for Cadomian (~0.5–0.6 Ga) subconti- nental lithospheric mantle beneath Iran, characterized by crust of the 6.1. Petrogenesis same age, as summarized by Moghadam et al. (2015). Further indications on the possible mantle source for Panjeh mafic The Panjeh mafic complex is composed of Late Jurassic (ca. 145 Ma) rocks can be inferred from immobile element geochemistry. In the basaltic and andesitic rock with medium- and high-K signatures respec- TiO2 vs. V system (after Shervais, 1982; Reagan et al., 2010), with TiO2 tively. Panjeh REE- and trace-element patterns are compared (in Fig. content in the range 0.5–3.0 wt% and Ti/V ratio ca. 50, Panjeh basalts 11a, b) to those of back-arc basalts (BABB; Pearce et al., 2005; Buchs et and andesites are distributed along the OIB array. This signature is al., 2013), forearc basalts (FAB; Reagan et al., 2010; Ishizuka et al., clear also in different immobile elements systems, such as Nb/Y vs. Zr/ 2011), mid-ocean ridge basalts (MORB; Jenner and O'Neill, 2012), Y(Fitton et al., 1997), in Th/Yb vs. Nb/Yb (after Pearce, 2008; Dilek ocean island basalts (OIB; Willbold and Stracke, 2006; Buchs et al., and Furnes, 2014)andThvs.Co(Hastie et al., 2007), where Panjeh 2013) and island arc basalts (after Buchs et al., 2013). Depletion in mafic rocks are always distributed at the boundary between OIB and HFSEs such as Nb, Ta and Ti, which is typical of subduction-zone BABB compositional fields. The OIB-signature is also shown in the Nb/ magmatism (e.g. Pearce, 2008; Pearce and Peate, 1995; Rossetti et al., Yb vs. TiO2/Yb diagram (after Pearce, 2008; Fig. 14a) and PM-normal- 2017; White and Patchett, 1984; Wilson, 1989) is recognized in all an- ized (N) La/Sm vs. Nb/La diagram (after Buchs et al., 2013; Fig. 14b). desitic bodies (red circles). In contrast, basaltic samples (blue squares) Condie (1999) concluded that La/Nb ~1.4 usefully separates oceanic pla- show no depletion in Nb-Ta and are comparable to OIB-like patterns. teau basalts (with lower La/Nb) from arc basalts (with higher La/Nb). Andesitic/dioritic dykes (yellow triangles) show variable behavior. Panjeh basalts have La/Nb ranging from 0.83 to 2.1, with a mean of These characteristics could be interpreted as melting of a MORB-OIB 1.16, significantly lower than expected for arc basalts. Comparable geo- mantle source that was contaminated by fluids released from a chemical features are recognized for the entire major coeval surround- subducting oceanic crust and sediment-derived melt (e.g. Azizi et al., ing magmatic complexes of Kangareh-Taghiabad, Ebrahim-Attar, 2015a; Dilek et al., 2007, 2008; Dilek and Furnes, 2011; Pearce and Ghalaylan and Mobarak-Abad (Azizi et al., 2015a, 2015b, 2016; Azizi Peate, 1995; Pearce and Stern, 2006; Rossetti et al., 2017; Saccani, and Asahara, 2013). 376 H. Azizi et al. / Lithos 308–309 (2018) 364–380

Fig. 12. Discrimination diagrams for basalt and andesite samples from Panjeh and nearby Jurassic magmatic complex; (a) TiO2 v. V (Reagan et al., 2010; Shervais, 1982); (b) Nb/Y v. Zr/Y (Fitton et al., 1997); (c) Nb/Yb v. Th/Yb diagram after Pearce (2008); (d) Th v. Co diagram (after Hastie et al., 2007). Petrological groups and references as in Fig. 10a and b; and Arc, volcanic arc (Reagan et al., 2008). Rock type: B, basalt; BA/A, basaltic andesites/andesites; CA, calc-alkaline series; D/R, dacite/rhyolite; E-MORB, enriched MORB; H-K, high-K series; IAT, island arc tholeiites; N-MORB, normal MORB.

Table 3 Sr-Nd isotope ratios for the Panjeh igneous rocks.

