Journal of Geological Research
Volume 2014 (2014), Article ID 590540, 25 pages
http://dx.doi.org/10.1155/2014/590540

Research Article

Geochemistry, Paragenesis, and Wall-Rock Alteration of the Qatruyeh Iron Deposits, Southwest of Iran: Implications for a Hydrothermal-Metasomatic Genetic Model

Sina Asadi and Mohammad Ali Rajabzadeh

Department of Earth Sciences, Faculty of Sciences, Shiraz University, Shiraz 7146713565, Iran

Received 16 June 2014; Accepted 27 August 2014; Published 22 October 2014

Academic Editor: Salvatore Gambino

Copyright © 2014 Sina Asadi and Mohammad Ali Rajabzadeh. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract.

The Qatruyeh iron deposits, located on the eastern border of the NW-SE trending Sanandaj-Sirjan metamorphic zone, southwest of Iran, are hosted by a late Proterozoic to early Paleozoic sequence dominated by metamorphosed carbonate rocks. The magnetite ores occurred as layered to massive bodies, with lesser amounts of disseminated magnetite and hematite-bearing veins. Textural evidences, along with geochemical analyses of the high field strengths (HFSEs), large ion lithophiles (LILEs), and rare earth elements (REEs), indicate that the main mineralization stage occurred as low-grade layered magnetite ores due to high-temperature hydrothermal fluids accompanied by Na-Ca alteration. Most of the main ore-stage minerals precipitated from an aqueous-carbonic fluid (3.5–15 wt.% NaCl equiv.) at temperatures ranging between 300° and 410°C during fluid mixing process, CO₂ effervescence, cooling, and increasing of pH. Low-temperature hydrothermal activity subsequently produced hematite ores associated with propylitic alteration. The metacarbonate host rocks are LILE-depleted and HFSE-enriched due to metasomatic alteration.

1. Introduction

The last decade has seen major progress in our understanding of the origin of iron ore deposits worldwide. The majority of interpretations focused on the igneous iron oxide deposits either having formed by magmatic liquid immiscibility [1–7] or by hydrothermal alteration and replacement [8–14]. The hydrothermal iron deposits generally are found at many locations around the Pacific basin, Central America, Australia, and Japan [15]. They are commercially far less important as global source of iron than banded iron formations and igneous iron deposits, except for many countries without these types of iron deposits. Genetic models for hydrothermal Fe-oxide deposits associated with hybrid magmatic to nonmagmatic fluids, which locally mix at the trap site [16], suggest that metamorphic processes or a primary felsic to intermediate intrusion could be regarded as source of the majority of hydrothermal fluids and metals [17, 18]. Therefore, metasomatic iron-rich fluid regimes are associated with magmatism or metamorphism, or both. Depending on the physicochemical conditions the protore iron mineralization could consist of magnetite or hematite, or a mix of the two. They occur in different tectonic environments, such as intracontinental terranes associated with anorogenic magmatism, continental arc terranes, and metamorphic belts [18–20].

The most favorable area for hydrothermal ore deposits in Iran is the Sanandaj-Sirjan zone (SSZ), which has a NW-SE trend and is characterized by magmatism-metamorphism and an obliquely thrusted wedge, with asymmetrical structures in the HP-LT metamorphic rocks [21]. This metamorphic belt contains abundance of iron ore deposits, including the Gol-Gohar (Kerman), Totak, Dehbid (Fars), Galali, Baba-Ali (Hamedan), and Shams-Abad (Arak). However, distribution of these deposits from NW toward SE Sanandaj-Sirjan is very important but the origin of these deposits has been a subject of heated debate. Eshraghi et al. [21] were the first to present the details of the geology and genesis of the Gol-Gohar and the Qatruyeh deposits and proposed metamorphism as main factor controlling the mineralization. However, based on textural and geochemical evidence, [22–24] suggested iron oxide-copper-gold (IOCG) origin for Sanandaj-Sirjan iron deposits. According to [25], the iron deposits from Hamadan to Gol-Gohar situated in the Sanandaj-Sirjan zone about 1200 km apart and show striking mineralogical and textural similarities. They believed that the ore bodies are of magmatic origin and formed at late stages of hydrothermal conditions.

In spite of the existence of the important iron ore deposits in the Qatruyeh area, there are a few reports on the ores with no exploitation activities. This paper presents detailed field observations, mineralogical alteration assemblages, textural relationships, fluid inclusions and geochemical data on the ore bodies, and the associated dolomitic-marble host and plutonic rocks at the Qatruyeh iron ores, southwest of Iran, in order to reveal a genetic model for the deposits in the area.

2. Methods

Major and trace elements analyses were carried out on representative samples using inductively coupled plasma optical emission spectroscopy (ICP-OES), with 0.1 ppm detection limit at Geological Survey of Iran (22 ore samples), and using standard wet chemical analysis by flame atomic absorption spectrophotometry (FAAS), with 0.5 ppm detection limit at the Department of Earth Sciences, at Shiraz University (5 fresh marbles, 11 altered marbles, and 12 diorites). Rare earth elements (REE) were analyzed by inductively coupled plasma mass spectrometry (ICP-MS) with 0.01 ppm detection limit at ALS Chemex Analytical Services, Canada (4 diorites and 22 ore samples). Sample locations are shown in Table 1 and they are described with regard to type of analyses.

Table 1: Location and description of samples used for fluid inclusion and chemical analyses.

Sample
Field number
Easting
Northing
Type of analysis

Chah Anjir plutonic rocks
CAP 1
54°34′22.6′′
29°14′00.7′′
ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 2
54°34′27.8′′
29°14′14.7′′
ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 3
54°33′24.2′′
29°13′00.5′′
ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 4
54°34′19.7′′
29°14′26.1′′
ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 5
54°34′22.6′′
29°14′00.3′′
ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 6
54°33′22.5′′
29°14′00.9′′
ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 7
54°34′34.4′′
29°14′12.0′′
ICP-MS, ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 8
54°34′34.6′′
29°14′12.0′′
ICP-MS, ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 9
54°34′34.6′′
29°14′12.0′′
ICP-MS, ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 10
54°34′34.6′′
29°14′12.0′′
ICP-MS, ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 11
54°33′43.7′′
29°14′05.5′′
ICP-OES, FAAS

