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Ukrainian Journal of Ecology
UkrainianJournal of Ecology, 2017, 7(4), 316-324, doi: 10.15421/2017_122
ORIGINAL ARTICLE
Petrogenesis and Geochemical Properties of Dome-shaped Subvolcanic Complexes in Southwest of Shahrab (Northeast of Isfahan)
Mohammad Ali Arian1*, Alikhan Nasr Isfahani2, Afsaneh Ranjbar1
1 Islamic Azad University, Tehran North Branch, Iran 2 Islamic Azad University, Isfahan (Khoraskan) Branch *Corresponding author E-mail: m arian@iau-tb.ac Submitted: 04.11.2017. Accepted: 14.12.2017
The studied area is located in southwest of Shahrab village near Ardestan city. This zone is part of Uremia- Dokhtar magmatic belt. Outcrops composed of rhyolite and rhyodacite dome-shaped volcanic complexes are scattered in the studied area; some of which are exploited as ornamental stone. The main rhyolite minerals include quartz, plagioclase and alkali feldspar. Minor minerals include Apatite, Sphene and opaque minerals and of the secondary minerals in these rocks Christie, Chlorite, Epidote and calcite could be mentioned. Calcite exists in rocks in form of filler of micro-fissures. The ignimbrite presence in this group of rocks in form of xenolith is one of the features of this rock group. The main primary texture in rhyolite and rhyodacite is porphyritic and the secondary texture includes pull-apart, snow flake and spherulitic textures. Geochemical evidences indicate that these rocks are sub-alkaline, Calc-alkaline compositions with high potassium and meta-alumina. These rocks have negative EU anomaly that is the feature of acidic igneous rocks. The studied rocks show high enrichment of LREE and LILE elements. The primary magmas constituting these rocks have mantel origin raised under extreme compressional conditions on continental crust in a tectonic environment of volcanic arc. It seems that these rocks are formed in connection with continuance of volcanic activities associated with subduction of Neolithic oceanic plate beneath continental plate of Iran. Key words: Ardestan; sub-volcanic rocks; Calc-alkaline; Volcanic arc
Introduction
The distribution of these sub-volcanic groups is mostly in southwest of Shahrab village in southeast of Ardestan in Isfahan province. The geographical coordination of the studied area is 33° 04' 08" to 33° 11' 15" N latitude and 52° 23' 10" and 52° 32' 18" altitude (figure 1). The studied zone is part of Uremia- Dokhtar belt (figure1).
Sub-volcanic outcrops dating Oligocene have discontinued Eocene volcanic rocks of mainly basaltic to dacite compositions. In terms of composition, Eocene volcanic rock is in range of basalt to dacite; however, it has more andesite (Nasr Isfahan and Ahmadi, 1999). These outcrops are reported to be in southeast of Zafarqand or west of Rangan village and also in south Ardestan (northeast of Baqam villge) (Radfar, 1997). Generally, in Ardestan area, Oligocene volcanic activities are mainly acidic (Emami et al, 1992). With this group of rocks, Zeolite roundish shapes of ignimbrite can be observed. In this area of Aedestan, mining works on constructional and ornamental stones are under operation in form of opencast mining on outcrops of studied stones. In this study, petrologic characteristics and tectonic pattern governing sub-volcanic dome-shaped outcrops formation will be studied in south area of Shahrab village.
Geology of the area
The outcrop place of these sub-volcanic rocks is in southwest of 1:100000 geological map of Shahrab (northeast of Isfahan). Based on this map, the lithology composition of rhyolite and rhyodacite studied stones are reported to be in white color and porphyritic texture. Based on Bahroudi studies (1997) inside these stones, phenocrysts in form of quartz, alkali feldspar and plagioclase could be seen. Parts of this sub-volcanic unit are in form of rhyodacite, tuff and ignimbrite. The more acidic parts of this unit have been injected in mid and high Eocene stones, (Middle and upper Eocene) that is the subject of this study (Figure1).
