Geochemistry and petrogenesis of the Feshark intrusion (NE Isfahan city)

Document Type : Research Article

Authors

• Ali Kananian ¹
• Fatemeh Ghahramani ¹
• Fatemeh Sarjoughian ²
• Jamshid Ahmadian ³
• Kazem Kazemi ¹

¹ Tehran

² University of Kurdistan

³ Payame Noor

10.22067/econg.v9i2.49676

Abstract

Introduction
Granitic rocks are the most abundant rock types in various tectonic settings and they have originated from mantle-derived magmas and/or partial melting of crustal rocks. The Oligo-Miocene Feshark intrusion is situated in the northeast of the city of Isfahan, and a small part of Urumieh–Dokhtar Magmatic Arc is between 52º21' E to 52º26'E and 32º50' N to - 32º53' N. The pluton has intruded into lower Eocene volcanic rocks such as rhyolite, andesite, and dacite and limestone.

Analytical methods
Fifteen representative samples from the Feshark intrusion were selected on the basis of their freshness. The major elements and some trace elements were analyzed by X-ray fluorescence (XRF) at Naruto University in Japan and the trace-element compositions were determined at the ALS Chemex lab.

Results
The Feshark intrusion can be divided into two phases, namely granodiorite with slightly granite and tonalite composition and quartz diorite with various quartz diorite and quartz monzodiorite abundant enclaves according to Middlemost (1994) classification. The quartz diorite show dark grey and are abundant at the western part of the intrusive rocks. Granodiorite are typically of white-light grey in color and change gradually into granite and tonalite. The granodiorite and granite rocks consist of quartz, K-feldspar, plagioclase, biotite, and amphibole, whereas in the quartz diorites the mineral assemblages between different minerals are very similar to those observed in the granodiorite. However, amphibole and plagioclase are more abundant and quartz and K-feldspar modal contents are lower than in the granodiorite whereas pyroxene occurs as rare grains. They are characterized as metaluminous to mildly peraluminous based on alumina saturation index (e.g. Shand, 1943) and are mostly medium-K calc-alkaline in nature (Rickwood, 1989).

Discussion
In the Yb vs. La/Yb and Tb/Yb variation diagrams (He et al., 2009), the studied samples show small variations in La/Yb and Tb/Yb ratios, suggesting fractional crystallization. Chondrite-normalized REE patterns (Sun and McDonough, 1989) of all the samples essentially have the same shape with light REE (LREE) enrichment, flat high REE (HREE) and significant negative Eu anomalies. All of the samples exhibit similar trace element abundance patterns, with enrichment in large ion lithophile elements (LILE) and negative anomalies in high field strength elements (HFSE; e.g. Ba, Nb, Ta, P, and Ti) compared to primitive mantle (Sun and McDonough, 1989). The enrichment of LILE and LREE relative to the HFSE and HREE along with Nb, Ta, and Ti anomalies display close similarities to those of magmatic arc granites (Pearce et al., 1984) and also negative Nb–Ti anomalies are thought to be related to the fractionation of Ti-bearing phases (titanite, etc.). Moreover, these are the typical features of arc and / or crustal contamination (Kuster and Harms, 1998), while the negative P anomalies should result from apatite fractionation. The increasing of Ba and slightly decreasing Sr with increasing Rb, indicate that plagioclase fractionation plays an important role in the evolution of the studied intrusion. Tectonic environment discrimination diagrams such as Nb vs. Y, Nb vs. Yb+Ta (Pearce et al., 1984) and Th/Yb vs. Ta/Yb (Pearce, 1983) with enrichment in the LILE and LREE relative to HFSE and HREE and negative anomaly in the Nb, Ti and Eu indicate that their initial magma is generated in the subduction zone related to an active continental margin setting. ‏The rocks genesis determining diagrams such as Nb vs. Nb/U (Taylor and McLennan, 1985), Ti vs. Ti/Zr (Rudnick et al. 2000), (La/Sm)cn vs. Nb/U (Hofmann et al., 1986), and Sr/Y vs. Y (Sun and McDonough, 1989) show that the magma was probably generated by partial melting of amphibolitic continental crust.

References
He, Y., Zhao, G., Sun, M. and Han, Y., 2009. Petrogenesis and tectonic setting of volcanic rocks in the Xiaoshan and Waifangshan areas along the southern margin of the North China Craton: Constraints from bulk-rock geochemistry and Sr-Nd isotopic composition. Lithos, 114(1-2): 186-199.
Hofmann, A.W., Jochum, K.P., Seufert, M. and White, W.M., 1986. Nb and Pb in oceanic basalts: new constraints on mantle evolution. Earth and Planetary Science Letters ,79(1-2): 33-45.
Kuster, D. and Harms, U., 1998. post – collisional potassic granitoids from the southern and northwestern parts of the late neoporterozoic East African Orogen: a review. Lithos. 45(1-4):177-195.
Pearce, J.A., 1983. The role of sub-continental lithosphere in magma genesis at destructive plate margins. In: C.J. Hawkesworth and M.j. Norry (Editors), continental basalts and mantle xenoliths. Shiva Publications, Nantwhich, pp. 230-249.
Middlemost, E.A.A. 1994. Naming materials in the magma/igneous rock system. Earth- Science Review. 37(3-4): 215–224.
Pearce, J.A., Harris, N.B.W. and Tindle, A.G., 1984. Trace element discrimination diagrams for the tectonic interpretation of granitic rocks. Journal of Petrology, 25(4): 956 – 983.
Rickwood, P.C., 1989. Boundary lines within petrologic diagrams which use of major and minor element. Lithos, 22(4): 247-263.
Rudnick, R.L., Barth, M., Horn, I. and McDonough, W. F., 2000. Rutile-Bearing Refractory Eclogites: Missing Link Between Continents and Depleted Mantle. Science, 287(5451): 278-281.
Shand, S.J., 1943. The Eruptive Rocks. 2nd edition. John Wiley, New York, 444 pp.
Sun, S.S. and McDonough, W.F., 1989. Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and processes. Geological Society, London, Special Publications, 42, pp. 313-345.
Taylor, S.R. and McLennan, S.M., 1985. The continental crust: its compositions and evolution. Blackwell, Oxford, 312 pp.

Keywords

• intrusive rock
• petrogenesis
• tectonic setting
• Feshark
• Isfahan
• Urumieh Dokhtar arc

20.1001.1.20087306.1396.9.2.4.2

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