Chah Anjir plutonic rocks
CAP 12
54°33′43.7′′
29°14′05.5′′
ICP-OES, FAAS

Hematite ore
H1
54°35′21.1′′
29°16′46.3′′
ICP-MS, ICP-OES, FAAS

Hematite ore
H2
54°35′03.8′′
29°15′03.4′′
ICP-MS, ICP-OES, FAAS

Hematite ore
H3
54°40′32.7′′
29°14′13.6′′
ICP-MS, ICP-OES, FAAS

Massive magnetite ore
MM1
54°36′20.0′′
29°15′30.0′′
ICP-MS, ICP-OES, FAAS

Massive magnetite ore
MM2
54°35′56.8′′
29°16′14.4′′
ICP-OES, FAAS

Massive magnetite ore
MM3
54°36′40.3′′
29°15′35.1′′
ICP-OES, FAAS

Massive magnetite ore
MM4
54°36′00.0′′
29°15′36.2′′
ICP-OES, FAAS

Massive magnetite ore
MM5
54°36′00.4′′
29°15′32.6′′
ICP-OES, FAAS

Massive magnetite ore
MM6
54°36′10.0′′
29°15′36.1′′
ICP-MS, ICP-OES, FAAS

Massive magnetite ore
MM7
54°36′12.1′′
29°15′36.2′′
ICP-MS, ICP-OES, FAAS

Massive magnetite ore
MM8
54°36′20.4′′
29°15′30.0′′
ICP-MS, ICP-OES, FAAS

Layered magnetite ore
LM1
54°41′59.9′′
29°15′28.9′′
ICP-MS, ICP-OES, FAAS

Layered magnetite ore
LM2
54°39′40.0′′
29°14′11.2′′
ICP-MS, ICP-OES, FAAS, FI

Layered magnetite ore
LM3
54°39′26.3′′
29°14′14.7′′
ICP-MS, ICP-OES, FAAS

Layered magnetite ore
LM4
54°39′29.1′′
29°14′21.1′′
ICP-OES, FAAS, FI

Layered magnetite ore
LM5
54°39′40.0′′
29°14′21.7′′
ICP-OES, FAAS, FI

Layered magnetite ore
LM6
54°39′29.5′′
29°14′21.2′′
ICP-OES, FAAS, FI

Layered magnetite ore
LM7
54°39′40.3′′
29°14′21.3′′
ICP-OES, FAAS, FI

Layered magnetite ore
LM8
54°39′27.6′′
29°14′16.4′′
ICP-OES, FAAS, FI

Layered magnetite ore
LM9
54°39′29.5′′
29°14′21.2′′
ICP-MS, ICP-OES, FAAS

Layered magnetite ore
LM10
54°39′21.1′′
29°14′08.2′′
ICP-MS, ICP-OES, FAAS

Layered magnetite ore
LM11
54°39′29.3′′
29°13′57.7′′
ICP-MS, ICP-OES, FAAS

Fresh dolomitic marble
FM 1
54°39′40.0′′
29°14′21.7′′
ICP-MS, ICP-OES, FAAS

Fresh dolomitic marble
FM 2
54°40′00.0′′
29°14′24.5′′
ICP-MS, ICP-OES, FAAS

Fresh dolomitic marble
FM 3
54°39′33.5′′
29°13′59.0′′
ICP-MS, ICP-OES, FAAS

Fresh dolomitic marble
FM 4
54°39′31.2′′
29°14′22.0′′
ICP-MS, ICP-OES, FAAS

Fresh dolomitic marble
FM 5
54°39′37.9′′
29°14′0.04′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 1
54°40′20.4′′
29°14′11.3′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 2
54°39′38.0′′
29°14′00.6′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 3
54°35′30.0′′
29°16′21.7′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 4
54°35′36.2′′
29°16′29.0′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 5
54°35′42.0′′
29°16′11.1′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 6
54°35′39.0′′
29°16′22.0′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 7
54°39′40.1′′
29°14′21.8′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 8
54°39′29.5′′
29°14′21.2′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 9
54°40′32.7′′
29°14′13.6′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 10
54°39′40.3′′
29°14′11.0′′
ICP-MS, ICP-OES, FAAS

Altered dolomitic marble
AM 11
54°36′20.6′′
29°15′30.8′′
ICP-MS, ICP-OES, FAAS

ICP-MS = inductively coupled plasma mass spectrometry, NICP-OES = inductively coupled plasma optical emission spectroscopy, FAAS = flame atomic absorption spectrophotometry, and FI = fluid inclusion.

3. Geological Setting and Lithostratigraphy

The Qatruyeh area is located about 50 km NE of Neyriz and lies within the Zagros orogenic belt in SW of Iran. The Zagros orogenic belt of Iran consists of three parallel tectonic domains: (1) the Urumieh-Dokhtar magmatic belt (UDMB), (2) the Sanandaj-Sirjan zone (SSZ), and (3) the Zagros folded-thrust belt (ZFTB) [35]. The iron deposits are located in the eastern margin of the NW-SE trending Sanandaj-Sirjan zone (Figure 1).

Figure 1: Schematic geological map of the Qatruyeh area and tectonic scheme of Iran and interpretative cross section A-A′ from south to north.

The SSZ consists of Paleozoic to Triassic high-grade metamorphic rocks overlaid by Mesozoic metasedimentary strata. The Mesozoic sediments were deposited along a passive continental margin [36–39] and subsequently large-scale Mesozoic plutons ranging from gabbro to granite, emplaced in about  Ma by the K-Ar methods [40]. The ore bodies show a strong deformation in parallel to the regional west-northwest structural trend. Lithostratigraphic relationships in the Qatruyeh area are summarized in Figure 2. Some researchers [40, 41] recognized five rock groups in Neyriz area, from base to top and from low- to high-grade metamorphic rocks, which are unconformably overlaid by Upper Triassic turbiditc rocks and basalt. These groups include the following.

Figure 2: Summarized schematic lithostratigraphic column in the Qatruyeh area.

Group A. Homogeneous orthogneiss with some amphibolite lenses and small bodies of anatectic granite. The orthogneiss has been dated by U-Pb method on zircons, at 520 Ma [41].

Group B. Alternation of amphibolite, migmatite, minor micaschist, marble, and metamorphosed mafic and ultramafic rocks. The age of the metamorphic rocks is 310 Ma based on ⁴⁰K-⁴⁰Ar dating method on extracted white mica, biotite, plagioclase, and amphibole.

Group C. Micaschist, calc-schist, marble, minor amphibolite, and mafic to ultramafic rocks. Along the Sanandaj-Sirjan zone, comparable rocks yielded deformed Devonian corals [21, 42, 43]. The Chah Pazhan metagabbro contains medium-grained clinopyroxene (e.g., augite, hedenbergite, and pigeonite), plagioclase feldspar, and orthopyroxenes (e.g., enstatite). The clinopyroxenes have been amphibolized and uralitized (actinolitization-tremolitization).

Group D. Schist, slate, calc-schist, metabasite, quartzite, and intercalations of marble. The metacarbonate intercalations are more frequent towards the upper part of the group. Palynomorphs (Galyptosporites, Laevigatosporites, Polyedrxium sp., Ancyspora sp., Geminospora sp., and Relusotrilletes sp.) indicate a late Devonian-early Carboniferous age for this group [21].

Group E. Limestone, dolomite, basalt, and synsedimentary monogenetic breccias. Above the early Cimmerian unconformity, the Upper Triassic and Jurassic sequence were deposited in turbiditic basins, geometry of which is still poorly known [40]. These rocks show a weak but obvious cleavage, indicative of a deformation that affects the upper Triassic and Jurassic conglomerates and sandstones, but not the overlying Cretaceous series in adjacent areas.

The Deh Vazir Jurassic deformed conglomerate is located in the north part of the area and is sandwiched between two thrust sheets which are part of the Main Zagros Thrust zone. Most of the pebbles in this conglomerate consist of micaschist and phyllite [44], but at some localities, the presence of massive magnetite pebbles indicates the ore formation is prior to main metamorphism (Laramide phase) (Figure 3(a)). The conglomerate was occurred extensively in the area which covers metamorphosed limestones, turbidite shales, and sandstones.

(a)

(b)

(c)

(d)

(e)

(f)

Figure 3: Photographs illustrating aspects of structures in the magnetite-hematite ores and host rock. (a) Massive magnetite pebbles within the Jurassic Deh Vazir conglomerate, (b) rhythmic banding and boudinage deformation of hematite and marble, (c) layered magnetite within dolomitic marble, (d) disseminated magnetite mineralization in chlorite-schist (magnetite chlorite-schist), (e) hematite veins with a mylonitic structure show evidence for strong ductile deformation, (f) quartz + pyrite ± chalcopyrite ± hematite secondary veins cut dolomitic marble and massive magnetite. Magnet size: 3 cm. (f) Mineral abbreviations: Ccp = chalcopyrite, Hem = hematite, and Py = pyrite.

4. Deformation and Metamorphism

The SSZ underwent polyphase deformation events during the Mesozoic era. The latest event recorded in the rocks reflects collision of the Afro-Arabian continent and Iranian microcontinents and subsequent southward propagation of the fold-thrust belt [39, 45, 46]. Geological and textural information suggest that there are at least three main deformation phases D₁, D₂, and D₃ [47].

The regional lithologies at the Qatruyeh record a clockwise metamorphic path followed by thrust deformation events. The peak pressure and temperature in the upper Triassic and Jurassic sequences were estimated at  kbar and °C, respectively. Using zircon sensitive high-resolution ion microprobe (SHRIMP) U-Pb and monazite chemical Th-U-total Pb isochron methods (CHIME) presumably regional metamorphic event occurred between  Ma and  Ma, respectively. These rocks experienced clockwise P-T path and thrusted into the imbricate slices during exhumation [48]. The amphibolite facies metamorphism in early Cimmerian orogeny could be correlated with the regional D₁ deformation. Exhumation of the metamorphic complexes and the resultant cooling and decompression of the metamorphic rocks followed by development of postearly Cimmerian sedimentary basins occurred in a transpressive regime due to subduction of the Neotethys. As a result, calc-alkaline mafic to felsic intrusive rocks were emplaced in the northeastern part of the region. A high-pressure-low-temperature metamorphic belt was formed during the first stage of the deformation. The result of this deformation is a composite foliation between massive magnetite and dolomitic marble that occurred along a wide ductile shear zone [40].

The D₂ deformation is associated with overthrusting of the old units (e.g., the Chah Pazhan ultramafic-mafic rocks) onto the Qatruyeh metacarbonate unit and the development of a mylonitic foliation in the various rocks units. Veinlets of iron oxides display pinch and swell features along the foliation. These relationships indicate that percolating fluids moved through permeable zones of foliation. The resulting boudinage show that ductile deformation went on after formation of iron oxides (hematite) and dolomitic-marble host rock (Figure 3(b)).