Fig.1. Geological map of studied zone (quoted from Radfar 1997 with changes)
Fig. 2. Geological and constructional units (adopted from Eftekharnejad 1980) and the studied zone situation that is specified by star
Methodology
During field visits, 40 stone samples were extracted from various parts of dome-shaped sub-volcanic outcrops of rhyodacite and dacite. After investigation of manual samples, 34 thin sections were selected and after preparation with polarization microscope they were studied. 11 samples of healthy rhyolite and 2 xenoliths were chemically analyzed using ICP-MS and XRF in the Canada SGS laboratory (Table 1 and 2).
Table 1. Chemical analysis data related to main oxides through ICP-MS
Element Rj A1 Rj 1 Rj 2 Rj 8 Rj 11 Rj 14 Rj 15 Rj 16 Rj 21 Rj 24 Rj 28 Rj C1 Rj C2
SiO2 68.4 67.9 67.9 67.3 67.4 69.8 69.0 68.8 61.7 70.6 58.8 68.2 69.3
P2O5 0.06 0.06 0.05 0.05 0.06 0.05 0.06 0.05 0.05 0.06 0.16 0.07 0.07
Na2O 5.0 4.9 6.6 3.0 2.3 3.1 3.5 2.9 3.8 4.0 4.4 4.4 4.5
MnO 0.04 0.09 0.08 0.08 0.06 0.05 0.05 0.06 0.33 0.05 0.11 0.04 0.04
MgO 0.40 0.26 0.24 0.68 0.54 0.15 0.34 0.61 5.24 0.16 1.86 0.52 0.52
K2O 4.36 3.82 4.12 4.24 4.70 6.73 5.26 6.31 4.53 6.59 3.20 3.77 3.81
Fe2O3 2.75 2.82 2.81 2.67 2.73 2.64 2.53 2.63 4.94 2.55 3.63 2.76 2.84
Cr2O3 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01 <0.01
CaO 1.26 1.26 1.24 1.55 1.20 0.36 1.61 0.42 0.41 0.39 1.35 0.54 0.56
Al2O3 13.0 13.7 13.5 13.4 13.2 12.8 12.5 13.0 12.6 12.8 16.8 13.2 13.4
TiO2 0.35 0.36 0.37 0.34 0.35 0.34 0.32 0.35 0.38 0.34 0.52 0.35 0.35
LOI 1.69 2.24 1.88 2.43 1.92 0.87 2.46 1.39 4.47 0.90 2.59 1.18 1.17
Total 97.32 97.42 99.99 97.96 98.93 98.99 90.98 94.99 93.92 97.99 98.97 97.93 97.91
Moreover, specialized software such as Minpet and Igpet were used for analysis, calculation of norm and drawing of figures. Table 2. Chemical analysis data of minor elements through ICP-MS
Element Rj C2 Rj C1 Rj 28 Rj 24 Rj 21 Rj 16 Rj 15 Rj 14 Rj 11 Rj 8 Rj 2 Rj 1 Rj A1
Ba 730 710 680 920 660 850 840 890 800 940 750 670 720
Sr 120 110 210 100 100 100 130 90 130 110 100 100 130
Zn 38 38 125 32 365 24 20 30 34 56 34 36 34
Sum 97 9/5 5 95/7 9/3 7 97 97/6 9/6 7 96/7 95/9 96/7 9/7 6 9/9 6 96/8
Ag <1 <1 <1 <1 <1 <1 <1 <1 <1 <1 <1 <1 <1
Ce 49/1 4/4 9 64/2 4/9 0 53/7 38/8 4/2 7 46/9 45/4 46/2 4/8 6 4/7 5 45/3
