Mineral Chemistry and Magmatic Differentiation Evidences in the Neshveh Intrusion ( NW Saveh , Central Iran )

Neshveh intrusion which is located in the NW of Saveh City is a part of Sahand-Bazman magmatic arc within the Central Iranian zone. This intrusion consists of quartz-monzogabbro, quartz-monzodiorite, granodiorite and granite that have intruded into the Eocene volcano-sedimentary rocks. This intrusion is medium to high-K calc alkaline, metaluminous, and I-type granitoid. All phases of the Neshveh granitoid are characterized by LREE-rich patterns with high LREE/HREE ratio and negative Eu anomalies. Similarity of patterns suggests a comagmatic source for these rocks and demonstrates the role of magmatic differentiation in their evolution. Clinopyroxene classified as calcic type with varying from clinoenstatite-clinofferosillite to diopside and augite from quartzmonzogabbros to quartz-monzodiorite and granodiorite. Plagioclase composition varies from bytownite and labradorite in quartz-monzogabbros to andesine in quartz-monzodiorites and oligoclase in granodiorites and granites. Core of some plagioclases in granodiorites and granites shows the calcic composition which is labradorite and andesine in granodiorite and andesine in granites. Field investigations along with petrographic and geochemical studies indicate that all phases of the Neshveh intrusion derived from a common magma source as a result of mineral differentiation. Geochemical evidences show smooth differentiation trends in which most of major elements (except Al2O3, K2O and Na2O) are negatively correlated with SiO2 and K2O, Ba, Rb, Ce, Nb, and Zr are positively correlated with SiO2. Some elements such as Na2O, Sr, Eu and Y follow curves that reflect crystal fractionation of clinopyroxene, plagioc1ase and hornblende. Furthermore, large volumes of quartz-monzogabbros compared to granites, as well as the lack of mafic enclaves in more evolved rocks, are also indicative of crystal fractionation. Clinopyroxene fractionation was the main control in the evolution of the magmas up to 55 wt% SiO2. Hornblende took over from 55 wt% Corresponding author. R. Keshavarzi et al. 263 SiO2, resulting in decreasing Dy/Yb with increasing silica content in the most siliceous rocks. Fractionation of opaque minerals and apatite throughout the sequence, and the continuous increase in K2O and Ba vs. SiO2 reflect the absence of significant fractionation of biotite and K-feldspar.


Introduction
Neshveh intrusion located at about 25 km in the northwest of Saveh city and is a small part of the Sahand-Bazman magmatic arc in the Alpine-Himalayan orogenic belt.The arc outcrops mainly consist of Eocene-Miocene volcano-sedimentary sequences and associated plutonic rocks typical of calc-alkaline magmatism developed at active continental margins.The arc developed during the closure of the Neotethyan Ocean between Arabia and Eurasia (e.g.[1] [2] [3]), and has been the subject of geophysical, kinematic, and neotectonic studies [4]- [9].However, little is known about the magmatic activity of the Sahand-Bazman magmatic belt, which was active from Tertiary to Pliocene-Quaternary times (Figure 1) [4] [10] [11].Volcanic rocks are so common in this magmatic belt.These rocks have varieties in composition and tectonic setting which is vary from acidic to basic and con-tinental to shallow marine environments.Acidic-intermediate volcanic and intrusive rocks are widespread in contrast to basic rocks.Intrusive rocks in this magmatic belt show a large range of rock types, dominated by granite and granodiorite but with small amounts of quartz diorite, diorite and gabbro.The Neshveh intrusion was intruded into the volcanic-sedimentary rocks of Eocene (Figure 2) and constitute of quartz monzogabbro, quartz monzodiorite, granodiorite and granite (Figure 3).
Several studies have been carried out in the Saveh region, such as studies of [12] and [13] which were focused on the petrography and Petrochemistry of igneous rocks in the south west of Saveh, volcanic and plutonic rocks in the south of studied area.Previous petrological studies have concentrated mainly on the petrology and tectonic setting of the intermediate-acidic volcanic-plutonic rocks [12]- [15].In this paper, we combine field and petrography studies with EMPA analysis of the main constitute minerals and whole-rock geochemical data to test whether these various rocks were generated by crystal fractionation or by mixing between basaltic and felsic magmas.

Research Methods
Our researches in this study consist of two parts: field and laboratory studies.Field studies include identifying the different phases of intrusion, relationship between them and host rock and finally sampling of different phases for laboratory studies.Laboratory investigations include preparing of 90 thin section and petrographic studies.After detailed optical inspection, 8 fresh samples selected for electron microprobe analysis.The major oxide compositions of the minerals (e.g.plagioclase, alkali feldspar, clinopyroxene, amphibole and biotite) in 92 point were determined at mineralogy division of the Iranian Mineral Processing Research Center (IMPRC) using Cameca SX-100 electron microprobe equipped with 5 wavelength-dispersive crystal spectrometers, operating at a 3 μm beam diameter, 15 kv accelerating voltage, 15 nA sample current and 60 s counting time.
Fifteen fresh whole-rock samples representative of the petrological range in the Neshveh intrusion were analyzed for major and trace elements and REEs by ICP and ICP-MS method at ALS Chemex laboratory in Canada.Detection limits range 0.01 -0.1 wt% for major oxides, 0.1 -10 ppm for trace elements, and 0.01 -0.5 ppm for the rare earth elements.