Whereas D₁ and D₂ developed under amphibolite and greenschist facies metamorphic conditions, D₃ represents an event leading to the development of kink bands, localized shear zones, and slickensides along the thrust sheet of the Qatruyeh area [47]. Abundant kink bands of several centimeter thicknesses overprinted all other deformation structures such as both magnetite and hematite ores.

5. Ore Bodies’ Geology

There are twelve ore bodies in the Qatruyeh area. Kuh-Sorkh and Kuh-Ghermez were chosen for detailed field investigation, petrography, and chemical analyses. Both ore bodies occur within the metasedimentary rocks of the early Paleozoic which consists predominantly of dolomitic limestone, greenschist, and quartzite (group B). The iron oxide ores can be divided into massive and layered magnetite ores with minor hematite. The ore bodies were not exploited due to their low tonnages in the area.

The massive magnetite ore bodies are often in contact with micaschist and dolomitic marble. They occurred often as very small sized masses with maximum 5 m² area which replaced metacarbonates. The ore bodies have variable orientation and shape and commonly have been fractured and cut by quartz-bearing hematite veins. The layered magnetite ores, however, have few centimeters to several meters width (>10 m) and are found throughout the area interbedded with the stratified metacarbonate rocks (Figure 3(c)). These host rocks were strongly affected by sodic-calcic alteration. These sodic-calcic alteration zones are spatially associated with layered magnetite bodies that appear to have replaced marbles, dolomitic marbles, and chlorite-schist rocks. Pervasive sodic-calcic alteration grades into zones of layered, actinolite crystals intergrown with magnetite. Most intense sodic-calcic alteration is dominated by pervasive rock replacement by siderite + paragonite with associated layered magnetite ores. The ores are most often horizontal to subhorizontal and elongated WNW-ESE trending, concordant with the regional structures.

Minor disseminated subhedral to euhedral magnetites are common in the area, dominantly appears in chlorite-schist (Figure 3(d)). Minor hematite occurrences are found in the upper parts of the brecciated and mylonitized metacarbonates (Figure 3(e)) that display propylitic alteration near the fault contact.

The metacarbonates and chlorite-schists adjacent to intrusive rocks (intrusions) are crossed by later veins of hematite + quartz ± pyrite ± chalcopyrite (Figure 3(f)). Such veins are generally poorly mineralized and appear to represent a late, high-level zone of hydrothermal alteration.

6. Petrography

The metamorphic rocks are extensively formed in the Qatruyeh area which is composed of metacarbonate rocks (marble and dolomitic marble), chlorite-schist, micaschist, and metagabbroic schist with small amounts of amphibolite. A heterogeneous intrusion with about 1 km in diameter is located in the south of the area showing a chilled margin. It has been emplaced within the calcareous sandstone and shale whose Dictyoconous sp. microfossils indicate late Jurassic to early Cretaceous age (Figure 4(a)). The plutonic rocks range from dioritic to monzodioritic in composition.

(a)

(b)

Figure 4: (a) Panorama photograph of the Chah Anjir intrusive unit, chilled margin and calcareous sandstone, and shale unit with Dictyoconous sp. fossil, (b) comparison between fresh and altered dolomitic marble.

The dolomitic-marble rocks appear white (fresh) to yellowish-brown (altered) in color due to the absence or presence of siderite, respectively (Figure 4(b)). The rocks are considered to be extensively replaced by magnetite and hematite. The rhythmic banding in dark altered and light colored fresh rocks is easily distinguished in the field.

Microscopic observations indicate several replacement textures due to alteration. These include widening of a fracture filling where a fracture crosses a chemically reactive rock (Figure 5(a)), irregular or vermicular intergrowths of hematite and calcite-dolomite (Figure 5(b)), remnant islands of nonreplaced host rock, rims of one mineral penetrating another along its crystallographic directions (Figure 5(c)), nonmatching walls or borders of a fracture, and cusp and caries textures (Figure 5(d)) [49].

(a)

(b)

(c)

(d)

Figure 5: Replacement textures in magnetite-hematite and host rock (all photomicrographs have been taken in transmitted light). (a) Widening of a fracture filling where the fracture crosses a chemically reactive rock, (b) irregular or vermicular intergrowths, (c) rims of one mineral penetrating another along its crystallographic direction, and (d) concave surface into the host or cusp and caries texture and remnant islands of the replaced host.

7. Alteration and Mineral Assemblages

Metasomatism accompanied by intrusions, and/or metamorphism, may be responsible for iron oxide mineralization in the Qatruyeh area. Microscopic observations and X-ray diffraction patterns on ore samples and metacarbonates have led to the recognition of two main alteration stages in the layered magnetite- and hematite-bearing ores (Table 2).

Table 2: Generalized paragenetic sequence in the Qatruyeh area.

Premetamorphic and syn-metamorphic
Postmetamorphic

Na-Ca alteration
Propylitic alteration
Oxidation

Massive magnetite
—

Layered magnetite

—
⋯

Hematite

⋯
—
—

Tourmaline

⋯

Titanite

—
⋯

Scapolite

—

Actinolite

—
⋯

Siderite

—

Paragonite

—

Epidote

—

Sericite

—

Chlorite

—

Quartz
⋯
⋯
—
⋯

Pyrite

⋯
⋯

Chalcopyrite

⋯
⋯

Calcite
—
⋯
⋯

Dolomite
—
⋯
⋯

Goethite

⋯

Limonite

⋯

Malachite

⋯

—Major phase, ⋯Minor phase.

The first stage of alteration includes Na-Ca metasomatism (actinolite + titanite + epidote + calcite + albite ± scapolite ± quartz), which is characteristic of diorite-monzodiorite plutonic rocks (Figure 6(a)). Epidote and actinolite replaced plagioclase; magnetite inclusions were found in some actinolites (Figure 6(b)). Magnetite, actinolite, tremolite, tourmaline, titanite, and quartz are the major minerals; pyrite and chalcopyrite occur as minor phases in the accompanying layered ore bodies (Figure 6(c)). Layered magnetite ores replaced dolomitic marble and the calc-silicate minerals that are typical of skarns are virtually absent from the ore zones [50]. Paragonite and siderite are exclusively identified within the halos of 1–3 m in diameter close to ore bodies that were only recorded at XRD data. Paragonite was formed during the early metasomatic stage. The same data records were observed in Lena Gold District, Siberia [51]. Siderite is produced by replacement of calcite or dolomite by an iron-rich solution [52] and paragonite is formed by solutions during regional metamorphism [51].

(a)

(b)

(c)

(d)

Figure 6: (a) Mineral assemblages of Na-Ca metasomatism in plutonic rocks. Albite + titanite + epidote + actinolite + calcite + magnetite (XPL), (b) magnetite mineralization is contemporaneous with the main phase of actinolitization (PPL), (c) chalcopyrite and pyrite as a late phase with magnetite (sulfides minerals include inclusion of magnetite) (RL), (d) a host-breccia (cataclastic texture), crashed calcite with hematite matrix (PPL). Mineral abbreviations: Act = actinolite, Alb = albite, Cal = calcite, Cal-Dol = calcite and dolomite, Ccp = chalcopyrite, Epi = epidote, Mt = magnetite, Py = pyrite, and Spn = sphene.

The second stage of alteration is shown by hematitization in brecciated metacarbonate (Figure 6(d)). Hydrothermal activity has produced a specific alteration around hematite ores, with a more regionally developed propylitic zone. This alteration style is very common in hematite ores and indicates the activity of a volatile-rich hydrothermal solution [6]. The alteration that is associated with oxidizing fluids often results in the formation of minerals with a high Fe³⁺/Fe²⁺ ratio and, in particular, hematite associated with sericite + quartz + epidote + chlorite ± magnetite [53]. Hematite + quartz ± pyrite ± chalcopyrite veins accompanied the late stage of each main ore mineralization in the Qatruyeh area.

8. Results

8.1. Geochemistry

In order to study the major, trace, and REE compositions of the Chah Anjir plutonic rocks, eleven samples were collected from surficial exposures. The emphasis during sampling was on fresh rocks, so as to avoid metasomatic changes during hydrothermal alteration.

