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.
4. Petrography
4.1. Quartz Monzogabbro
The quartz monzogabbro is poorly exposed in the western part of the Neshveh intrusion and was intruded into the volcanic rocks (Figure 3). It occupies about 50% of the pluton and is medium to coarse-grained with various textures; some samples show inter-granular and poiklitic textures, while others show hetero-granular texture (Figure 4(A)). The inter-granular texture is constituted by grains of clinopyroxene which occupy the angular interstices between plagioclase crystals. The quartz monzogabbro consists dominantly of plagioclase (51.5 - 55.6 modal %), clinopyroxene (20.2% - 25.7%), K-feldspar (9% - 14.1%), quartz (7.9% - 11.7%), and subordinate opaque minerals (2.3% - 3.5%) and apatite (0.6%) (Table 1).
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.
4.2. Quartz Monzodiorite
The quartz monzodiorite surrounds the granodiorite and granite. To the west, quartz monzodiorite is transitional to more mafic rocks, the quartz monzogabbro while to the east it forms the margin of the pluton (Figure 3). The
quartz monzodiorite is generally medium-grained and characterized by equigranular texture. It consists dominantly of plagioclase (41.1 - 52.4 modal %), K-feldspar (9% - 19%), quartz (10.9% - 18.4%), hornblende (6.9% - 16.3%), subordinatesclinopyroxene (0% - 12.1%), biotite (2.5% - 5%) and opaque minerals (2.3% - 3%) (Table 1). Accessory minerals such as titanite and apatite are rare. Clinopyroxene is subhedral and, in some samples, replaced by hornblende, actinolite and biotite aggregates. Hornblende is common in the quartz monzodiorite, where it occurs as euhedral to subhedral and isolated crystals, sometimes accompanied by biotite (Figure 4(B)). Minor interstitial quartz occurs in crude graphic intergrowth with K-feldspar (Figure 5(A)). Opaque minerals are rare but typically form euhedral grains.
4.3. Granodiorite
About 20% of the Neshveh intrusion is constituted by granodiorite, emplaced within the quartz monzodiorite hosted by volcanic rocks. It is relatively homogeneous, white to pale grey massive rocks with a medium-grained texture. The mineral assemblages consist of plagioclase (41.1 - 44.7 modal %), K-feldspar (15% - 25%), quartz (19.5% - 21.3%), hornblende (11% - 12.3%), biotite (0% - 5.4%), opaque minerals (1.2% - 2.9%) and clinopyroxene (<1.2%), with traces of accessory minerals. Mafic phases are well-formed hornblende and biotite. Biotite forms individual crystals in the granodiorites and is sometimes observed in contact with euhedral to subhedral hornblende crystals (Figure 4(C)). Plagioclase occurs as zoned subhedral crystals, 0.3 - 1 mm in diameter and usually twinned. Also, there are some plagioclases that have different composition in the core and rim (Figure 5(B)). Subhedral to anhedral K-feldspar crystals have locally microperthitic texture.
4.4. Granite
5. 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.
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] .
Table 2. EPMA analysis of different minerals in the Neshveh intrusion samples.
Continued
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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 + Fe2) vs. Si binary diagrams.
Chemical composition and classifying of biotite were done by using Fe/(Fe + Mg) vs. AlIV 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 + Fe2) 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. AlIV 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
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. (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 + Fe2) vs. Si binary diagram [22] .
Figure 8. (A) Classification of the analyzed biotites based on Fe/(Fe + Mg) vs. AlIV 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.
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)).
6. 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 SiO2 vs. K2O diagram [23] , which are the samples all plot within the medium to high-K calcalkaline field (Figure 9). The molecular ratio of Al2O3/(CaO + Na2O + K2O) ranges from 0.73 to 1, exhibiting metaluminous characteristics [15] . Features such as Na2O > K2O, A/CNK < 1, decreasing P2O5 versus SiO2 [24] and SiO2 vs. K2O [25] and ACNK versus SiO2 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 Na2O/K2O (1.53) and Na2O + K2O (5.33) (Table 3).
The Neshveh intrusion rocks have a wide range in SiO2 (52.1% - 71.2%), Fe2O3, MgO, MnO, CaO, TiO2 and P2O5 (Table 3). Most major elements except Al2O3, Na2O and K2O show negative linear trends with increasing SiO2 (Figure 10). K2O shows a descending trend, while Al2O3 and Na2O have bent trends. Na2O is positive up to 62 wt% SiO2 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% SiO2 (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 Table 3. Major (wt. %) and trace element (ppm) abundances in Neshveh intrusion samples.
Continued
Figure 9. (A) Plot of K2O vs. SiO2 showing the calc-alkaline nature for the Neshveh intrusion [23] ; (B) Decreasing of P2O5 vs. SiO2 indicating that Neshveh intrusion is I-type.
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.
7. 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] .
Figure 10. Selected major oxides vs. SiO2 (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 SiO2 and K2O increase in abundance, but others such as TiO2, Fe2O3, 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 Ior 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 11. Selected trace elements (ppm) vs. SiO2 (wt%) contents for the Neshveh intrusion samples.
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] .
7.1. 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 Na2O, Al2O3, 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 increasingSiO2, 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 -
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.
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.
7.2. Mineral Controls
A general crystal fractionation trend within the representative samples is indicated by decreasing TiO2, MgO, Fe2O3, CaO and P2O5 concentrations, and increasing K2O together with most of the trace elements, e.g., Ba, Rb, La and Ce (Figure 10 and Figure 11). Some elements such as Na2O, Al2O3, 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.% SiO2) 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, Fe2O3, 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 SiO2 > 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% SiO2 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-
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. The Neshveh intrusion samples follow the fractionated trends of hornblende on the Dy/Yb vs. SiO2 (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% SiO2 and consequently caused decrease of CaO, MgO and FeO in the magma.
The role of plagioclase is best examined through Na2O, Sr and Eu trends in the representative samples. Na2O shows an inflected trend with increasing silica content, increasing up to 55 wt% SiO2 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 Na2O. These trends can be interpreted as indicating that plagioclase fractionation was more important in the formation of rocks with SiO2 > 55 wt% compared to the rocks with SiO2 < 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, Na2O and Al2O3 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% SiO2 and then increases, showing the effect of plagioclase precipitation (Figure 16). Ba concentration increases with increasing SiO2without 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 K2O and SiO2 (Figure 11) are also consistent with no K-feldspar removal. In addition,
Figure 16. Increasing Ba/Sr vs. SiO2 indicates fractionation of plagioc1ase rather than K-feldspar in the Neshveh intrusion.
the lack 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 (Figure 12(B)).
Fractionation of biotite and K-feldspar should buffer or reduce Ba in the residual liquid [60] . K2O 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 P2O5 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 TiO2 with increasing SiO2 (Figure 10). Moreover, as hornblende and biotite fractionated from the magma forming rocks with SiO2 >~ 62 wt%, a combination of ilmenite, titanite, hornblende and biotite fractionations can be considered responsible for the decreasing TiO2 in granodioritic and granitic melts. There is a larger negative Ti anomaly in the granitic rocks and decreasing Dy/Yb ratio vs. SiO2in the representative samples (Figure 12(B) and Figure 15(A)).
8. 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 SiO2enrichment. The initial magma for the Neshveh intrusion was probably similar to the most mafic rock type exposed, the quartz monzogabbro, with about 52 wt% SiO2.
Acknowledgements
This study was financially support by Research Deputy of Tehran University for the proposal entitled Petrography and Petrology of Neshveh intrusion (northwest Saveh). Our gratitude is expressed to their helps.
NOTES
*Corresponding author.