Co 3/5 3/5 5/3 3/4 33/7 4 3 2/9 3/8 5/2 3/8 3/9 3/8
Cs 1/6 1 /5 2/3 3/9 3/9 2/5 2/4 3/8 4/1 4/9 4 4/5 1 /3
Cu 15 16 47 10 10 131 25 9 25 31 33 38 8
Dy 3/96 /02 4 5/59 /51 4 4/51 3/57 /78 3 4/27 3/73 3/94 /99 3 4 3/61
Eu 0/73 /73 0 1/34 /67 0 0/67 0/45 /67 0 0/62 0/71 0/74 /74 0 /78 0 0/65
Er 2/47 /57 2 3/6 /96 2 2/96 2/34 /45 2 2/86 2/45 2/41 2/6 /58 2 2/56
Ga 15 15 22 14 14 16 12 14 14 17 16 16 15
Gd 3/92 /79 3 5/43 /09 4 4/09 3/22 /58 3 3/78 3/7 3/52 /85 3 /68 2 3/42
Hf 6 6 6 6 6 6 6 6 5 6 6 6 6
Ho 0/75 0/8 1/17 /93 0 0/93 0/71 /79 0 0/86 0/81 0/76 /81 0 /77 0 0/78
La 25/4 26 33/4 1 /3 9 19/3 15 /8 2/9 3 24/2 52/3 26/8 2/5 4 2/6 4 24/4
Lu 0/36 /39 0 0/55 /42 0 0/42 0/37 /38 0 0/41 0/39 0/39 /39 0 /38 0 0/41
Mo <2 <2 <2 <2 <2 <2 <2 <2 <2 2 <2 <2 <2
Nb 11 11 12 13 13 12 11 12 11 11 11 11 12
Nd 19/6 1 /8 9 29/3 1 /8 8 18/8 16/8 1 /2 9 20/7 19/5 18/3 1 /1 9 1 /6 9 18/7
Ni 5 < <5 <5 <5 <5 <5 12 <5 <5 <5 <5 <5 <5
Pr 5/43 /42 5 7/62 /81 4 4/81 4/39 /09 5 5/48 5/39 5/25 /17 5 /27 5 5/12
Rb 109 111 90/5 184 184 166 144 184 135 136 133 120 124
Sm 3/7 3/7 5/8 % % 3/2 3/5 % 7/3 3/7 3/9 3/8 3/6
Sn 1 1 2 2 2 2 2 <1 1 <1 <1 2 <1
Ta 0/7 0/7 0/8 0/9 0/9 0/8 0/7 0/9 0/7 0/8 0/7 0/7 0/8
Tb 0/6 /65 0 0/91 /68 0 0/68 0/54 /59 0 0/69 0/54 0/6 0/6 /62 0 0/57
Th 11/6 1 /7 1 11 /8 1 /7 2 12/7 12/6 1 /3 2 13/5 11 /3 11 /7 12 1 /3 1 12/5
Tl 0/5 < </5 0 <0/5 </5 0 <0/5 <0/5 </5 0 <0/5 <0/5 <0/5 </5 0 </5 0 <0/5
Tm 0/35 /32 0 0/49 /41 0 0/41 0/33 /35 0 0/4 0/37 0/37 /34 0 /38 0 0/37
U 2/59 /65 2 3/07 /09 3 3/09 3/13 /98 2 3/05 2/68 2/88 /76 2 /53 2 2/78
V 29 29 53 36 36 40 33 35 34 37 33 36 26
W 1 1 2 2 2 2 1 2 1 2 2 2 1
Y 22/3 2/7 2 31 /5 2/1 7 27/1 22 2/4 2 25/5 22 22/1 2/9 2 2/9 2 22
Yb 2/5 2/4 3/7 3 3 2/5 2/7 2/7 2/7 2/5 2/6 2/6 2/7
Zr 216 213 225 240 240 214 211 216 201 212 226 23 232
Petrography
Petrologically, this stone is in the group of rhyodacite stones and constituted from main minerals including quartz, Plagioclase and feldspar alkali. Quartz crystals are abundantly seen in form of Phoenocrystal and microcrystal in stones. Phoenocrystal are usually Subhedral to Euhedral with corrosion gulf (figure3-a). The interesting phenomenon seen in these sections, are absorbed quartz that are also known as armored quartz. In such state, quartz is in the middle and feldspar alkali and quartz are in surrounding (figure3-b).