Results of the whole rocks chemical analyses of major, trace, and REE in the Chah Anjir migmatite are summarized in Table 3. According to - discrimination diagram [26] and the classification diagram for plutonic rocks [28], the Chah Anjir intrusive rocks can be classified as diorite, monzodiorite (Figure 7(a)), and diorite to syenodiorite, respectively (Figure 7(b)), with subalkaline to alkaline affinity (Figure 8(a)). As indicated in Figure 8(b), the plutonic rocks plot within the calc-alkaline to tholeiitic fields. In order to determine the tectonic setting for the plutonic rocks and its relation to ore mineralization, Y − Nb and (Y + Nb)-Rb diagrams [30] were used. On the Y − Nb diagram, the samples plot in the volcanic arc to syn-collisional granite fields (Figure 8(c)). On the Rb-(Y + Nb) diagram the samples fall in the field of volcanic arc granitoids (Figure 8(d)). The tectonic setting is confirmed to geological characteristics of the Qatruyeh area.

Table 3: Results of whole rocks chemical analyses of major, trace, and rare earth elements in the Chah Anjir magmatic samples.

Field number
SiO₂
TiO₂
Al₂O₃
Fe₂O₃
MnO
MgO
CaO
Na₂O
K₂O
P₂O₅
Ba
Co
Cu
Hf
Mo
Nb
Rb
Y
Zn
Zr

CAP 1
57.00
0.90
16.82
6.90
0.20
3.50
5.50
4.40
1.76
0.10
61.00
32.00
38.00
3.00
0.40
8.60
2.50
18.20
46.20
177.00

CAP 2
57.00
0.91
16.40
7.10
0.30
3.60
6.20
4.20
1.61
0.10
76.00
25.00
24.00
1.70
0.33
6.40
2.20
15.40
36.10
138.00

CAP 3
56.90
0.95
17.70
6.60
0.37
4.00
6.40
3.80
1.50
0.10
59.00
40.00
21.00
1.60
1.20
4.80
3.70
13.50
64.80
102.00

CAP 4
55.00
1.10
17.67
7.50
0.40
4.50
6.50
3.10
1.30
0.10
55.00
50.00
19.00
1.10
0.90
4.00
1.60
11.10
33.80
93.00

CAP 5
57.00
0.90
16.90
6.80
0.30
4.10
6.10
3.50
2.10
0.10
65.00
35.00
34.00
2.70
0.33
5.60
3.20
14.20
56.20
156.00

CAP 6
55.90
1.30
17.20
7.30
0.20
4.00
6.80
3.20
2.50
0.10
60.00
30.00
28.00
2.50
1.00
7.50
2.70
12.70
44.30
112.00

CAP 7
56.00
1.10
16.10
7.00
0.37
3.00
6.10
4.30
1.61
0.10
385.00
37.10
15.00
4.50
1.50
12.80
143.50
21.70
72.00
156.00

CAP 8
55.60
1.40
16.70
6.60
0.10
3.50
6.40
4.10
1.20
0.10
411.00
44.50
10.00
4.50
1.50
11.20
160.00
30.10
72.00
160.00

CAP 9
57.00
0.95
16.60
7.20
0.30
4.00
6.00
3.70
1.40
0.10
302.00
75.20
12.00
6.10
1.50
13.80
136.50
27.50
74.00
212.00

CAP 10
56.30
1.10
16.90
6.80
0.30
4.10
6.10
4.20
2.10
0.10
384.00
44.00
15.00
6.10
1.50
14.80
116.50
28.40
93.00
219.00

CAP 11
57.80
0.88
16.23
6.50
0.22
3.30
5.40
4.54
2.90
0.34
168.00
22.00
98.00
8.80
1.33
11.30
59.70
34.30
131.00
229.70

CAP 12
57.40
0.80
16.56
6.60
0.22
3.40
5.70
4.90
2.80
0.39
158.00
28.00
113.00
7.23
1.00
10.40
22.30
29.20
159.00
221.30

D 25189
56.11
1.32
16.87
7.54
0.05
2.45
7.85
4.78
0.61
0.61
75.00
36.80
31.00
2.30
1.10
5.60
3.40
15.60
55.30
129.80

D 25213
60.23
0.91
16.43
2.84
0.09
3.32
9.38
5.68
0.33
0.05
69.50
45.10
17.50
2.30
1.30
8.92
12.50
12.63
32.80
111.30

D 25229
57.78
0.81
16.66
8.11
0.16
3.23
6.92
3.51
1.82
0.17
66.10
55.30
14.30
3.40
0.98
9.95
16.40
14.74
62.54
231.50

El Romeral
57.04
0.61
17.31
4.18
0.06
4.35
9.89
4.73
0.06
0.10
51.20
32.10
13.80
2.70
1.00
15.43
8.64
20.33
32.72
132.50

Field number
La
Ce
Pr
Nd
Sm
Eu
Gd
Tb
Dy
Ho
Er
Tm
Yb
Lu
REE
(La/Lu)N
(La/Sm)N
(Gd/Lu)N
[Eu]/[Eu*]
[Ce]/[Ce*]

CAP 7
32.60
68.20
7.32
26.50
5.38
1.14
5.55
0.83
4.17
0.88
2.30
0.32
2.10
0.31
157.60
10.51
3.47
2.34
0.64
0.97

CAP 8
31.20
65.90
7.10
25.40
5.43
1.05
5.91
0.97
5.30
1.07
3.06
0.44
2.79
0.43
156.05
7.259
3.29
1.79
0.57
0.98

CAP 9
34.80
73.80
8.03
29.10
5.85
1.08
6.32
0.98
5.05
0.97
2.71
0.39
2.48
0.39
171.95
8.92
3.41
2.12
0.55
0.98

CAP 10
39.30
82.20
8.57
31.10
5.89
1.21
6.22
0.95
5.11
1.07
3.12
0.44
2.90
0.47
188.55
8.546
3.82
1.77
0.62
0.99

Note: CAP 1 to CAP 12 = Chah Anjir magmatic samples and D. 25189, D. 23213, D. 25229, and El Romeral = data of Andean calc-alkaline plutonic rocks related to iron oxide deposits [1, 50]. Major elements are in wt.% and trace elements are in ppm.

(a)

(b)

Figure 7: (a) The classification of plutonic rocks using the parameters - [26]. Parameters are defined by the = [4Si − 11(Na + K) − 2(Fe + Ti)] and = (Al + 2Mg + 6Ca) and (b) the chemical classification of plutonic rocks using total alkaline versus SiO₂ from [27] and modified by [28]. The analyzed samples were present as black circles.

(a)

(b)

(c)

(d)

Figure 8: (a) alkali-silica diagram for determining subalkaline and alkaline fields [29], (b) AFM diagram for determining submagma type (tholeiitic or calc-alkaline), (c) and (d) position of the Chah Anjir samples on Y versus Nb and Rb versus Y + Nb diagrams [30]. Abbreviations: AFM = alkaline components (Na₂O + K₂O)-FeOtotal-MgO, ORG = ocean ridge granites, Syn-COLG = syn-collision granites, VAG + Syn-COLG = volcanic arc granites + syn-collision granites, and VAG = volcanic arc granites. The analyzed samples were presents as black circles.

In the A-B diagram of [31], the samples show a negative slope in IV sectors of metaaluminous area that is such a trend characteristic of cafemic (CAFEM) rocks due to presence of hornblende, ortho- and clinopyroxene, biotite, epidote, and titanite in origin (Figure 9(a)). According to the A/CNK <1.1 ratio [54] and Zn versus SiO₂ diagrams (Figure 9(b)) [32] and SiO₂-Fe₂O₃/FeO diagram [33] the Qatruyeh plutonic rocks are considered I-type and magnetite series granitoids (Figure 9(c)). These results associated with those of the intrusions fall in the hydrothermal iron deposits field.

(a)

(b)

(c)

(d)

Figure 9: (a) Distribution of the Chah Anjir samples on A-B diagram (A = Al − (K + Na + 2Ca) and B = Fe + Mg + Ti) [31], (b) separation of I-type and A-type magma series according to Zn-SiO₂ Diagrams [32], (c) SiO₂-Fe₂O₃/FeO variation diagram showing fields for magnetite series and ilmenite series granites and intrusive rocks associated with hydrothermal iron deposits [33], (d) Chondrite-normalized REE distribution pattern of the Qatruyeh samples (Chah Anjir intrusive rocks, layered magnetite ores, massive magnetite ores, and hematite ores). Abbreviations: peraluminous (I = muscovite or muscovite > biotite, II = biotite > muscovite, and III = biotite) and metaluminous (IV = mainly hornblende and biotite + orthopyroxene + clinopyroxene + epidote + titanite, V = clinopyroxene ± epidote ± titanite, and VI = exceptional igneous rocks (e.g., carbonatite).

