Eocene volcanic occurrences are the most important volcanic demonstrations In Iran, because it has led to the creation of a volcanic arc which has a length of 1700 km and a width of 100 km [1] [2] . This volcanic arc which is known as the Urmia Dokhtar volcanic arc is widespread from northwest to southeast in Iran and is the most important volcanic zone of Iran [3] -[6] . Eocene volcanic occurrence in almost all regions, except Zagros and Kopet Dagh, took place [7] . One of the most complete volcanic sequences of the Urmia Dokhtar magmatic arc, with a thickness of over 3 km, is in the north and northeast Tafresh. Volcanic occurrences in this area have begun since Lutetian, so that these volcanic units are located on the Upper Cretaceous units [8] . The purpose of this article is to identify and determine the structural formulas of minerals in the Upper Eocene volcanic rocks of NE part of Tafresh (Figure 1).

In order to achieve the aims of this work, at the first field surveying and sampling was done, then thin and thin polished sections were prepared. About the rocks of area, 5 rocks include andesitic basalt, basaltic andesite and andesite were selected for microprobe analysis and their olivine, clinopyroxene and plagioclase minerals by using XGT-7200 micro-XRF analyzer-Horiba with voltage of 50 kv and a current of 3 mA in Kansaran Binaloud Laboratory were analyzed. A total of 80 points were analyzed which results of this analysis are given in Tables 1-3.

This area is located in Markazi Province with geographical coordinates to east longitude and to north latitude and is part of the magmatic zone of Urmia Dokhtar. Also, from structural and metallurgical viewpoint, it is located at the northwest corner of Central Iranian plate (Figure 2). The most ancient rock outcrops of the area are related to the Middle Triassic (Ladinian) time, which in Noghre Kamar defile are reached to the level by Tafresh fault [9] . Jurassic in north Tafresh only limited to Lower Jurassic and includes deposits made of shale and sandstone (Shemshak formation). In the Upper Cretaceous, because of orogenic event, sediments with a thickness of 1000 m and a basal conglomerate are located on old folded layers. Eocene in the studied area is very important, because in this period the volcanic activity starts and reaches its peak [10] . Eocene deposits included pyroclastic rocks, lava flows and some sedimentary rocks, which have a thickness of 3000 m. Based on sedimentary units between different phases of volcanism in the study area; Eocene series is classified into six distinct lithologic zones (Lithozone) [11] . This unit consists of basic and acidic lavas with a dominant andesite composition and

alternative pyroclastic rocks of the basaltic-andesitic composition. In the Upper Eocene, magmatic activity is significant and mostly consists of basaltic andesite lavas with porphyritic texture along with tuff cuts, Ignimbrite and tuffit. In Oligocene-Miocene, it contains limestone-marly formation (Qom Formation) [12] . Magmatism at this time is mostly of basic to moderate types and partially occurred.

The studied volcanic rocks are in the hybrid domain of andesitic basalt, basaltic andesite and andesite. The main minerals of their constituents include phenocrysts plagioclase, clinopyroxene, olivine and Alkali feldspar (Figure 3). The texture of these rocks is porphyritic with microlitic to aphyric matrix and in some cases contains micro-

litic glassy matrix or pitted microlitic dough. Pores often are filled by secondary minerals such as calcite, chlorite and quartz and based on the petrographic features; plagioclases are automorphic to semi-automorphic crystals with eroded margins. In some cases in feldspars, carlsbad and albite and sometimes polysynthetic twining and zoning can be seen. Also in some cases plagioclases sometimes can be seen as megaporphyry crystals in the rocks. In some plagioclase, their margins are destroyed, while center of crystals are relatively intact (Figure 3). The pyroxene crystals are automorphic to heteromorphic phenocrysts as well as tiny crystals in the groundmass of rock. Microscopic features of these crystals indicate that their compositions are diopsiditic. We can see olivine phenocrysts in the andesitic basalt rocks (Figure 3). These phenocrysts are automorphic to heteromorphic shapes and are mostly seen as casts of olivine which are disintegrated to chlorite, serpentine and Iddingsite.