Fig. 3. Microscopic images of studied area: a. Quartz phenocrystal with Porphyritic texture suffering from corrosion gulf (PPL light), b) Quartz phenocrysts with reabsorption margin in the rhyolites of zone (XPL light)
In this group of stones, Microcytic Porphyritic to hyaluporphyritic could be observed (figure 4-a); moreover, Calcite of sponge texture is also seen (figure4-b). Tectonic forces lead to crushing and expansion of fractures and tracks in plagioclase phenocrysts and tracks parallel to traction-separation tissue are clearly obvious in plagioclase phenocrysts (figure4- c). Quartz has welded plagioclase crushes and other feldspars as cement and made shear texture (figure4-d).
Fig. 4. Microscopic images of the textures of zone: a) Microcytic Porphyritic to hyaluporphyritic (XPL light), b) sponge texture (XPL light), c) traction-separation texture (XPL light), d) shear texture (XPL light).
In terms of alteration studies, it can be said that some of the plagioclase phenocrysts are characterized by complete fading that is probably due to alteration (Fig. 5a). In some parts, feldspar alkali which is due to alteration has developed in the form of cement material and welded phenocrysts. In addition, the formation of calcite in the field indicate carbonation phenomenon (which is a kind of alteration) (Fig. 5b)
Fig. 5. Microscopic images of secondary textures; a) plagioclase phenocrysts with complete fading are clear (XPL light); b. Calcite formation in the background shows carbonation phenomenon (XPL light).
Geochemistry
One of the geochemical features of these rocks is enrichment from LILE elements similar to Rb (109-184 ppm) and Zr (201 -232 ppm) and enrichment from mobile elements such as Cs and Ba.
Based on classification figures of igneous rocks, the samples are placed in rhyolite zone in terms of chemical composition of stones (figure 6-a). In the proposed figure, Le Maitre et al (1989) show the samples of behavioral zone of semi-alkali or subalkali (figure 6-b). The samples placement in AFM figure (Irvine and Baragar, 1971) indicates their calc-alkaline feature (figure 6-c). According to the studies carried out on the stones of studied area and drawing of potassium rate determination figure, these samples are located in the range of stones of high potassium which in the figure, the zone of these stones is determined in K2O versus SiO2 (figure 6-d). The location of felsic specimens in A/CNK vs. A/NK and ACF figures (figure 7) shows their Metaloumin nature and their similarity with I-type granite. To investigate the patterns of minor elements and REE, normalized figures in respect to initial crust and chondrite are used. Normalized figure in respect to chondrite (figure 8-a) indicates a uniform smooth trend and undifferentiated pattern in distribution of JREE elements. While LREE has enrichment and differentiation (La/Yb)N=4.21 -7.2), Gd/Yb)N=1.01 -1.26 and Eu shows negative anomaly (Eu/Eu*= 0.48- 0.61). The separation of Feldspar from
felsic melt leads to negative anomaly of Eu (Sun and McDonough, 1989). The presence of enrichment and abundance of LREE elements could be due to melting of a small part of these stones or relatively enriched origin of alkali elements associated with Subduction areas. LREE enrichment to HREE might be associated with the minor minerals of Zircon and apatite (Pearce et al., 1984).
Na - Series
Fig. 6. a) Cox et al classification (1979) for igneous rocks, b) alkali vs. Silica alkali ((Le Maitre et al.,1989) for distinction of alkali and sub-alkali series zone, c) triangular figure of AFM where calc-alkaline series are separated from tholeiitic (Irvine and Baragar, 1971), d) weight percentage of K2O against weight percentage of Na2O of magma series of high potassium, containing potassium and containing sodium (Middlemost, 1985).