REEs from the samples were normalized to chondrites using the values of Wakita et al. [55]. Enrichment coefficients of La (), La (), Gd (), and [Eu]/[Eu*] as Eu anomaly were examined. The results indicate that the Chah Anjir intrusive rocks were enriched in light rare earth elements (LREEs) compared to heavy rare earth elements (HREEs) (Figure 9(d)). Moderate to negative Eu anomalies, high total REE contents ( with average of 168), and high LREE/HREE ratios () are also observed. These evidences suggest continental or continental-margin geological settings for the intrusive rocks in the Qatruyeh area. The negative Eu anomalies can be explained by the abundance of plagioclase feldspar in the melt. As proposed by Henderson [56], small amounts of garnet, amphibole, or pyroxene can reduce the HREE relative to LREE in the melt.

As mentioned, iron ores could be divided into high-grade magnetite ores (consisting of massive magnetite with minor silicate minerals) and low-grade magnetite ores (layered magnetite with silicate minerals) and hematite ores. The major, trace, and rare earth elements of the Qatruyeh iron oxide ores are presented in Table 4. The high-grade magnetite ores typically have high contents of TiO₂ (0.09 to 1.08 wt.%), whereas the low-grade ores indicate the high amounts Na₂O + K₂O (avg. 1.08 wt.%) and CaO (avg. 3.8 wt.%).

Table 4: Chemical compositions of Qatruyeh iron oxides.

(a)

Field number
SiO₂
TiO₂
MnO
P₂O₅
Al₂O₃
Fe₂O₃
MgO
CaO
Na₂O
K₂O
L.O.I
Ba
Co
Cr
Cs
Cu
F
Cl

H1
37.00
0.03
0.14
0.18
0.49
55.00
0.52
0.12
0.02
0.98
3.67
9.57
68.30
55.31
2.96
0.45
33.00
21.00

H2
48.00
0.02
0.31
0.18
0.38
45.60
0.52
0.24
0.04
0.85
3.20
11.14
51.92
23.95
7.72
8.95
24.00
14.00

H3
48.00
0.02
0.80
0.13
0.38
43.30
0.14
0.66
0.11
0.92
3.90
117.37
69.44
35.96
0.08
13.22
42.00
5.00

MM1
5.00
0.09
0.32
0.10
0.52
88.30
0.80
0.71
0.13
0.24
1.20
19.52
114.00
207.00
4.90
50.00
55.00
78.00

MM2
23.00
0.11
0.16
0.20
1.00
70.70
0.35
0.18
0.12
0.22
2.42
15.19
142.00
334.00
7.63
12.00
42.00
55.00

MM3
14.00
0.23
0.33
0.30
0.50
75.99
0.39
0.35
0.15
0.22
3.60
34.60
133.00
237.00
4.92
17.00
11.00
4.00

MM4
8.00
0.17
0.04
0.20
0.20
86.00
0.60
0.48
0.14
0.28
1.67
51.98
107.00
233.00
7.72
13.00
24.00
19.00

MM5
26.00
1.08
0.10
0.20
3.25
63.10
0.42
2.54
0.19
0.43
0.96
208.67
63.49
52.59
9.01
29.55
25.00
2.00

MM6
15.00
0.20
0.41
0.10
0.10
75.50
0.80
0.90
0.13
0.39
3.99
5.70
122.00
7.50
0.03
23.00
37.00
19.00

MM7
12.20
0.30
0.50
0.10
0.20
82.80
0.30
0.18
0.11
0.32
2.40
8.00
94.20
7.50
0.04
43.00
nd
nd

MM8
8.00
0.10
0.32
0.30
0.40
86.70
0.39
0.50
0.15
0.22
2.50
353.00
103.00
7.50
0.04
37.00
37.00
19.00

LM1
42.00
0.06
0.68
0.34
2.50
41.40
0.24
4.85
0.44
0.74
5.30
405.30
48.27
298.00
1.76
373.40
72.00
252.00

LM2
44.00
0.04
0.73
0.32
2.10
40.40
0.74
4.18
0.39
0.37
5.76
81.83
42.00
280.00
1.52
110.20
38.00
226.00

LM3
38.00
0.06
0.77
0.26
1.39
50.10
0.42
2.92
0.31
0.37
4.66
49.68
59.00
344.00
3.08
295.30
53.00
311.00

LM4
21.00
0.08
0.53
0.11
1.30
60.20
0.63
5.51
0.50
0.79
4.30
203.12
78.00
317.00
1.24
273.00
24.00
221.00

LM5
17.00
0.08
0.58
0.40
1.50
65.99
1.40
7.60
0.55
0.63
3.25
65.90
67.00
442.00
2.33
363.00
17.00
334.00

LM6
29.00
0.08
0.60
0.30
1.80
53.00
0.99
4.60
0.47
0.73
5.66
88.89
59.63
359.59
1.18
232.00
24.00
286.00

LM7
38.00
0.08
0.05
0.33
2.20
48.99
1.20
0.24
0.64
0.59
5.40
54.97
50.38
355.91
1.98
79.00
2.00
153.00

LM8
32.00
0.08
0.95
0.29
1.50
54.99
0.64
0.86
0.49
0.60
4.45
254.20
64.00
357.63
2.12
121.00
21.00
342.00

LM9
42.30
0.05
0.73
0.40
2.30
43.40
0.54
2.60
0.59
0.62
4.23
357.00
93.80
420.00
1.24
343.00
14.00
278.00

LM10
41.20
0.08
0.76
0.39
1.24
44.40
0.40
3.21
0.57
0.79
3.98
63.30
83.20
477.50
2.33
84.00
32.00
359.00

LM11
37.30
0.07
0.55
0.32
1.52
49.10
0.52
5.24
0.69
0.69
3.21
37.30
88.20
497.50
1.18
244.00
48.00
169.00

(b)

Field number
La
Ce
Pr
Nd
Sm
Eu
Gd
Tb
Dy
Ho
Er
Tm
Yb
Lu
REE
(La/Lu)N
(La/Sm)N
(Gd/Lu)N
[Eu]/[Eu*]
[Ce]/[Ce*]

H1
1.13
0.90
0.73
0.70
0.15
0.08
0.05
0.03
1.03
0.01
0.03
0.01
0.06
0.01
4.91
11.29
4.31
0.65
2.85
0.22

H2
1.12
0.77
0.99
0.74
0.08
0.09
0.09
0.05
0.38
0.01
0.04
0.01
0.03
0.01
4.39
11.19
8.02
1.17
3.27
0.16

H3
1.22
0.82
0.83
0.94
0.08
0.08
0.06
0.04
1.05
0.02
0.03
0.04
0.06
0.01
5.27
12.27
8.75
0.78
3.56
0.18

MM1
0.92
0.33
0.21
0.40
0.24
0.03
0.73
0.08
0.72
0.07
0.3
0.04
0.4
0.04
4.51
2.29
2.19
2.38
0.22
0.16

MM6
0.48
0.52
0.14
0.38
0.15
0.02
0.98
0.12
0.50
0.05
0.4
0.07
0.23
0.03
3.99
1.63
1.83
4.26
0.16
0.44

MM7
0.64
0.40
0.07
0.30
0.13
0.05
0.56
0.08
0.50
0.09
0.3
0.05
0.30
0.02
3.48
3.25
2.82
3.66
0.57
0.42

MM8
0.74
0.90
0.07
0.40
0.18
0.02
0.92
0.07
0.80
0.04
0.4
0.04
0.32
0.03
4.93
2.46
2.36
4.01
0.15
0.88

LM1
12.00
12.69
0.99
2.46
2.10
0.12
2.80
nd
nd
0.20
1.64
nd
0.66
0.22
35.88
5.45
3.28
1.66
0.15
0.82

LM2
10.88
20.93
1.20
2.87
1.64
0.08
2.03
nd
nd
0.22
1.48
nd
0.67
0.15
42.15
7.25
3.80
1.76
0.13
1.28

LM3
11.85
16.30
1.00
5.94
1.28
0.50
2.09
nd
nd
0.10
2.68
nd
0.62
0.29
42.64
4.09
5.31
0.94
0.94
1.05

LM9
10.20
19.40
2.42
9.60
1.95
0.51
2.04
0.35
0.92
0.31
1.71
0.12
0.75
0.12
50.40
8.49
3.84
2.22
0.78
0.87

LM10
6.00
9.50
1.00
3.90
0.88
0.17
1.02
0.20
0.55
0.17
0.80
0.06
0.64
0.09
24.98
6.68
3.91
1.48
0.55
0.86

LM11
5.10
6.30
0.79
3.10
0.65
0.11
0.95
0.19
0.51
0.16
0.89
0.04
0.40
0.08
19.27
6.38
4.50
1.55
0.43
0.69

(c)