Regional Geology
Neshveh region which is located in the northwest of Saveh is a small part of the Sahand-Bazman magmatic belt within the Central Iranian zone.All rocks crops out in this region have Cenozoic age and older rocks don't exposed.Based on Saveh geological map 1:100,000 [17] the main rocks in this area consists of sedimentary, volcanic and intrusive rocks have Paleocene-Eocene age and later (Figure 2).These rocks composed of conglo- Several granitoid intrusions were intruded into the Eocene volcanic-sedimentary rocks.Dating of some of these intrusions by [12] using K-Ar method on the amphibole, biotite, K-feldspar and whole rock indicate 28 -42 Ma (Table 1).The Selijerd granodiorite, Khalkhab tonalite-diorite, Neshveh intrusion (this study) and Neivesht micro-granite are the most important intrusions in the northwest of Saveh.Neshveh intrusion composed of quartz monzogabbro, quartz monzodiorite, granodiorite and granite.In addition to mentioned intrusives, some subvolcanic domes also exist in different parts of the northwest Saveh that have acidic-intermediate composi-   tion.These domes intruded into the Upper Eocene-Oligocene intrusives.In this base, these sub-volcanic intrusions attributed to the Post Oligocene.
There are some acidic and basic dykes in this area.Basic dykes with a desite-andesitic basalt composition are widespread in comparison to acidic dike with daciteandesite composition.These dikes cut the Eocene volcanic rocks and Oligocene intrusives.In this base, their intrusions have been attributed to the post Oligocene.
The country rocks of the Neshveh intrusion are dominated by andesitic lava and rhyodacitic tuff, andesitic-basaltic lava and andesitic-basaltic breccia associated with limestones [17] (Figure 3).The rhyodacitic tuff is dominantly composed of volcanic grains which, due to explosive acidic eruptions, were ejected as glass shards (now devitrified) and other fragments into a marine environment, forming green minerals such as chlorite and epidote, with various clay minerals [18].The andesitic-basaltic lavas are dark green and brown in color, with medium-grained phenocrysts, and have minor beds of andesitic tuff.Plagioclase occurs as phenocrysts that range in size from less than 0.2 mm to several mm.In addition to the ubiquitous laths of plagioclase, the basaltic lavas contain olivine and clinopyroxene, in places altered to iddingsite, and actinolite and chlorite, respectively.The lavas occur as clumps a few mm to cm in size within a highly hydrated, oxidized, and altered volcanic matrix, suggesting eruption in a shallow marine environment.In many cases, the exterior margin of these blobs consists of volcanic glass or oxidized material, while the interior parts are more intact, and have preserved an original volcanic texture and structure [18].The andesitic-basaltic breccia composed of a sequence of hyaloclastic breccia and tuff at the base grade upwards into aphyric lava followed by autoclastic breccia at the top.The tuff grains vary in size from a few mm to a fewcm, and the smaller grains are replaced by green minerals such as chlorite and epidote, probably because of reaction with water, whereas the larger grains are less altered.Hand specimens show altered phenocrysts of clinopyroxene and plagioclase.Moreover, the olivine basaltic lava at the middle of the sequence and the hyaloclastic breccia at the top might indicate explosive volcanic/volcaniclastic activity under water, probably in a marine basin [18].
The chemical compositions of the volcanic rocks show a calc-alkaline affinity, enrichment in LILEs (Rb, Ba, Th, U, and Pb) and depletion in Nb, Ti, and Zr [18].Significant U enrichment relative to Nb and Th is mainly a result of source enrichment by slab-derived fluids.The results of geochemical modelling suggest a mantle lithosphere source for these volcanic rocks [18].
Two plutonic bodies, Khalkhab-Neshveh and Selijerd intrusions, were intruded into the volcano-sedimentary rocks (Figure 2 and Figure 3).The former comprises quartz monzogabbro, quartz monzodiorite, granodiorite and granite, while the Selijerd pluton in the southern map area consists of tonalite and granodiorite.

Petrography
The Neshveh intrusion covers an area of about 22 km 2 and consists of a wide spectrum of rock types, which form high elevation terrains.It was subdivided into two compositional zones: quartz monzogabbro in the West and quartz monzodiorite, granodiorite and granite in the East (Figure 3 and Table 1) based on mineralogy and using the terminology of [19].The contacts are gradational but the rock types are distinct and easily recognized both in outcrop and in aerial photos and satellite images.
Clinopyroxene is a primary mafic phase in the rock and amphibole is absent as a primary phase.In a few samples, especially in the porphyritic quartz monzogabbros, clinopyroxene is replaced completely by actinolite.Plagioclase forms mainly euhedral and lath-shaped crystals.Large plagioclase crystals (>3 mm) often contain many inclusions of clinopyroxene and opaque minerals (Figure 4(A)).They mainly show zoning, twinning and prismatic-cellular growth.Some large crystals of plagioclase are altered to sericite and clay minerals.Quartz and K-feldspar are anhedral and occupy the interstices between plagioclase tablets, suggesting late crystallization.