87 86 87 86 87 86 147 144 143 144 143 144 Sample Rb Sr Nd Sm Rb/ Sr Sr/ Sr ±1SE Sr/ Sr Sm/ Nd Nd/ Nd ±1SE Nd/ Nd εNd TDM1

(ppm) (ppm) (ppm) (ppm) (p) (i) (p) (i) (i) (Ga) Andesitic rock IR-P4 67.2 717 41.7 7.36 0.272 0.705636 0.000006 0.7051 0.107 0.512528 0.000004 0.51243 −0.5 0.85 IR-P7 100 1147 31.5 5.70 0.253 0.705231 0.000006 0.7047 0.109 0.512504 0.000004 0.51240 −1.0 0.90 IR-P9 111 535 23.3 4.54 0.602 0.706371 0.000007 0.7051 0.118 0.512575 0.000005 0.51246 0.2 0.87 IR-P14 41.5 1470 18.2 3.47 0.082 0.704705 0.000007 0.7045 0.115 0.512654 0.000004 0.51254 1.8 0.73 IR-P15 70.6 1166 45.1 7.87 0.175 0.704708 0.000007 0.7043 0.106 0.512557 0.000004 0.51246 0.1 0.80 IR-P23 62.9 806 47.3 8.28 0.226 0.705178 0.000006 0.7047 0.106 0.512529 0.000004 0.51243 −0.5 0.84 IR-P24 70.9 1112 40.2 6.86 0.185 0.704930 0.000007 0.7046 0.103 0.512457 0.000004 0.51236 −1.8 0.91

Basaltic rock IR-P11 33.1 326 16.0 3.64 0.294 0.704528 0.000006 0.7039 0.138 0.512804 0.000004 0.51267 4.3 0.65 IR-P16 40.0 784 11.7 2.78 0.148 0.706082 0.000006 0.7058 0.145 0.512746 0.000004 0.51261 3.1 0.83 IR-P21 92.8 876 10.4 2.57 0.307 0.704758 0.000007 0.7041 0.149 0.512739 0.000004 0.51260 2.9 0.90 IR-P27 2.94 322 13.5 2.98 0.026 0.704851 0.000006 0.7048 0.134 0.512567 0.000004 0.51244 −0.2 1.05 IR-P28 88.7 1167 41.6 7.39 0.220 0.706537 0.000007 0.7061 0.107 0.512559 0.000004 0.51246 0.1 0.81 IR-P29 9.41 195 15.6 3.73 0.140 0.706191 0.000008 0.7059 0.144 0.512738 0.000004 0.51260 2.9 0.84 IR-P30 36.3 385 36.8 7.89 0.273 0.705659 0.000007 0.7051 0.130 0.512738 0.000004 0.51262 3.2 0.71

Dioritic dike IR-P10 78.0 915 44.9 7.94 0.247 0.705251 0.000006 0.7047 0.107 0.512524 0.000005 0.51242 −0.6 0.85

Gabbroic dike IR-P25 54.5 731 39.1 6.65 0.216 0.705030 0.000007 0.7046 0.103 0.512763 0.000004 0.51267 4.2 0.51 IR-P26 9.01 169 17.7 4.02 0.154 0.707876 0.000007 0.7076 0.137 0.512763 0.000004 0.51263 3.5 0.73

The Nd and Sr natural isotope ratios were normalized based on the 146Nd/144Nd = 0.7219 and 86Sr/88Sr = 0.1194. Averages and 1SE for isotope ratio standards, JNdi-1 and NIST-SRM987, are 143Nd/144Nd = 0.512113 ± 0.00006 (n = 9) and for 87Sr/86Sr = 0.710244 ± 0.000009 (n = 11). The CHUR (Chondritic Uniform Reservoir) values, 147Sm/144Nd = 0.1967 and 143 144 87 86 87 86 Nd/ Nd = 0.512638 were used to calculate the εNd(0) (DePaolo and Wasserburg, 1976). The BABI (Basaltic Achondritic Best Initial) value, Sr/ Sr = 0.69899, and Rb/ Sr ratios of UR (Undifferentiated Reservoir) = 0.0827 were used. p = primitive and i = initial ratios. H. Azizi et al. / Lithos 308–309 (2018) 364–380 377