Field number
Hf
Nb
Ni
Pb
Rb
S
Sb
Sc
Sr
Ta
Th
U
V
Y
Zn
Zr

H1
21.24
3.59
138.51
114.82
0.60
390.82
0.32
1.54
11.01
24.13
258.81
84.67
11.78
0.75
177.78
775.35

H2
20.48
3.08
121.90
73.94
0.60
25.68
0.28
1.15
13.71
19.15
211.91
89.50
3.71
1.88
172.49
686.05

H3
14.48
0.75
77.04
99.04
0.60
173.58
0.68
0.60
33.43
18.19
210.53
85.97
6.75
0.73
413.49
560.11

MM1
1.37
0.79
61.00
12.00
1.83
0.32
0.42
2.16
64.00
21.41
198.86
0.30
73.02
0.68
128.00
986.23

MM2
2.15
2.34
84.00
18.00
0.20
0.12
0.37
0.30
11.00
10.18
209.32
1.55
15.60
0.78
272.00
867.12

MM3
0.20
8.34
62.00
14.00
0.25
nd
0.48
0.64
24.00
17.86
111.24
3.83
13.65
0.33
147.00
457.27

MM4
0.22
33.50
29.00
15.00
0.87
nd
0.65
0.23
13.00
22.40
98.65
77.30
14.23
1.23
102.00
772.54

MM5
21.37
48.39
59.66
94.01
11.68
0.75
0.67
13.12
49.21
27.18
289.44
115.95
93.90
32.41
188.90
1050.08

MM6
0.15
0.15
33.75
6.00
0.20
Nd
Nd
4.76
12.90
0.08
0.65
0.30
14.00
0.60
75.00
952.16

MM7
0.15
0.15
45.50
3.75
0.15
0.72
Nd
7.93
16.20
0.08
0.38
4.75
3.75
0.80
157.00
793.45

MM8
0.15
0.15
39.00
30.00
0.30
0.98
Nd
0.32
43.80
0.08
0.19
2.23
23.00
5.20
36.00
568.87

LM1
18.45
0.75
80.00
320.57
26.29
53.51
1.01
5.12
82.00
18.39
190.10
61.40
23.68
6.33
115.00
645.96

LM2
17.41
0.75
69.00
85.00
12.60
0.75
0.77
2.16
46.00
16.95
186.50
58.80
18.28
4.45
111.00
613.99

LM3
18.69
7.48
85.00
166.63
9.01
89.34
0.52
6.35
52.00
19.75
231.00
83.40
29.59
11.90
139.00
700.41

LM4
0.19
2.80
185.47
102.00
14.50
23.06
1.93
5.59
134.78
28.29
290.12
55.40
43.69
12.44
1184.32
634.54

LM5
0.17
3.51
190.00
8.00
13.80
435.00
1.71
3.18
94.18
26.53
196.50
63.10
48.28
15.23
1967.77
45.65

LM6
0.15
0.40
103.76
Nd
25.90
39.34
1.03
8.37
63.07
28.76
132.39
52.43
28.54
4.18
1988.46
423.44

LM7
1.46
0.43
96.55
62.00
18.54
0.87
0.98
6.43
31.00
1.43
11.53
4.44
33.98
3.53
138.00
162.86

LM8
0.65
0.26
89.00
13.00
12.57
23.84
0.84
3.52
11.00
2.87
84.96
12.83
21.60
7.98
147.00
235.73

LM9
0.80
1.80
79.00
309.00
24.50
12.43
1.01
8.32
132.00
0.20
2.09
3.06
76.00
11.40
3040.00
31.00

LM10
0.40
0.50
53.75
32.00
9.90
10.32
0.75
4.23
90.80
0.08
1.12
2.48
27.00
5.30
1430.00
17.00

LM11
0.20
0.30
63.75
86.00
15.90
1.28
nd
Nd
61.50
0.08
0.91
2.96
27.00
5.80
880.00
11.00

Note: H1 to H3 = hematite ores, MM1 to MM8 = massive magnetite ores, and LM1 to LM11 = layered magnetite ores. Major elements are in wt.% and trace elements are in ppm (“nd” = not detected).

Enrichment of sulfur in the layered magnetite is reflected by the presence of sulfides such as pyrite and chalcopyrite. There are strong positive correlations among Fe₂O₃, TiO₂ and HFSEs (Hf, Sc, Th, U, Nb, and Zr), LREEs, and transition metals (Cr, Co, and Ni) in layered magnetite. In contrast, the strong negative correlations between the two oxides with HREEs and LILEs (Ba, K, and Rb) indicate that layered magnetite acts as a scavenger for HFSEs, LREEs, and intermediate elements (Figure 10). It was inferred that the relationship was due to the similarity of the behavior of those elements in spinel group minerals.

Figure 10: Major and trace element correlation coefficient for massive and layered magnetite ores.

The positive correlation between LREEs and Al₂O₃, CaO, Na₂O, and MgO indicate that the LREEs are collected in the silicate phases in the ore bodies.

High values of chalcophile elements (Hg, Bi, Cu, and Ag) were observed in layered magnetite as a below-ore halo and deep-seated iron mineralization.

The REE distribution patterns in high-grade massive magnetite and low-grade layered magnetite ores are very different (Figure 9(d)). These patterns can show differential origins of both ore bodies. An average ratio of 6.3 in the layered ores indicates a high degree of fractionation. A weak negative Eu anomaly and LREE enrichment are observed in the layered magnetite. In contrast, high-grade ores are depleted in LREE, enriched in HREE, and display a strong negative Eu anomaly. The depleted LREE pattern is interpreted as high-temperature leaching of LREE or the occurrence of a lower temperature metamorphism [57]. It is suggested that Ce depletion in high-grade magnetite may be the result of a late stage metasomatic alteration in the Qatruyeh area. This indicates that the two ore occurrences, layered and massive, are different in origin.

The bulk compositions of the altered and fresh metacarbonates are given in Table 5. Altered rocks are depleted in CaO and MgO relative to fresh metacarbonate samples whereas the Fe₂O₃, Al₂O₃, K₂O, and Na₂O contents increased in the rocks during metasomatic alteration. An increase in the K₂O and Al₂O₃ contents is the result of muscovite abundance in the altered rocks. TiO₂, Ba, Rb, Cr, and V can also be present within muscovite. The difference in the position of data points of altered and fresh rocks is explained in Figure 11.

Table 5: The bulk compositions of the altered and fresh metacarbonates of Qatruyeh area.

(a)

Field number
SiO₂
TiO₂
Al₂O₃
Fe₂O₃
MnO
MgO
CaO
Na₂O
K₂O
P₂O₅
L.O.I
Ba
Ce
Cr
Cs
Cu
Dy
Eu
Ga

FM 1
17.00
0.01
0.38
0.32
0.02
3.70
34.55
1.55
0.13
0.03
41.00
921.10
2.60
27.80
12.66
0.45
0.30
0.08
2.27

FM 2
19.00
0.01
0.40
0.29
0.14
3.40
38.00
2.20
0.14
0.04
35.00
823.40
nd
88.00
14.34
10.00
nd
nd
1.34

FM 3
14.00
0.01
0.30
0.32
0.09
3.80
37.00
1.30
0.13
0.02
42.00
762.51
nd
92.00
10.27
4.00
nd
nd
2.51

FM 4
20.00
0.01
0.50
0.43
0.07
5.40
32.00
2.10
0.16
0.02
38.00
973.55
nd
123.00
13.18
5.00
nd
nd
0.98

FM 5
24.50
0.01
0.44
1.23
0.08
4.23
39.40
1.44
0.12
0.01
29.00
812.10
2.59
7.50
10.00
3.75
0.20
0.06
0.80

AM 1
26.00
0.01
1.60
9.50
0.18
6.00
19.54
0.85
0.80
0.12
33.00
24.40
85.30
59.81
0.15
767.00
8.51
0.43
6.45

AM 2
22.00
0.01
1.70
15.50
0.97
1.40
25.00
2.30
0.70
0.13
29.00
33.21
nd
67.00
0.23
507.00
nd
nd
14.63

AM 3
31.00
0.01
1.90
10.00
0.23
2.00
17.54
0.70
0.90
0.12
35.00
25.67
nd
371.00
0.14
7.00
nd
nd
15.32

AM 4
27.00
0.05
2.64
14.00
0.31
1.67
16.67
0.83
1.10
0.14
35.00
54.50
nd
381.00
0.34
525.00
nd
nd
25.27