Granite
The white granites are restricted to the centre of intrusion (Figure 3).They are generally medium-grained and have granular to porphyritic textures with megacrysts of plagioclase.They contain plagioclase (32 -35 al %), K-feldspar (28% -29.7%) and quartz (30% -33%) with mafic minerals of green hornblende (2.3% -4%) and biotite (1.2% -2.2%) (Figure 4(D)).There are two kinds of plagioclase in the granitic rocks including medium-grained and large phenocrysts (~2 mm).Some of K-feldspars are altered, particularly to clay minerals, and occasionally show intergrowth with quartz.Otherwise, quartz is medium-grained and shows undulose extinction.Green hornblende is partially replaced by chlorite and opaque minerals.Magnetite and hematite are the main opaque minerals.

Mineral Chemistry
As mentioned before, for determining of mineral composition of the Neshveh intrusion, 8 samples from the different parts of this intrusion (quartz monzogabbro, quartz monzodiorite, granodiorite and granite) were selected and 92 points were analyzed by EPMA.Analyzed minerals include plagioclase, alkali feldspar, biotite, amphibole and clinopyroxene.The results of analysis demonstrated in Table 2.Chemical formulae and mineral name for clinopyroxene were done following the method of [21].In this method, it must be distinguished different kind of clinopyroxenes include sodic, sodiccalcic and calcic, at first step by using Q-J diagram.Then, Wo-En-Fs triangular diagram must be used for determining calcic clinopyroxenes and Q-Jd-Ae triangular diagram for classifying sodic and sodiccalcic clinopyroxenes.
For amphiboles, Chemical formulae and mineral name distinguished by using the [22] method.In this method, based on occupancy of B location in the mineral structure by Ca and Na, 4 main groups of amphiboles (rich in Fe-Mg-Mn, calcic, sodic-calcic and sodic groups) were recognized.Then, exact name and composition of amphibole identified by using Mg/ (Mg + Fe 2 ) vs. Si binary diagrams.
Chemical composition and classifying of biotite were done by using Fe/(Fe + Mg) vs. Al IV binary diagram.Finally, feldspars (include plagioclases and alkali feldspars) classified by using the Or-Ab-An triangular diagram.
As mentioned in the petrography section, clinopyroxenes present in the all phases of Neshveh intrusion, but it is predominant at the quartz monzogabbros.All of the analyzed clinopyroxenes classified as calcic clinopyroxenes (Figure 6(A)).Most of the clinopyroxenes in the quartz monzogabbros are clinoenstatite-clinofferosillite but some minerals have diopside and augite composition (Figure 6(B)).Clinopyroxenes within the quartz monzodiorites and granites have diopside and augite-diopside composition (Figure 6

(B)).
As mentioned in the petrography section, clinopyroxenes present in the all phases of Neshveh intrusion, but it is predominant at the quartz monzogabbros.All of the analyzed clinopyroxene classified as calcic clinopyroxenes (Figure 6(A)).Most of the clinopyroxenes in the quartz monzogabbros are clinoenstatite-clinofferosillite but some minerals have diopside and augite composition (Figure 6(B)).Clinopyroxenes within the quartz monzodiorites and granites have diopside and augite-diopside composition (Figure 6(B)).
All of the analyzed amphiboles from the different parts of the Neshveh intrusion are classified as calcic amphiboles (Figure 7(A)).Based on Mg/(Mg + Fe 2 ) vs. Si binary diagrams, amphiboles of the quartz monzogabbros have actinolitic hornblende composition, analyzed amphiboles from the quartz monzodiorites are hornblende, Fe-hornblende, Mg-hornblende and actinolite, amphiboles from the granodiorites are Mg-hornblende and finally, amphiboles of the granites have actinolitic composition (Figure 7(B)).Most of them are edenite in composition (Figure 7

(C)).
Based on Fe/(Fe + Mg) vs. Al IV binary diagram, analyzed biotites from the quartz monzogabbros and quartz monzodiorites have intermediate composition between the phlogopite and annite (Figure 8(A)).
Plagioclase is the most common mineral that occur in all phases of the Neshveh intrusion.Its composition varies within the quartz monzogabbros, quartz monzodiorites, granodiorites and granites.As mentioned before, within the granitic and granodioritic parts of the Neshveh intrusion, there are some plagioclases that their compositions vary at the core and rims (Figure 5(B)).This subject is supported by EPMA analysis, also.Analyzed   plagioclases from the quartz monzogabbros indicate that most of them are labradorite and some bytownite (Figure 8(B)).The rims of some crystals are andesine in composition (Figure 8(B)).Plagioclases from the quartz monzodiorite are mainly andesine and occasionally labradorite (Figure 8(B)).Some of them indicate oligoclase composition and in one point, the core of plagioclase has bytownite composition (Figure 8(B)).Plagioclases of the granodiorites have oligoclase compositionbut core of some crystals show different and calcic composition which is labradorite and andesine (Figure 8(B)).Plagioclases in the granites also have oligoclase composition but some crystals have calcic core that its composition is andesine (Figure 8(B)).
All analyzed alkali feldspars locate near the Or corner on the Or-Ab-An triangular diagram (Figure 8(C)).