The Upper Eocene volcanic rocks in Tafresh include andesitic basalt, basaltic andesite and andesite which have constituted significant volumes of lava in the region. Plagioclase feldspar, pyroxene and olivine are the major minerals in them. Plagioclase (60% - 70%) is as phenocryst and microlite. Plagioclase phenocrysts are mostly of calcic to sodic types and their anorthite component (X_an) vary between 0.05 to 0.98 (anorthite to oligoclase), (Figure 4). Petrographic studies of plagioclases also confirm that anorthite component of the andesitic basalt rocks is much more than that of other basaltic rocks. The potassium component (X_or) of plagioclase phenocrysts vary between 0.01 to 0.90 (albite to sanidine). Pyroxene phenocrysts are clinopyroxene and orthopyroxene. Pyroxene as orthopyroxene is the dominant phase in andesitic basalts. According to the classification of Deer, Howie and Zussman [13] the pyroxenes of andesitic basalts have hypersthene and pigeonite composition. However, calcic pyroxene (augite) is also seen. The basaltic andesite rocks contain iron pyroxene with a compositional range from En₃Fs₅₁Wo₁₀ to En₁₃Fs₇₈Wo₃₈ (Figure 5). The andesitic rocks are characterized by Ca-rich pyroxenes with hedenbergite composition which show compositional range from En₂Fs₄₃Wo₃₈ to En₁₂Fs₅₁Wo₄₆ (Figure 5). According to the classification of Morimoto [14] , pyroxenes often are located in the ranges of A and D. Two possible processes can explain the existence of iron-reach portion (hedenbergite-ferrosilite) in basaltic andesite and andesite rocks, (1) opacitization and oxidation of the pyroxenes with removal of calcium and magnesium as carbonate from minerals, and (2) remove of calcium as well as fixing magnesium in some clinopyroxenes. According to Figure 6 olivine ranges in composition from Fo₁₉ to Fo₂₄ show ferrohortonolite composition.

Empirical and experimental studies indicate that mineral compositions can be effectively used to quantify the P-T conditions during crystallization [15] -[17] . So the researches proposed several ways such as Pyroxene-oli- vin, Amphibole-clinopyroxene and pyroxene-feldspare thermometer and pyroxene baromether for this meaning. To determine the temperature of clinopyroxene formation in the andesitic basalt, basaltic andesite and andesite rocks, clinopyroxene barometry has been used. According to Lindsley [18] graphical thermometer, andesitic basalts have been formed at 1100˚C (Figure 7). The basaltic andesite rocks are formed in the higher temperature ranges from 700˚C to 1000˚C. However the andesitic basalt rocks have the highest formation temperature of 1100˚C. Furthermore, also according to the Aoki and Shiba [19] and Helz [20] approaches, the pyroxenes of the study area are in a wide range of low pressure to medium pressure (Figure 8). This indicates their crystallization while are stopping during the magma ascent. The compositions of Al in clinopyroxene have been used to determine the depth of the magma chamber. According to these diagrams, the clinopyroxenes in intermediate to basic rocks have been crystalized at intermediate pressure (<5 kbar).

Oxygen fugacity plays an important role in changing of the liquidus temperature, melt and crystals composition, magmatic processes controlling, crystallization sequence and types of crystallized minerals [21] -[24] . Using Al^IV + Na vs Al^IV + 2Ti + Cr diagram which depend on the amount of 3-valent iron in pyroxenes, we can get oxygen fugacity. The diagram is set based on the aluminum balance in the tetrahedral position with Cr³⁺ in the octahedral position. The Fe³⁺ in pyroxenes can be displaced 3-valence elements such as Al^VI, Ti and Cr in the octahedral position. In the other hand Fe³⁺ in pyroxenes depends on the amount of Al^VI which means it depends on the aluminum balance in tetrahedral and octahedral position. Figure 9 show that the pyroxenes which crystalized at high oxygen fugacity, has been situated above the line of Fe³⁺. Furthermore, Papike and Cameron [25] have mentioned to the distances of the samples from the Fe³⁺ line and noted that further distances of the samples from this line are indicating more oxygen frugalities in their geological setting. In this diagram some samples are located above the line of Fe³⁺ line and some are below that (Figure 9).

Pyroxene composition depends on the chemical composition and tectonic setting of the host lava which can be used widely to determine geological setting of the rocks [27] [28] . Ti + Cr vs Ca and TiO₂ vs Na₂O + CaO diagrams define the pyroxenes which generated by tholeiitic and calc-alkaline magmas from those of alkaline. Plotting data on Ti + Cr vs Ca and TiO₂ vs Na₂O + CaO diagrams shows that the samples are subalkaline to alkaline tendency. Diagrams (Figure 10) indicate the extensional setting of the area when the rocks were formed.

The andesitic basalts have the most calcic plagioclase in comparison with the other rocks and contain two coexisting clinopyroxene and orthopyroxene. Andesite rocks are defined by the most calsic pyroxenes in comparison with other rocks in the study area. Clinopyroxene thermobarometry diagrams suggest that basaltic andesites have been crystalized at <5 kbar pressure and a temperature between 750˚C - 1000˚C. The andesitic basalts and andesites have been crystalized at higher 1100˚C and lower (<750˚C) temperature respectively. According to the distribution of aluminum in clinopyroxenes, these minerals have been formed at <5 kbar pressure and water content between 5 to 10 percent. The mineral compositions of the rocks display an alkaline nature which indicates a tensional setting.

The authors appreciate the support received from the Islamic Azad University, Sciences and Researches Branch.