AM 5
15.00
0.01
0.48
33.26
1.25
0.83
18.25
2.50
0.05
0.13
30.00
16.46
203.72
44.64
0.07
739.60
2.55
0.32
13.65

AM 6
9.00
0.06
1.20
35.02
1.10
1.00
18.41
2.80
0.46
0.17
31.00
19.40
258.22
158.00
0.08
780.00
39.79
0.44
24.33

AM 7
19.00
0.06
0.53
8.92
0.10
17.27
13.00
2.50
0.13
0.19
38.00
25.21
nd
67.25
1.24
137.00
nd
nd
1.98

AM 8
16.00
0.02
0.90
12.60
0.21
1.70
23.80
3.00
0.50
0.14
41.00
44.82
nd
363.00
1.05
192.00
nd
nd
3.42

AM 9
18.50
0.03
1.75
14.65
0.45
1.84
21.24
1.43
0.42
0.12
38.00
53.14
4.90
50.00
3.70
267.55
0.53
0.13
1.20

AM 10
17.32
0.04
0.99
12.54
0.78
2.26
17.25
1.50
0.65
0.10
40.00
42.20
2.80
10.00
3.52
3.75
0.49
0.10
1.60

AM 11
14.65
0.01
0.87
19.35
0.29
1.92
18.51
2.65
0.73
0.13
39.00
723.62
4.20
7.50
5.75
1.76
0.33
0.13
1.00

(b)

Field number
Hf
La
Lu
Nb
Nd
Ni
Pb
Pr
Rb
Sc
Sm
Sr
Ta
Th
U
Y
Yb
Zn
Zr

FM 1
0.15
1.24
nd
0.25
1.71
46.12
27.25
nd
0.61
1.34
0.24
950.21
0.03
0.70
0.08
2.12
0.10
56.00
1.35

FM 2
0.10
nd
nd
0.32
nd
17.00
105.00
nd
0.32
1.25
nd
444.00
0.01
0.52
0.09
1.84
nd
81.00
2.34

FM 3
1.43
nd
nd
0.29
nd
15.00
134.00
nd
0.55
0.99
nd
615.00
0.04
0.42
4.32
3.25
nd
25.00
0.86

FM 4
0.42
nd
nd
0.35
nd
19.00
231.00
nd
1.23
1.63
nd
126.00
0.10
0.79
0.98
1.94
nd
34.00
1.58

FM 5
0.15
1.70
0.02
0.40
1.00
3.75
6.00
0.32
2.90
0.74
0.29
763.00
0.07
0.28
0.17
1.40
0.10
14.00
2.00

AM 1
6.74
32.20
nd
0.75
12.56
57.76
40.92
nd
1.50
0.60
4.19
168.07
3.71
37.30
12.55
6.90
8.58
158.29
158.40

AM 2
16.53
nd
nd
15.56
nd
26.00
17.00
nd
11.34
2.56
nd
266.00
0.12
129.40
63.45
5.63
nd
168.00
227.40

AM 3
15.36
nd
nd
18.43
nd
22.00
11.00
nd
18.21
3.84
nd
118.00
1.43
192.50
98.45
8.28
nd
169.00
3.52.71

AM 4
17.27
nd
nd
11.34
nd
37.00
1.00
nd
0.98
nd
nd
101.00
2.76
48.70
44.61
2.73
nd
144.00
121.52

AM 5
8.71
35.18
nd
9.41
22.38
59.02
76.42
nd
0.60
2.00
7.47
170.00
13.31
147.35
51.32
4.76
8.33
180.86
396.37

AM 6
14.02
39.74
nd
18.42
25.38
109.08
150.80
nd
0.60
2.52
8.56
139.00
14.58
152.64
52.06
18.74
8.37
1266.51
490.00

AM 7
1.43
nd
nd
3.23
nd
49.00
87.00
nd
2.32
1.48
nd
61.00
2.51
6.67
3.67
1.32
nd
59.00
7.93

AM 8
2.78
nd
nd
2.65
nd
67.00
55.00
nd
4.54
2.53
nd
163.00
1.73
3.50
5.59
0.99
nd
103.00
19.47

AM 9
0.15
3.30
0.04
0.70
2.40
14.00
13.00
0.61
1.50
2.32
0.54
173.00
0.10
0.51
0.69
2.80
0.25
113.00
4.00

AM 10
0.15
2.10
0.03
0.30
1.30
3.75
14.00
0.35
3.10
1.65
0.30
267.91
0.08
0.35
2.51
3.60
0.17
135.00
5.00

AM 11
0.15
3.00
0.03
0.15
2.40
3.75
33.00
0.60
14.27
2.01
0.51
361.00
0.08
0.27
1.74
3.90
0.19
205.00
3.00

FM1 to FM5 = fresh dolomitic marbles and AM1 to AM11 = altered dolomitic marbles. Major elements are in wt.% and trace elements are in ppm (“nd” = not detected).

Figure 11: Plot of minor elements (Ba + Rb + Cr + V) versus major elements (Al₂O₃ + K₂O + TiO₂) in altered and fresh dolomitic marbles at the Qatruyeh area.

High MnO and Fe₂O₃ values in altered dolomitic marbles indicate that Fe and Mn replace Mg in dolomite lattice. In order to evaluate the compositional change which accompanies hydrothermal alteration, the concentrations of elements of interest are compared to those of immobile elements such as Zirconium. Typically, Zr is used as immobile and incompatible element during hydrothermal alteration due to the very high ionic radius [58]. In the case of chemically incompatible elements, the regression lines REEs and HFSEs which are considered to be immobile with each other in the Qatruyeh altered dolomitic marbles (Figures 12(a)–12(d)). The REEs are less well correlated with the above HFSEs and the regression lines shift from the origin, which suggests that the REEs were somewhat mobile during alteration. The interelement correlation among the REEs is significant (generally with coefficients higher than 0.7), which is consistent with their similar geochemical behavior. However, the interelement correlation among LREEs and HREEs treated separately is considerably stronger, which indicates fractionation between the two subgroups. LILEs (Ba, Sr, Rb, and Cs) are more mobile relative to Zr during hydrothermal alteration as shown by their poor correlations in Figures 12(e) and 12(f).

(a)

(b)

(c)

(d)

(e)

(f)

Figure 12: Binary trace element plots for dolomitic-marble samples of the Qatruyeh area. (a) and (b) high field strength elements (Ta and Hf), (c) and (d) rare earth elements (Yb and Sm), and (e) and (f) large ion lithophile elements (Sr and Sc).

8.2. Fluid Inclusions Study

Microthermometric measurements were made using a Linkam THMSG600 combined heating and freezing stage with a temperature range of −196 to +600°C and a reproducibility of ±0.1°C, at the fluid research laboratory at the Geological Survey of Iran by optical microscopy and microthermometry, attached to an Olympus petrographic microscope with LinkSys software (version 1.83). Ten doubly polished quartz wafers were prepared using the procedure of Shepherd et al. [59]. The thickness of the wafers varied between 150 and 300 μm, depending upon the transparency of the quartz crystals. Sample selection was biased to quartz containing an abundance of Na-Ca minerals in low-grade magnetite type. The fluid inclusions have a variety of shapes (mainly rounded, elongate, or square and, less commonly, irregular) and typically are of low to medium size (5 to 50 μm). Quartz in the samples contains inclusions >10 μm which allows for more confident thermometric analysis. Based on petrographic and microthermometric studies and present phases at temperature room, inclusions are divided into the following types (Figures 13(a)–13(d)).

Figure 13: Photomicrographs of different fluid inclusions in quartz from layered magnetite at the Qatruyeh (crossed nicols). (a) Fluid inclusions with two-phase liquid + vapor (type A), (b) fluid inclusions with three-phase vapor + liquid (L₁) + CO₂ liquid (L₂) (type B), (c) fluid inclusions with monophase liquid (type C), and (d) fluid inclusions with monophase vapor (type D).

(1) Two-phase liquid + vapor (type A), (2) three-phase vapor + liquid () + CO₂ liquid (L₂) (type B), (3) monophase liquid (type C), and (4) monophase vapor (type D). Types A and B constitute the majority of fluid inclusions in the Qatruyeh quartz veins (proximal to the Chah Anjir intrusive unit) and account for 80% of the inclusion population and were chosen for microthermometric studies for two important reasons: (1) the inclusions are mostly intimately associated with layered magnetite mineralization, (2) these types contain inclusions >5 μm which allows for more confident thermometric analysis. In addition, primary fluid inclusions, with no evidence of necking down, were selected for microthermometric analyses.