Geochemistry
As mentioned before, 15 fresh whole-rock samples representative of the petrological range in the Neshveh intrusion were analyzed for major and trace elements and REEs by ICP and ICP-MS method at ALS Chemex laboratory in Canada (Table 3).
The calc-alkaline nature of the all rock types of the Neshveh intrusion is illustrated on the SiO 2 vs. K 2 O diagram [23], which are the samples all plot within the medium to high-K calcalkaline field (Figure 9).The molecular ratio of Al 2 O 3 /(CaO + Na 2 O + K 2 O) ranges from 0.73 to 1, exhibiting metaluminous characteristics [15].Features such as Na 2 O > K 2 O, A/CNK < 1, decreasing P 2 O 5 versus SiO 2 [24] and SiO 2 vs. K 2 O [25] and ACNK versus SiO 2 diagrams [26] are characteristic of I-type rocks, which is also consistent with the presence of key modal minerals such as hornblende and titaniteand absence of muscovite, garnet, cordierite, andalusite and sillimanite.The rocks are sodic as shown by the high average values of Na 2 O/K 2 O (1.53) and Na 2 O + K 2 O (5.33) (Table 3).
The Neshveh intrusion rocks have a wide range in SiO 2 (52.1% -71.2%),Fe 2 O 3 , MgO, MnO, CaO, TiO 2 and P 2 O 5 (Table 3).Most major elements except Al 2 O 3 , Na 2 O and K 2 O show negative linear trends with increasing SiO 2 (Figure 10).K 2 O shows a descending trend, while Al 2 O 3 and Na 2 O have bent trends.Na 2 O is positive up to 62 wt% SiO 2 and negative from this point onward.
In the Harker diagrams (Figure 11), Ba, Rb, Zr, Nb, and Ce show ascending linear trends, whereas V and Co decrease with increasing silica content.Sr, Eu and Y follow curved trends that suggest these elements behaved incompatibly in the magmas that formed the quartz monzogabbro and quartz monzodiorite, and compatibly during the crystallization of granodiorite and granite.
The samples display similar chondrite-normalized REE patterns.They are characterized by LREE enrichment with (La/Sm) N = 2.11 -4.27 and weakly fractionated HREE with (Gd/Yb) N = 1.16 -1.46, suggesting garnet-free sources [27].The mafic to intermediate rocks have slight but very consistent negative Eu anomalies (Eu/Eu * = 0.91 -0.82), decreasing more markedly in the granodiorites to a minimum of 0.42 in the granite with 71 wt% SiO 2 (Figure 12(A)).The primitive mantle normalized spider diagrams for different phases of Neshveh intrusion demonstrate negative anomalies of HFSEs including Nb, Ti and P, along with positive anomalies in LILEs including Rb, Ba, Th, K and Pb (Figure 12(B)).
These geochemical characteristics, with light-REE enrichment, positive Pb anomaly and the Nb-Ti troughs on the spider diagram are typical of calc alkaline magmatism in active continental margins [29].A marked Nb-Ta trough in primitive-mantle normalized trace element patterns has been ascribed to retention of these elements in mineral phases containing Ti (e.g., rutile, ilmenite, rutile, garnet and some amphiboles) during dehydration of subducted oceanic crust or crustal contamination [30].With increasing pressure, the solubility of titanium bearing minerals reduces in aqueous fluids [31].Therefore, theses minerals that are rich in HFSEs will be stable during partial melting process at depths greater than 30 km that is led to negative anomalies in the melt [31].The negative anomaly in phosphorus indicative for low content of apatite is in the studied rocks.As mentioned before, in the I-type granitoids, phosphorus acts as a consistent element and fractionation this element in the early stages of magma crystallization, led to negative anomalies in the crystalized rocks.
Fluids and melts derived from the subducted oceanic slab, led to the metasomatism of upper mantle wedge and thereupon, negative anomalies of Nb and Ta [27] [32] [33].Positive anomalies in Pb, K, Rb and Ba are attributed to metasomatism of mantle wedge by fluids derived from the subducted slab or/ and contamination with continental crust [34] [35].
The Chondrite-normalized REE patterns in the different phases of the Neshveh intrusion indicate negative Eu anomalies (Figure 12(A)).Negative anomalies in Eu are related to the feldspar fractionation during magma crystallization or remaining of feldspar at the source.If these negative anomalies are associated with negative  anomalies in Sr, fractional crystallization of plagioclase is responsible for these anomalies.While, the negative anomalies in Eu are associated with negative anomalies in Ba, K-feldspar fractionation has the main role in this respect [27].In the studied rocks, negative anomalies of Eu occur along with Sr, which refers to the plagioclase fractionation.
In terms of geodynamic setting, this intrusion classified as volcanic arc granites (VAG) and active continental margin granites (CAG) [15] [36].Geochemical studies indicate that the Neshveh intrusion was formed in a volcanic arc and active continental margin.In this base, it is assumed that this intrusion was formed as a result of Neotethys oceanic lithosphere subduction beneath the Central Iran zone in which replaced in the Sahand-Bazman magmatic arc.