3.0 2.8 2.6 2.4 2.2 2.0 1.8 1.6 1.4 1.2 1.0 0.8 0.6
Z
0.4
Metaluminous Peraluminous
1
- Peralkaline 1
0.5 1.0
Fig. 7. A/CNK vs. A/NK diagram (Maniar and Piccli , 1989)
1.5
2.0
ACNK
In distribution figure of minor normalized elements compared to chondrite (figure 8-b), elements U, Th, Ba and LILE show high enrichment (for example for Rb, there is 1000 times enrichment); instead, a fall is seen compared to Ta and Nb and Sr which indicates the crust origin or extreme pollution with crust. This distribution pattern is special for arc calc-alkaline felsic magma.
b
d
1000
«J
r 100
- 10
~l I I I I I I I I I I 1 I r
a
.1
_i_I_I_I_I_I_I_I_I_I_I_I_I_I_I_
La Pr Eu Tb Ho Tm Lu
Ce Nd Sm Gd Dv Er Yb
1000 F
b
Cs Rb U Nb Sr Zr Tb Cr Ni Ta Ba Th Pb Li Ce Y Zn
Fig. 8. Spider figures; a) The samples of rhyolite rare earth elements normalized in terms of chondrite; b) samples of minor and rhyolite rare elements normalized in terms of Chondrite.
Tectonic- magma position
Harris et al (1986) classified Granitoid Magma in terms of tectonic area using minor elements. In these figures, the studied samples are located in volcano arc magma (VA) and due to plate subduction (figure9).
Fig. 9. The distinguishing figure of granite magma tectonic environment (Harris et al, 1986); a) based on Hf-Rb/10-Ta*3, b) based on Hf/Rb/30-Ta*3
Discussion and conclusion
Felsic sub-volcanic rocks in the studied area are classified in rhyolite rocks group in terms of mineralogy and chemical composition. The texture features in phenocrysts such as gulf texture in quartz, margined quartz, zoning in plagioclases and some corrosion in them and the presence of basic micropiles, all indicate chemical imbalance, magma quick swelling and sudden drop of pressure. These observations make clear the role of crust contamination or magma mix (Raymond, 2002). These sub-volcanic stones are geochemically sub-alkali with calc-alkaline nature, Metaloumin indicates negative EU anomaly, enriched of potassium. The studied rocks show high enrichment in terms of LREE and LILE elements.
Wilson (1989) believes that rhyolites of subduction zones are sub-alkaline. High potassium (K>4 weight percentage), iron enrichment (FeO/Mg>4.5) and silica are the signs of igneous rocks in thrust environment.
The specifications of subduction zone include enrichment of Ba, Rb, K and LREE compared to HREE and HFSE and decreasing Nb anomaly (Sajona et al, 1996). Nb values below 70 ppm are related to subduction zone (Green, 2006).
High potassium in these rocks might be due to increased contamination degree of crusts in continental active magma (Wilson, 1989; Brown et al, 1984). In the continental active margin zones, there is some relation between increased potassium and increased depth of Beniow plane (Miskovic and Francis, 2006). The researchers consider the reason as increased thickness of continental crust and its increased effect on changing initial magma composition (Scandl and Gorton, 2002). Tectonic-magma figures separating various tectonic environments confirm the formation in an active volcanic arc environment (Thompson, 1982; Martin, 1993).
Emami et al (1992) believe that Oligocene rhyolite in Ardestan are poured out due to continuation of Eocene rift in extend of Oligocene cracks; however, Moein Vaziri (2004) believes that extreme and expanded volcanism of Eocene and its continuation in a subduction regime led to mild magmatism in Oligocene and onward. He considers the origin of this magmatism as compression discharge of deep Eocene magma reservoirs. The studied sub-volcanic groups might also have been created in this way.