oceanic subduction for the northern SaSZ, however our isotope data in- dicate that Panjeh formed as part of Iran. Based on the whole-rock geochemistry and Sr-Nd isotopic ratios presented in this study and taking into account the lines of evidence outlined above, it is possible that Panjeh mafic calc-alkaline rocks were generated by the partial melting of the metasomatized mantle wedge above the subducting Neo-Tethyan slab (Dilek et al., 2007; Dilek and Furnes, 2011, 2014; Furnes and Dilek, 2017). REE- and trace-patterns together with immobile elements and Sr-Nd isotopic ra- tios highlight an affinity with OIB-type basalts. Panjeh and all the sur- roundings, in the εNd(t) vs. 87Sr/86Sr(i) diagram, plot in the major field of both ocean island- and active continental margin- basalts (OIB/ ACM) (e.g. Puga et al., 2010; Saccani et al., 2008). This OIB signature may reflect formation in a back-arc basin for Panjeh basalt and andesites. To summarize, the OIB-signature, in the light of an arc and back-arc system in a supra-subduction setting (in the meaning of Dilek et al., 2007; Dilek and Furnes, 2011, 2014) could be interpreted as an OIB- 87 86 Fig. 13. εNd vs. Sr/ Sr diagram for the Panjeh magmatic rocks compared with the type lithospheric mantle upwelling. This may have occurred beneath a mantle components HIMU, EM2 and DM (after Zindler and Hart, 1986); present day back-arc system (Burd et al., 2014; Holm et al., 2016; Søager et al., Bulk Earth and CHUR (Chondritic Uniform Reservoir) are also shown. Field of ocean island- and active continental margin-basalts (OIB/ACM) after Saccani et al. (2008) and 2015)(Fig. 15a). This scenario agrees with those proposed for the evo- Puga et al. (2010). Panjeh rocks are also compared with Late Jurassic surrounding mafic lution of Kangareh-Taghiabad (Azizi et al., 2015a) and Ghalaylan (Azizi complexes (see references in text). et al., 2016) complexes; models where a back-arc basin with both BABB- and OIB-signature developed in an extensional regime, before the colli- sion between the Songhor-Ghorveh island arc (Azizi and Asahara, 2013) 6.2. Tectonic settings and implications and the northern Sanandaj-Sirjan Zone at the end of Jurassic time.

There are two general interpretations for the tectonic setting of the 6.2.2. Rift/mantle plume interpretation composite Panjeh-Kangareh-Taghiabad volcano: it could have formed There are geometric problems with BABB interpretation for the in a convergent margin or in an intra-plate rift or plume setting. These Panjeh igneous complex and other Jurassic igneous rocks of the SaSZ. two possibilities are further explored below. First is that there is no known associated arc, how can there be a BABB without an associated magmatic arc and an accretionary complex? High-pressure (HP) complexes in the SaSZ were reported in the 6.2.1. Convergent margin interpretation Share-Kurd area (Davoudian et al., 2008) and Soghan locality Magmatism at convergent plate margins is part of subduction fac- (Angiboust et al., 2016). Ar-Ar ages point to Jurassic for the Share- tory processes at volcanic arc settings (e.g. Pichavant and Macdonald, Kurd eclogites and to Cretaceous for Soghan blueschist. However, both 2007; Tatsumi, 2005; Zhang et al., 2011). There is abundant literature of these HP complexes are located in the southern SaSZ and there is demonstrating how the partial melting of a mantle source, previously no evidence of accretionary complexes or HP-rocks in the northern metasomatized by slab melts and fluids, is responsible for producing SaSZ where Panjeh magmatic complex is. Second, there is a NW-ward most magmas at active convergent margin settings (e.g. Bryant et al., younging progression in SaSZ igneous rocks, from ~170 Ma in far SE to 2006; 2005, 2006; Lucci et al., 2016). This is the dominant interpretation ~145 Ma in NW. Igneous activity was brief at any one location along for SaSZ igneous activity starting from Middle Jurassic time (e.g. this trend. This is very different from arc or BABB magmatism where ig- Berberian et al., 1982; Berberian and Berberian, 1981; Davoudian et neous activity occurs contemporaneously along the arc or spreading al., 2008; Ghasemi and Talbot, 2006; Mohajjel et al., 2003; Nadimi and and continues for tens of millions of years. Hunziker et al. (2015) con- Konon, 2012). A recent study from Azizi et al. (2015a) proposed intra- sidered this magmatic younging progression of Jurassic granitoids as

Fig. 14. Discrimination diagrams for mafic rocks of the Panjeh magmatic complex: a) Nb/Yb vs. TiO2/Yb diagram (after Pearce, 2008) and b) Primitive Mantle-normalized (N) La/Sm vs. Nb/ La diagram (after Buchs et al., 2013). OIB field after Buchs et al. (2013); supra-subduction OIB after Gazel et al. (2011) and Buchs et al. (2013). 378 H. Azizi et al. / Lithos 308–309 (2018) 364–380