Crystal Fractionation Evidences
Volcanic arc igneous rocks in orogenic belts mostly range in composition from gabbro-diorite to granite [37]- [41].This wide variation is variously ascribed to crystal fractionation, multi-pulse intrusion when the new pulse has different composition compare to the previous magma, magma mixing, variable degrees of restite separation, and contamination by assimilation [42] [43].those elements such as V, Cr,Ni, Zn and Sr fall, (e) some trace elements may rise or fall depending on whether or not the melt is saturated in the dominant mineral containing that element, e.g.Zr and Ba, (f) in some cases mineral saturation in felsic melts depends on whether the melt is I-or S-type, the most important example being apatite saturation which is a feature of felsic I-type melts (P falls) but not of more strongly peraluminous S-type melts (P rises).[28] and [29].

Petrographical and Geochemical Variations
Many researchers have shown that mineralogical and geochemical variations in magmatic suites from volcanic arcs can be produced by either magma mixing (e.g.[46] [47]) or assimilation-fractional crystallization processes [48]- [51].The fractionation process can be further tested by the field, petrographic and geochemical data.
Clinopyroxene is dominant mafic mineral in the quartz monzogabbro, but it is subordinate in the quartz monzodiorite and totally scarce or disappears in the granodiorite and granite.Green hornblende occurs in most samples from the quartz monzodiorite to felsic rocks, sometimes partly replaced by actinolite and biotite.Thus with increasing content of biotite and quartz, clinopyroxene may disappear or give way to hornblende and biotite.Apatite is not ubiquitous but appears as euhedral crystals of variable size; its modal abundance is less than 0.7% in the quartz monzodiorite and decreases with increasing silica.K-feldspar and quartz occur throughout; they are interstitial in the quartz monzogabbro and their grain-size and abundances increase from these rocks to the granites.Given the wide range of compositions, the lack of disequilibrium minerals, these progressive changes are interpreted as due to crystal fractionation rather than mixing between a mantle-derived basaltic magma and a crustal granitic magma; to this we may add the gradational internal contacts and the lack of mafic enclaves in the more evolved rocks.
Magma mixing and/or mingling and assimilation has frequently been observed in calc alkaline magmatic arc complexes (e.g.[52]) but cannot be invoked to account for the large scale compositional variations seen in the Neshveh intrusion.Although magma mixing can result in linear variations in Harker diagrams, it cannot explain the inflected trends shown by Na 2 O, Al 2 O 3 , Sr, Eu and Y (Figure 10 and Figure 11).Finally, minor and trace element abundances plotted in multi-element and rare earth element diagrams (Figure 12) show similar and smoothprogression from one rock type to the next within the intrusion, which is interpreted as resulting from crystal fractionation of the quartz monzogabbros.
A method exhibited by [53] to recognition of the three main processes of partial melting, fractional crystallization and magma mixing in the magmas.In this method, an incompatible element is used against a consistent element.Crystal fractionation is more effective at fractionating compatible elements and discrimination between these two mechanisms may be based on the behavior of trace elements in a logarithmic plot of an incompatible element against a compatible element, where they have very different bulk partition coefficients.In such a diagram, liquids produced by crystal fractionation give a straight line with strong decrease in the compatible element whereas the concentration of the incompatible element (D << 1) increases slowly; the opposite relationships apply to liquids produced by partial melting [53].Figure 10 shows that V content decreases with increa-singSiO 2 , thus demonstrating its compatible behavior, whereas positive correlations point to the incompatible behavior of Rb and Ba (Figure 10).In the log-log plots of V (compatible element) vs. Rb and Ba (incompatible element) (Figure 13), the trends shown are sub-vertical with drastic reduction of the concentration of compatible element (V) throughout the quartz monzogabbro to granodiorite sequence, and the incompatible element contents only increasing rapidly in the granites.This suggests that the main mechanism of differentiation is crystal fractionation.
Although the Neshveh intrusion has various petrographic and mineralogical characteristics, they show similar REE patterns, especially in the HREE (Figure 12).The widely varying concentrations of Nb, Ta and Th (4.3 -  3) and fractional fusion with continual removing of the melt formed (4).The initial material is (i) [53]; (B) and (C) Plots for the Neshveh intrusion samples showing near-vertical trends that suggest the main mechanism of differentiation is crystal fractionation.9.9 ppm, 0.3 -0.8 ppm, 2.7 -21.1 ppm, respectively) and gradual changes in Eu-anomaly are also key features.The hypothesis that provides the most satisfactory explanation of thesefeatures is a crystal fractionation model, in which all the rocks were derived from a parental magma via the fractionation.The granitic rocks of the intrusion are the most fractionated rocks, enriched in large-ion lithophile elements (Rb, Tb, U, and K) and depleted in Sr, P and Ti compared to the others.