All evidences provide the possibility of proposing a probable origin of sub-volcanic outcrops with low melting temperature of metasomatism crust (enriched of silica and alkaline) affected by the solutions accompanying ocean crust beneath thrust in continuation of magma processes along with tectonic active regime. Swelling of rhyolite magma in extension of existing cracks in a tensile environment is similar to volcanic art backward from late Eocene to Oligocene. Although this proposed tectonic magma model requires geochemical and field evidences and isotopic data; this doesn't well reject the results of Emami et al (1992) studies in this area, indeed it is used to confirm the subduction regime model (Moein Vaziri, 2004) under the influence of a volcanic art at least in Ardestan area in Oligocene time later on.
References
Abdalla, H. M., Matsued, H., Obeid, M. A. and Takahashi, R. (2008) Chemistry of cassiterite in rare metal granitoids and the associated rocks in the Eastern Desert, Egypt. Journal of Mineralogical and Petrological Sciences,103, 318-326. Antipin, V. S., Andreeva, I. A., Kovalenko, V. I. and Kuznetsov, V. A: (2009) Geochemical specifics of ongonites in the Ary-Bulak Massif, Eastern Transbaikalia. Petrology,17, 558-569.
Brown, G. C., Thorpe, R. S. and W~bb, P. C. (1984) The geochemical characteristics of granitoids in contrasting arcs and comments on magma sources. Journal of Geological Society London,141, 413- 426.
Condie, K. C. (I 989) Geochemical changes in basalts and andesites across the Archean-Proterozoic boundary: Identification and significance. Lithos, 23, 1- 18.
Cox, K. G., Bell, J. D. and Pankhurst, R, J., I 979. The interpretation of igneous rocks. George Allen and Unwin 45. Darvishzadeh, A. (1984). Principles of Volcanology. Tehran University Press, Tehran. Radfar, J. (1997) Geological map of Ardestan 1: 1000000. Publications of Geological Survey and Mineral Exploration of Iran.
Emami, M. H. Khalatbari, M. Vosoughi Abedini, M. (1992). Organization of Geological Survey and Mineral Exploration of Iran) Tertiary Plutonium of Ardestan and Central Iran. Quarterly 4, 23-28.
Green, N. L. (2006) Influence of slab thermal structure on basalt source regions and melting conditions. Lithos, 87, 23-49. Harris, N. B. W., Pearce, J. A. and Tindle, A. G. (1986) Geochemical characteristics of collision-zone magmatism. In: Coward, M. P. and Ries, A. C. (Eds.). Collision Tectonics. Geological Society. London, Special publication, 19, 67-81.
Irvine, T. N. and Baragar, W.R.A. (1971) A guide to the chemical classification of the common volcanic rocks. Canadian Journal of Earth Sciences, 8, 523-548.
Kumral, M., Caban, H., Gedikoglu, A. and Kilinc, A. (2006) Petrology and geochemistry of augite trachytes and porphyritic trachytes from the Golcuk volcanic region. Journal of Asian Earth Sciences, 27, 707-716.
Le Maitre, R. W., Bateman, P., Dudek, A. Geller, J. (1989) A classification of igneous rocks and glossary of terms. Blackwell, Oxford. Maniar, P. D. and Piccoli P. M. (1989) Tectonic discrimination of granitoids, Geological Society of America Bulletin, 101, 635-643. Martin, H. (1993) The Archaean grey gneisses and the genesis of the continental crust. In: Condie, K. C.(Eds.): The Achaean Crustal.Evolution. Elsevier, Amsterdam.
Middlemost E.A.K. (1985). Magmas and Magmatic Rocks. Longman, London.
Miskovic, A. and Francis, D. (2006) Interaction between mantle - derived and crustal calc alkaline magmas in the Petrogenesis alkaline of the Sifton Range. Lithos, 87, 204-134.