Fig. 15. Schematic conceptual models showing alternatives for the Late Jurassic geodynamic evolution of the Panjeh magmatic rocks. a) Back arc basin in an intra-oceanic arc and back-arc system in Neo-Tethys oceanic crust with lateral relations between identified mantle compositions (DM is depleted mantle). b) Extensional tectonic regime due to the upwelling of old metasomatized mantle and development of the Panjeh basin with injection of mafic lava. See text for further discussion. consequence of continental rifting or the evidence of an extensional SaSZ tectonic setting was like this, just to show a possible variation basin scenario, rejecting the Neo-Tethys subduction under Iran at Juras- on the basic plume/rift scenario (Fig. 15b). sic time at least for the northern SaSZ. Furthermore, chemical composi- tions of the most Jurassic SaSZ mafic lavas are consistent with an 7. Conclusions extensional setting (Nasr-Esfahani, 2012). Third, with respect to both northern and southern SaSZ, Jurassic igneous rocks of the Ghorveh The Panjeh mafic complex provides important insights for area show no evidence of Precambrian basement (Azizi et al., 2015a, reconstructing the Late Jurassic tectono-magmatic evolution of the 2015b). The Ghorveh area is characterized by Jurassic maficrocksinter- northern Sanandaj-Sirjan zone. Significant outcomes of this work are: bedded with marine limestone and chert, indicating a marine basinal (i) The Panjeh magmatic complex marks the location of a basaltic environment as might be expected for a continental rift. and andesitic volcano of Late Jurassic age (ca. 145 Ma, as deter- This study has firmly established the OIB-like signature of Panjeh mined by zircon U-Pb dating). Whole rock geochemistry of coe- Complex mafic igneous rocks and the contributions of continental val surrounding Late Jurassic magmatic complexes is similar to crust to the generation of andesitic magmas. However, in the light of Panjeh igneous complex; i) positive Nb-Ta anomaly, ii) behavior in (La/Sm)N vs. (Nb/La)N system (ii) Panjeh magmatic complex formed in a shallow marine shelf on and iii) Sr-Nd isotope signature of mafic uncontaminated Panjeh rocks, thinned continental crust. Interaction with crust affected it is reasonable to consider that the OIB-like nature usefully identifies magma evolution. the tectonic setting of these igneous rocks: they formed in a rift or (iii) Trace element geochemistry of mafic igneous rocks shows OIB- above a plume that affected Iran in Jurassic time. like characteristics and Sr-Nd isotope compositions indicate der- Details of the rift or plume responsible for Panjeh igneous com- ivation from Cadomian subcontinental lithospheric mantle. An- plex are not clear, nor are the reasons for the NW-ward migration desitic rocks show assimilation of continental crust. through time. An interesting Cenozoic analogue for Jurassic SaSZ (iv) It is controversial whether Panjeh igneous complex formed at a may be found in Coast Range volcanism in Neogene time in Califor- convergent margin or as part of a rift or plume. nia. The Farallon-Pacific spreading ridge was subducted in Oligocene time, leading to formation of the San Andreas transform plate boundary. A line of igneous activity propagated NNW along this Acknowledgements transform boundary, reflecting propagation of upwelling astheno- sphere along this migrating slab window (Liu and Furlong, 1992)at This work was supported by University of Kurdistan for fieldwork a rate of ~50 mm/y. Cenozoic igneous activity SaSZ NW propagation and Japan Society for the Promotion of Science (JSPS) KAKENHI Grant of igneous activity happened at 60 mm/y. We are not claiming that (Nos. 25303029, 17H01671). We really appreciate. Koshi Yamamoto, H. Azizi et al. / Lithos 308–309 (2018) 364–380 379

Simon Wallis, Kodai Mano and Fatemah Nouri for their help for LA-ICP- Fitton, J.G., Saunders, A.D., Norry, M.J., Hardarson, B.S., Taylor, R.N., 1997. Thermal and MS, BSE and CL images by SEM, and special thanks to Mehdi Alavi be- chemical structure of the Iceland plume. Earth and Planetary Science Letters 153, – fi 197 208. cause of his support in the eldwork and ensuing discussions. This is Furnes, H., Dilek, Y., 2017. Geochemical characterization and petrogenesis of inter- UTD Geosciences contribution number 1320. This version much mediate to silicic rocks in ophiolites: a global synthesis. Earth Science Reviews benefited from critical comments of reviewers Gültekin Topuz and 166, 1–37. Gao, J.F., Zhou, M.F., 2013. Generation and evolution of siliceous high magnesium basaltic Mohammad Maanijou and editor Nelson Eby. magmas in the formation of the Permian Huangshandong intrusion (Xinjiang, NW China). Lithos 162, 128–139. 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