Mineral Controls
A general crystal fractionation trend within the representative samples is indicated by decreasing TiO 2 , MgO, Fe 2 O 3 , CaO and P 2 O 5 concentrations, and increasing K 2 O together with most of the trace elements, e.g., Ba, Rb, La and Ce (Figure 10 and Figure 11).Some elements such as Na 2 O, Al 2 O 3 , Sr and Y define broken or curved trends (Figure 10 and Figure 11), a characteristic that allows us to discount their derivation by mixing and/or mingling mechanisms, and instead indicates that they result from crystal fractionation.In order to determine the magmatic evolution of the Neshveh intrusion, the modal mineralogical and chemical compositions are used to model the role of minerals leading to chemical variations in the evolving magma.
The average mode of clinopyroxene is 23% in the quartz monzogabbro, falling to zero in the granites (Table 1).At the same time, CaO decreases (Figure 10), suggesting removal of Ca-rich phases.Three Ca bearing minerals in the Neshveh intrusion rocks are plagioclase, clinopyroxene and hornblende.Sr is a compatible trace element in plagioclase but not in clinopyroxene, so that fractionation of plagioclase causes decreasing Sr with increasingsilica content [27].In the Sr vs. MgO plot (Figure 14(A)), Sr increases with increasing MgO up to 3.1 wt% (corresponding to 55 wt.% SiO 2 ) and then decreases.Since there is no hornblende in the rocks with Si02 less than 55 wt% (Table 1), it seems thatclinopyroxene had the main role in decreasing concentrations of, e.g., MgO, Fe 2 O 3 , CaO in the rocks with MgO> 3.1 wt.%.In the rocks with MgO < 3.1 wt%, magmatic evolution could have been controlled by fractionation of clinopyroxene, plagioclase and hornblende.In the log-log diagram of Rb vs. Sr (Figure 14(B)) [54], it appears that Sr concentration increases from about 350 to 590 ppm as Rb increases to about 40 ppm in the quartz monzodiorite, and then decreases to 150 ppm in the Rb-rich granite.This can be explained by crystallization of clinopyroxene in the early stages followed by crystallization of the plagioclase, clinopyroxene and hornblende together in the later stage.
Hornblende appears in the Neshveh intrusion phases with SiO 2 > 55 wt% (Table 1).Its mode increases from about 7% to 16.3% in the quartz monzodiorite, and then decreases to ~2.3% in the granite.Y and Yb are commonly incompatible elements when garnet and hornblende are absent [55] [56].A significant decrease in Dy/Yb ratio with increasing silica is attributable to removal of hornblende and titanite [57].In the Neshveh intrusion, Y concentration and Dy/Yb ratio remain fairly constant up to 62 wt% SiO 2 and then decrease which is indicating the onset of hornblende and/or titanite fractionation (Figure 11 and Figure 15(A)).The data in Figure 15(B) display a combined vector of hornblende and plagioclase fractionation, suggesting that both played a significant role during magmaticdifferentiation.Considering the modal mineralogical compositions and geochemical re-  The role of plagioclase is best examined through Na 2 O, Sr and Eu trends in the representative samples.Na 2 O shows an inflected trend with increasing silica content, increasing up to 55 wt% SiO 2 and then decreasing (Figure 10).Sr and Eu substitute for Ca and Na in plagioclase (but not in clinopyroxene); they have inflected trends in these samples that mimic that of Na 2 O.These trends can be interpreted as indicating that plagioclase fractionation was more important in the formation of rocks with SiO 2 > 55 wt% compared to the rocks with SiO 2 < 55 wt% (petrographic observations show that there is no significant change in the proportion of plagioclase up to this point, Table 1).This is also the only reasonable explanation for the development of negative Eu anomalies in the granites.Thus, plagioclase would have had no effect on CaO, Na 2 O and Al 2 O 3 in the less siliceous rocks.
Ba/Sr ratio will help to identify the relative roles of K-feldspar and plagioclase, since it increases with precipitation of plagioclase from the magma, but decreases when K-feldspar and biotite start to precipitate [58].In the Neshveh intrusion rocks, Ba/Sr is constant up to 55 wt% SiO 2 and then increases, showing the effect of plagioclase precipitation (Figure 16).Ba concentration increases with increasing SiO 2 without any inflection (Figure 11), suggesting that K-feldspar and biotite are late-crystallized minerals and/or sank very slowly in the co-existing melt during magmatic evolution [59].Essentially, constant K/Rb ratios (Figure 14(B)) and the positive correlation between K 2 O and SiO 2 (Figure 11) are also consistent with no K-feldspar removal.In addition, Fractionation of biotite and K-feldspar should buffer or reduce Ba in the residual liquid [60].K 2 O and Ba contents increase from 1.21 wt% and 247 ppm, respectively, in quartz monzogabbro to 5.14 wt% and 808 ppm in granite (Figure 10 and Figure 11; Table 2), indicating that biotite and K-feldspar crystallized late or sank very slowly in co-existing melt during magmatic differentiation.As presented in Table 1, biotite content decreases in the granitic samples, thus increasing of Ba in these samples is mostly related to late-crystallize Kfeldspar in the magma.
The regular decrease in P 2 O 5 content from the quartz monzogabbroic to granitic rocks (Figure 10) is attributed to fractionation of apatite [9].
Ti-bearing minerals such as ilmenite and titanite might be other fractionated phases in the Neshveh intrusion, as indicated by the decrease of TiO 2 with increasing SiO 2 (Figure 10).Moreover, as hornblende and biotite fractionated from the magma forming rocks with SiO 2 >~ 62 wt%, a combination of ilmenite, titanite, hornblende and biotite fractionations can be considered responsible for the decreasing TiO 2 in granodioritic and granitic melts.There is a larger negative Ti anomaly in the granitic rocks and decreasing Dy/Yb ratio vs. SiO 2 in the representative samples (Figure 12(B) and Figure 15(A)).