Moin Vaziri, H. (1996) A Preface on Magmatism in Iran. Tarbiat Moallem University Press.
Moin Vaziri, H. (2004) Several Milestones in the History of Tectonomagmatic of Iran. Geological Survey and Mineral Exploration of Iran, Quarterly, 50-49, 32-39.
Nakamura, N. (1974) Determination of REE, Ba, Fe, Mg, Na and K in carbonaceous and ordinary chondrite. Geochimca et Cosmochimica Acta, 38, 757-775.
Nasr Isfahani, A. Ahmadi, M. (2008) Lithology of Shoshonitic lavas in the south of Eshin (east of Isfahan). Journal of Basic Sciences of Islamic Azad University, Science and Research Branch of Tehran, 69, 89-98.
Nasr Isfahani, A. Hajian, M (2007) Geology of Manganese Bagan Ore (Southern Ardestan) with an emphasis on petrological properties of felsic volcanic rocks. First International Congress on Applied Geology, Mashhad.
Parada, M. A., Nystrom, J. 0. and Levi, B. (1999) Multiple source for the Coastal Batholith of Central Chile: geochemical a Sr-Nd isotopic evidence and tectonic implication. Lithos, 46, 505-521.
Qorbani, M. (2003). The Principles of Volcanology with an Attitude toward Volcanoes in Iran. Aryan Zamin publication.
Raymond, L. A. (2002) The Study of igneous Sedimentary and Metamorphic Rocks. McGraw Hill.
Rollinson, H. R. (1993) Using Geochemical Data: Evaluation, Presentation, Interpretation. John Wiley and Sons.
Sajona, F. G., Maury, R. C., Bellon, H., Cotton, J. and Defant, M. (1996) High field strength elements of Pliocene-Pleistocene island-arc basalts Zamboanga Peninsula, Western Mindanao (Philippines). Journal of Petrology, 37, 693-726.
Scharidl, E. S. and Gorton, M. P. (2002) Application of high field strength elements to discriminate tectonic setting in VMS environments. Economic Geology, 97, 629-642.
Shahabpour, J. (2005) Tectonic evolution of the orogenic belt in the region located between Kerman and Neyriz. Journal of Asian Earth Sciences, 24, 405-417.
Shelly, D. (1993) Microscopic Study oflgneous and Metamorphic rocks, Chapman and Hall, London.
Sun, S. S. and McDonough, W. F. (1989) Chemical and isotopic systematic of qceanic basalts: implications for mantle composition and processes. In: Saunders, A. D. and Norry M. J. (Eds.): Magmatism in ocean basins. Geological Society of London. Special Publication,42, 313-345.
Tetsuichi, T., Yuji, 0., Kazuki, N.,Yasushi, W. (1999) Petrology of a mantle derived rhyolite, Hokkaido, Japan. Chemical Geology,160, 425-445.
Thompson, A. B.(1982) Magmatic of the British Tertiary volcanic province. Scottish Journal of Geology,18, 50-107.
Watter, S. W.A and Etminan, H. (1973) Manganese in Iran from contribution to the Geology of mineral Resources in Iran
Geological Survey of Iran.
Wilson, M. (1989) ligneous Petrogenesis: A Global Tectonic Approach. Chapman and Hall, London.
Zhu, X., Mo, X., White N.C. Zhang, B, Sun, M., Wang, S., Zhao, S. and Yang, Y. (2009) Geology and metallogenetic setting of the habo porohyry Cu (Mo-Au) deposit Yunnan. Acta Geologica Sinica, 83, 1915-1928.
Citation:
Mohammad Ali Arian, Alikhan Nasr Isfahani, Afsaneh Ranjbar (2017). Petrogenesis and Geochemical Properties of Dome-shaped Subvolcanic Complexes in Southwest of Shahrab (Northeast of Isfahan). Ukrainian Journal of Ecology, 7^4), 316-324. I This work is licensed under a Creative Commons Attribution 4.0. License
