The study area is located in Kerman province, 38 Km NE of Zarand town. This area is a part of the central Iranian microplate situated between Kuh-Banan and Davaran faults in east and west, respectively [1] . Metallogenically, the region makes the southeastern part of the Bafq mining district [2] . The Zarand region contains several iron ore deposits sporadically being mined of which the Jalal-Abad iron mine has a reserve of about 200 million tons (Mt) of iron ore. The Jalal-Abad iron ore deposit is, volumetrically, mostly composed of magnetite. The aim of this study is to investigate the geochemical distribution of REE and heavy elements in the western part of the Jalal-Abad iron ore deposit in the Zarand region.

The study area is mostly covered by volcano-sedimentary rocks associated with rhyolitic and rhyodacitic lavas, dykes, pyroclastic rocks, tuffs and ignimbrites [3] . Intercalations of sedimentary rocks, such as dolostone, limestone, sandstone and siltstone are also included (Figure 1). Gray sandstones and sandy shales, with heterogenous composition, along with tillites and conglomeratic fragments of carbonate rocks in a fine grain matrix (diamictite) form the lower part of the stratigraphic units of the region. Spilitized basic and acidic volcanic rocks are found with magnetite and hematite ore rocks. Carbonate rocks, cherty dolomites and dolostones associated with jaspilites are found in the upper parts of this succession. Dolomitic carbanate rocks thoroughly cover the upper part of the series. The host rock for the iron ore deposit is a dolomitized limestone unit (Figure 2) [4] .

In addition, subvolcanic units as dykes and sills (microgabbro and microdiorite) also outcrop in the area. Investigations by Ale-Taha-Kuhbanani (1994) [5] indicate that the basic magmas in the study area belong to alkaline series, whereas the acidic magmas are in the field of calk-alkaline rocks. Geochemical composition of these rocks, in the study area, indicates an intra-continental rift setting for this region. According to Mohseni (2007) [6] , the iron ore deposits of the central Iranian iron ore field are BIF-type iron ore deposits formed in a sedimentary environment dominantly affected by submarine exhalative activities noting the occurrence of distinct keratophyre-jaspilite-diamictite associations and the observation of glacial erratics and dropstones in the enclosing sediments.

Mineralization in the Jalal Abad ore deposit is hosted by siltstones, shaly siltstones, acidic volcanic rocks and dolomitic limestones. The Jalal-Abad iron deposit mainly consist of magnetite ore showing a range of primary to post-mineralization textures including, massive, disseminated and cataclastic textures. Hematite is mainly found near the surface levels. Pyrite is widely distributed in the Jalal-Abad ore deposit and hosted much of the sulfur in the ore. Chalcopyrite as the second mineral in abundance after pyrite is the most important copper-bearing mineral mainly observed as irregular veins and open-space filling bodies. Sulfide mineralization can be envisaged as a late-stage phase which occurs as secondary fracture-filling veins and veinlets within the host iron ore minerals [7] . The primary minerals are intensely altered to iron hydroxides and copper carbonates, such as malachite and azurite. Quartz is associated with magnetite, pyrite, hematite, chalcopyrite and calcite which shows higher concentrations in the lower parts and oxidized part of the ore deposit. Carbonate minerals, mainly calcite and dolomite, occur more abundantly around the ore deposit. Calcite and dolomite filled the open spaces and fractures in the oxidized zone and form the matrix of the iron ore in the mineralized parts where it occurs in dolomitic limestones. Dolomite is dominantly replaced by talc and actinolite [8] .

Alteration as occurs in the haloes around the ore deposit. Chlorite, quartz, calcite, sericite and epidote are the main alteration minerals in the study area (Figure 3) [9] . Chlorite is associated with quartz-chlorite, quartz- chlorite-calcite, and quartz-chlorite-pyrite mineral assemblages. Silicification occurred as veins, veinlets and open-space fillings.

The study area covering a region of 119 hectars extending 1250 m EW and 950 m SN was chosen for surveying

the surface geochemical distribution of the certian elements. 44 samples were collected, including 14 samples from drilling holes and 30 samples from the surface materials. The Jalal Abad System was sampled from October 10 to 25 in the year 2013. 30 sampling along the Veins and Altration in Western Part were selected.. Chip samples are taken from veins and alteration. The average volume of the samples was 3 kg. The samples were then analyzed by XRF in the commercial lab of Kansaran Binaloud, Tehran, Iran. The surface samples were collected from three exploration districts. The locations of the collected samples are shown in Figure 4.

The common statistical techniques were used to construct maps based on the frequency distribution of the elements. Since this study was aimed at examining the frequency distribution of the precious metals associated with Fe and REE, the distribution map of the normal data was drawn (Figure 8 & Figure 9). Surfer software was used for drawing the maps and Inverse Distance Squared method was utilized for estimating the data points by multivariate interpolation. The map coloration was based on the frequency percentage values in Table 5. 5 colors including red, orange, yellow, green and blue were used for the elements in Table 5.