Conclusion
Field studies along with petrographic and geochemical investigations indicate that the Neshveh intrusion composed from the quartz monzogabbro, quartz monzodiorite, granodiorite and granite.The wide compositional and mineralogical range of the Neshveh intrusion, from quartz monzogabbro through to granite, is typical of a calc alkaline arc intrusion.This intrusion has high-K calc-alkaline nature classified as I-type granitoids.All phases of the Neshveh granitoid are characterized by LREE-rich patterns with high LREE/HREE ratio and negative Eu anomalies.Similarity of patterns suggests a comagmatic source for these rocks and demonstrates the role of magmatic differentiation in their evolution.Field relations, together with mineral composition and geochemical studies demonstrate that all rock types are co-magmatic and related to a single parent magma which is underwent fractional crystallization.This process commonly present as mineral assemblage at different stages, clinopyroxene in the quartz monzogabbro, clinopyroxene, hornblende and plagioclase in the quartz monzodiorite, and hornblende, plagioclase ± biotite thereafter.K-Feldspar, biotite and quartz are progressively concentrated in the granodiorite and granite, but did not separate from them in large amounts until the final stage of SiO 2 enrichment.The initial magma for the Neshveh intrusion was probably similar to the most mafic rock type exposed, the quartz monzogabbro, with about 52 wt% SiO 2 .

Figure 1 .
Figure 1.Schematic geological map of Iran, showing the distribution of the sedimentary and structural units and plutonic igneous rocks [after 16].Sahand-Bazman magmatic arc and studied area is shown on the map.merate equal to Fajan formation, volcanic-sedimentary rocks of Middle-Upper Eocene consist of intermediateacidic tuffs and lavas, agglomerate and intermediate-basic lavas along with the tuffaceous and sandy limestone and finally Upper Eocene ignimbrite, Lower Red Formation (conglomerate, sandstone, siltstone and red-brown marl), Qom Formation (limestone, marly limestone and marl), Upper Red Formation (conglomerate with red sandstone intercalation), Mio-Pliocene marl, conglomerate equal to Hezar Dareh Formation and quaternary alluvial deposits.Several granitoid intrusions were intruded into the Eocene volcanic-sedimentary rocks.Dating of some of these intrusions by[12] using K-Ar method on the amphibole, biotite, K-feldspar and whole rock indicate 28 -42 Ma (Table1).The Selijerd granodiorite, Khalkhab tonalite-diorite, Neshveh intrusion (this study) and Neivesht micro-granite are the most important intrusions in the northwest of Saveh.Neshveh intrusion composed of quartz monzogabbro, quartz monzodiorite, granodiorite and granite.In addition to mentioned intrusives, some subvolcanic domes also exist in different parts of the northwest Saveh that have acidic-intermediate composi-

Figure 3 .
Figure 3. Simplified geological map of NW Saveh intrusions (based on satellite data and the geological map of Saveh in1:100,000 scale [17]).

Figure 5 .
Figure 5. (A) Graphic intergrowth in the quartz monzodiorites; (B) Plagioclase crystal with different composition at the core and rim in the granodiorites.Abbreviations are after [20].

Figure 6 .
Figure 6.(A) Location of the analyzed clinopyroxenes on the Q-J diagram of Morimoto (1988); (B) Classifying of the analyzed clinopyroxenes based on Wo-En-Fs triangular diagram [21].

Figure 7 .
Figure 7. (A) Classification of the analyzed amphiboles based on occupancy of B location in the mineral structure by Ca and Na [22]; (B) and (C) Classifying of the analyzed amphiboles based on Mg/(Mg + Fe 2 ) vs. Si binary diagram [22].

Figure 8 .
Figure 8. (A) Classification of the analyzed biotites based on Fe/(Fe + Mg) vs. Al IV binary diagram; (B) Classification of the analyzed plagioclases based on the Or-Ab-An triangular diagram; (C) Classification of the analyzed alkali feldspars based on the Or-Ab-An triangular diagram.

Figure 9 .
Figure 9. (A) Plot of K 2 O vs. SiO 2 showing the calc-alkaline nature for the Neshveh intrusion [23]; (B) Decreasing of P 2 O 5 vs. SiO 2 indicating that Neshveh intrusion is I-type.

Figure 10 .
Figure 10.Selected major oxides vs. SiO 2 (wt%) contents for the Neshveh intrusion samples.The types of change that are typically seen during magmatic differentiation [44] [45] include: (a) major elements such as SiO 2 and K 2 O increase in abundance, but others such as TiO 2 , Fe 2 O 3 , MgO and CaO decrease, (b) Mg/Fe and Ca/Na ratios decrease, (c) concentrations of trace elements such as Rb, Sn, Cs, W and U rise, (d)those elements such as V, Cr,Ni, Zn and Sr fall, (e) some trace elements may rise or fall depending on whether or not the melt is saturated in the dominant mineral containing that element, e.g.Zr and Ba, (f) in some cases mineral saturation in felsic melts depends on whether the melt is I-or S-type, the most important example being apatite saturation which is a feature of felsic I-type melts (P falls) but not of more strongly peraluminous S-type melts (P rises).