Cu and Ti are proposed to be associated with Fe in the Jalal-Abad exploration area. The concentrations of Cu, Ti and REE in the collected samples are low. Geochemical distribution maps of the elements indicate that the distribution of TiO₂ in most other areas is at background values and in some areas is lower than the background and only in limited parts (in NW of the area) show anomalous values. Cu distribution in the eastern part of the area is at the background and in the western part is lower than the background. Two smaller parts in the southern part of the area show Cu concentrations near to the threshold values. The combined concentration of Ce, La and Y indicates that in most places they are in the range of background, values whereas in some places they reach threshold amounts. Separation of two groups of rare earth elements (HREE and LREE) function Mineralogy is unaltered stones. The difference Due to the separation of the REE in the capacity of cationic The different environments [11] -[13] .

The results of analysis of 14 samples collected from drilled holes show average TiO₂ values of 2227 ppm while the surface samples collected have on average 1420 ppm of TiO₂. Moreover, average Cu concentration reaches 135 and 2911 ppm in the drilled holes and in the surface samples, respectively. The average amount of V and REE in the drilled hole samples is slightly more than the average amount of these elements in the surface samples. This evidence suggests that Ti content is higher in depth in comparison with the shallower parts. Moreover, oxidation of the copper sulfide samples resulted in the accumulation of Cu oxides, with higher Cu concentrations, on the surface. The results of the chemical analysis of the iron ore samples in the Jalal-Abad area show low Ti and P contents. Furthermore, low-P iron mineralization occurs in the area. The results of chemical analysis by XRF indicate copper enrichments (up to 2500 ppm) related to malachite and azurite mineralization.

[6] Has compared the chemical composition of a Jaspilitic iron ore sample with the host rocks of the BIF-type iron deposits showing a similar enrichment for two rock samples in LREE related to the concentration of such elements in OH-bearing minerals like chlorite, talc and sericite which in turn suggest high water/rock ratios during the exhalative hydrothermal water interactions. In a similarly manner, [6] [14] also show that the REE distribution pattern matches that of the oceanic waters. Eu shows negative anomaly in this pattern indicating the effect of hydrothermal processes on acidic rocks containing Ca-rich plagioclase with large amounts of detrital and diamictitic sediments involved in the process.

Magnetite is the main ore mineral in Jalal-Abad iron deposit, mainly in deeper parts where the original mineralization escaped the surface weathering processes. Hematite formed as a secondary mineral during the oxidation of magnetite, largely found in shallow levels and enriched in the crashed zones. The ore minerals include magnetite, hematite, pyrite, chalcopyrite, limonite, goethite, malachite and azurite. Cu and Ti are among the associated elements with iron in the ore samples. The geochemical distribution maps of the elements indicate that TiO₂ distribution is as much as the background contents; however, in some parts, it is characterized by a negative anomaly. Cu concentration in the eastern part is at the background values, whereas, in the western part it shows a negative anomaly. The combined concentrations of Ce, La and Y show background values for most areas, although in some cases higher, threshold values have been measured. The average TiO₂ content in the drilled core and surface samples reaches 2227 and 1420 ppm, respectively. The average copper contents in the drilled core and the surface samples are 135 and 2911 ppm, respectively. The Pearson correlation coefficient values show a good correlation between Cu and Cl. The strong correlation among Pb, Zn and Sr suggests a common source for these elements. Also, there is a strong and positive correlation among La with Ce and Y. A close association between Cu and Cl with metasomatic host rock, and among Pb, Zn and Ba with carbonate host rocks are also indicated.

Four geochemical associations identified by cluster analysis (using dendrograms) in the Jalal-Abad deposit include La and Ce associated with Ba, Nb, W, Y; TiO₂ and Zr in association with Cr and V; Ga and Rb associated with Mo and U; and Th, As and Cu associated with Co, Ni, Pb and Zn. In the factor analysis performed, six factors were introduced as followed: the first factor comprises TiO₂, Ce, La, W, Zr, Y, Rb, Nb and Sr; The second factor comprises Co, As and Mo; The third factor comprises Pb, Zn and Ba; The forth factor comprises Ni, Cu and Cl; The fifth factor comprises Cr and V; and the sixth factor comprises Ga and Th.

AbdollahYazdi,SajadZiaaldini,RahimDabiri, (2015) Investigation on the Geochemical Distribution of REE and Heavy Metals in Western Part of Jalal-Abad Iron Ore Deposit, Zarand, SE of Iran. Open Journal of Ecology,05,460-476. doi: 10.4236/oje.2015.59038