Figure 12 .
Figure 12.Chondrite-normalized rare earth element plot of the Neshveh intrusion samples (A); Primitive mantle normalized trace element patterns (B).Studied samples are depleted in the incompatible HFSEs such as Nb and Ti which are relative to the primitive mantle.Normalization values after[28] and[29].

Figure 13 .
Figure 13.(A) Logarithmic evolution of concentrations for an incompatible element vs. a compatible element during crystal fractionation (1), batch partial melting (2), aggregate melting or fractional fusion with extraction of the mixed melts (3) and fractional fusion with continual removing of the melt formed (4).The initial material is (i) [53]; (B) and (C) Plots for the Neshveh intrusion samples showing near-vertical trends that suggest the main mechanism of differentiation is crystal fractionation.

Figure 14 .
Figure 14.(A) Sr vs. MgO plot showing that as Mg decreases, Sr increases.This relationship suggests plagioclase did not fractionate together with clinopyroxene in the rocks with MgO > 3.1 wt%; if it had, Sr as a compatible element in plagioclase, would decrease as MgO decreases [27]; (B) Rb vs. Sr diagram (logarithmic scale) showing the variation of Neshveh intrusion samples (solid vectors are Rayleigh fractionation trends after [54]).

Figure 15 .
Figure 15.The Neshveh intrusion samples follow the fractionated trends of hornblende on the Dy/Yb vs. SiO 2 (A) and Kf/Rb vs. Rb (B) diagrams.sults,hornblende fractionation only played a role in the formation of rocks with more than 62 wt% SiO 2 and consequently caused decrease of CaO, MgO and FeO in the magma.The role of plagioclase is best examined through Na 2 O, Sr and Eu trends in the representative samples.Na 2 O shows an inflected trend with increasing silica content, increasing up to 55 wt% SiO 2 and then decreasing (Figure10).Sr and Eu substitute for Ca and Na in plagioclase (but not in clinopyroxene); they have inflected trends in these samples that mimic that of Na 2 O.These trends can be interpreted as indicating that plagioclase fractionation was more important in the formation of rocks with SiO 2 > 55 wt% compared to the rocks with SiO 2 < 55 wt% (petrographic observations show that there is no significant change in the proportion of plagioclase up to this point, Table1).This is also the only reasonable explanation for the development of negative Eu anomalies in the granites.Thus, plagioclase would have had no effect on CaO, Na 2 O and Al 2 O 3 in the less siliceous rocks.Ba/Sr ratio will help to identify the relative roles of K-feldspar and plagioclase, since it increases with precipitation of plagioclase from the magma, but decreases when K-feldspar and biotite start to precipitate[58].In the Neshveh intrusion rocks, Ba/Sr is constant up to 55 wt% SiO 2 and then increases, showing the effect of plagioclase precipitation (Figure16).Ba concentration increases with increasing SiO 2 without any inflection (Figure11), suggesting that K-feldspar and biotite are late-crystallized minerals and/or sank very slowly in the co-existing melt during magmatic evolution[59].Essentially, constant K/Rb ratios (Figure14(B)) and the positive correlation between K 2 O and SiO 2 (Figure11) are also consistent with no K-feldspar removal.In addition,

Figure 16 .
Figure 16.Increasing Ba/Sr vs. SiO 2 indicates fractionation of pla-gioc1ase rather than K-feldspar in the Neshveh intrusion.thelack of K-feldspar and biotite fractionations are also confirmed by the absence of a negative Ba anomaly in the primitive mantlenormalized rare earth element patterns (Figure12(B)).Fractionation of biotite and K-feldspar should buffer or reduce Ba in the residual liquid[60].K 2 O and Ba contents increase from 1.21 wt% and 247 ppm, respectively, in quartz monzogabbro to 5.14 wt% and 808 ppm in granite (Figure10and Figure11; Table2), indicating that biotite and K-feldspar crystallized late or sank very slowly in co-existing melt during magmatic differentiation.As presented in Table1, biotite content decreases in the granitic samples, thus increasing of Ba in these samples is mostly related to late-crystallize Kfeldspar in the magma.The regular decrease in P 2 O 5 content from the quartz monzogabbroic to granitic rocks (Figure10) is attributed to fractionation of apatite[9].Ti-bearing minerals such as ilmenite and titanite might be other fractionated phases in the Neshveh intrusion, as indicated by the decrease of TiO 2 with increasing SiO 2 (Figure10).Moreover, as hornblende and biotite fractionated from the magma forming rocks with SiO 2 >~ 62 wt%, a combination of ilmenite, titanite, hornblende and biotite fractionations can be considered responsible for the decreasing TiO 2 in granodioritic and granitic melts.There is a larger negative Ti anomaly in the granitic rocks and decreasing Dy/Yb ratio vs. SiO 2 in the representative samples (Figure12(B) and Figure15(A)).

Table 1 .
Modal mineralogical compositions of the Neshveh intrusion rocks.

Table 2 .
EPMA analysis of different minerals in the Neshveh intrusion samples.