Type A inclusions are dominated by more than 80 vol.% of H₂O at room temperature. These inclusions occur in a variety of forms: in growth zones, small clusters, and as dispersed arrays. Measurements on trapped phases were not attempted. The first ice temperature of melting () often occurs around −24.5 to −19.5°C, corresponding to stable eutectic melting in the NaCl-MgCl₂-CaCl₂-H₂O system (Figure 14(a)). Salinities determined by last ice temperature of melting () were 3.5 to 15 wt.% NaCl equivalent (size of inclusions between 10 and 30 μm) for inclusions trapped in whole quartz samples (Figure 14(b)). The homogenization temperature () values change between 280 and 385°C (Figure 14(c)) and Tm measurements range from −11.3 to −3.5°C (Figure 14(d)). Homogenization temperature existing for primary types (A) of fluid inclusion may indicate episodes of hydrothermal activities in mesothermal systems for Fe deposits in this region.

(a)

(b)

(c)

(d)

Figure 14: Fluid inclusion data plotted in histograms. (a) Distribution of first ice-melting temperatures or eutectic temperatures (), (b) frequency distribution of salinity based on weight percent NaCl equivalent (wt. %NaCl equivalent), (c) distribution of homogenization temperatures (), and (d) distribution of last ice-melting temperatures ().

Type B inclusions, characterized by much more gas bubble within an aqueous liquid, are commonly found in all selected samples. The inclusions are dominated by more than 45 vol.% H₂O-CO₂ at room temperature. Carbonic liquid is a visible phase as immiscible solution within H₂O liquid. But, vapor bubbles of the inclusions do not contain enough CO₂ to form clathrate or a visible phase of liquid CO₂ during cooling. This suggests that the CO₂ content of the bubble is less than 0.85 mol.% [60]. of type B fluid inclusions (Figure 14(a)) is in the range of −39.5 to −37.6°C. The first ice melting temperatures indicate that the mineralizing fluid contained a complex mixture of metal chlorides, particularly NaCl-MgCl₂-CaCl₂-FeCl₂. In this type, liquid-CO₂ homogenizes to vapor in the temperature range 396 to 410°C (Figure 14(c)). A general increase in values is observed for type B inclusions in comparison to type A. Values of of type B inclusions fall within a narrow range from −2.4 to −1.8°C (Figure 14(d)) corresponding to low salinity, between 3.9 and 2.9 wt.% NaCl equivalent. These fluids consist of mixtures of H₂O and CO₂, the most common fluids released during metamorphic reactions [61].

9. Discussion

These deposits have a number of distinct features [15, 18–20, 62]: (1) an epigenetic origin, formed at moderate to high temperatures (200°–350°C), (2) volcanic, sedimentary, and metamorphosed host rocks, (3) widespread alkali-rich alteration halos, (4) the presence of hydrothermal-metasomatic magnetite and/or hematite ores, (5) a common association with calc-alkaline, I-type granitoid, (6) the presence of deep seated hydrothermal replacement and shallower brecciated textures, and (7) hydrothermal fluids with low to high salinity and CO₂ and other gaseous components and also chloride complexes for iron mobilization. This indicates that no single genetic model can be developed for hydrothermal Fe-oxide deposits [17, 18, 22–25, 63, 64].

There are some similarities between the Qatruyeh iron ores and hydrothermal Fe-oxide deposits such as Andean iron oxide and Iron springs Utah deposits [15, 18]; these are (1) occurrence of ore bodies along a subduction-related active continental margin, (2) abundances of magnetite with lesser hematite, (3) the presence of breccia and replacement textures, (4) iron oxides with low Ti contents, (5) uranium anomalies, and (6) chemical analyses results of magmatic rock samples of the Qatruyeh similar to those of calc-alkaline plutonic rocks in Andean iron belt (Table 1). At the Qatruyeh area, titanium in both types of magnetite ores was depleted like to other hydrothermal iron deposits. It was concentrated in early magmatic ferromagnesian minerals in mafic rocks and hence was depleted in the residual late magmatic hydrothermal fluids. Layered magnetite and hematite ores related to massive magnetite in the Qatruyeh area generally have anomalous, though uneconomic, uranium grades. The relatively high values of uranium could be related to uranium-rich magmatic fluids from causative intrusions, particularly magnetite-series intrusions such as the Chah Anjir plutonic rocks at the Qatruyeh area. Alternatively, uranium could be contributed by a second fluid mixing with hydrothermal fluids at the site of mineralization or it may have been leached from host rocks [65]. The hydrothermal systems within intermediate to mafic calc-alkaline sequences, such as the subduction-related deposits of the Andean iron belt, would be expected to have low uranium contents. Therefore, uranium-rich iron oxide systems with relatively low copper values (e.g., the Qatruyeh area) suggest the presence of iron oxide uranium deposits and may be important exploration targets [65]. On this basis, the intermediate intrusions would be considered as a potential source of mineralizing components for the iron ore deposits.

HFSEs were immobile in the metacarbonate rocks, whereas large-ion lithophile elements were mobile during hydrothermal alteration and associated iron mineralization.

According to major oxide analyses of magnetite, the high Na₂O content in magnetite is called alkali iron effect [15] and the system, such as FeO + Na₂O + K₂O + Al₂O₃ + MgO and FeO + MnO + TiO₂ + CaO + P₂O₅ + SiO₂, kept iron in solution at temperatures significantly lower than the melting point of magnetite at rather shallow depth [66]. The role of other volatile constituents such as CO₂ and F is also important in this process [67]. The PCO₂ at the Qatruyeh may have been raised by the assimilation of dolomitic-marble host rock by iron-rich hydrothermal fluids, as is evidenced by the presence of carbonate xenoliths in the magnetite ore.

The REE distribution in hydrothermal minerals is often used for discussing ore genesis. It is influenced by chemical-crystallographical constraints, kinetics of crystallization, - conditions, and the composition of the hydrothermal fluids [68]. In addition, it is necessary to take into account the effect of subsequent metamorphism and hydrothermal alteration when using REE data in ore genetic discussions. REEs geochemical investigations on the metacarbonate host rocks were shown that these elements were moderately mobilized due to metasomatic-alteration in the study area. Alderton et al. [69] stated that REE mobilization in fluids is controlled largely by (1) the REE concentrations of the reacting minerals; (2) the relative stability of these minerals against the fluid; (3) the availability of suitable crystallographic sites within the secondary minerals to accommodate released REE during alteration; (4) the REE concentrations of the hydrothermal fluid; and (5) the ability of the fluid phase to remove REE from the system.

Besides, the REE patterns for magnetite, as well as their geochemical character, show a clear difference between the high-grade and low-grade ores. The similarity of REE patterns in the layered magnetite ores and magmatic rocks is consistent with this conclusion that the layered magnetite was formed from magmatic derived hydrothermal fluids. On the contrary, different REE distribution patterns in massive magnetite indicate that these ores formed by dissimilar agents and processes at different times (e.g., by metamorphic fluids derived from dehydration and decarbonation reactions during prograde metamorphism). The metamorphic grade of the Qatruyeh area has been determined to epidote-amphibolite facies, which according to Apted and Liou [70] took place between 575 and 675°C (at 7 kb) and could consequently have produced hot fluids enough for magnetite mineralization. Also, Magnetite is not normally a major REE-bearing mineral; due to the small ionic radius of Fe therefore it has a very little influence on the REE budget in the hydrous systems. In contrast, the silicate partition coefficients for the REE are highest in such systems [71]. LREEs enrichment in low-grade ores is opposite to what one should expect based on the small ionic radius of the iron site. Schock [72] cited analyses of magnetite contained Ca²⁺ ions in its structure. He further noted the plausibility that REE ions with comparable ionic radii to Ca²⁺ (7- and 9-fold coordination with ionic radii of 1.06 and 1.18 Å, resp.) could also enter the same lattice sites. Frietsch and Predhal [73] according to de Sitter et al. [74] have showed substitution of Ca²⁺ ions for ferrous ion in the magnetite structure, which can contain up to 6.67 wt.% Ca²⁺, corresponding to the composition (Fe2.8Ca0.2)O₄. The large ionic radius of Eu²⁺ (7- and 9-fold coordination with ionic radii of 1.20 and 1.30 Å, resp.) discriminates against, is in contradiction to incorporation into the magnetite. Accordingly, the negative Eu anomaly in low-grade magnetite indicates Eu enrichment in the remaining hydrothermal fluids after iron ore formation. Divalent Eu will thus be stable over a wide range of pH values at the magnetite-hematite buffer and moderate to high temperature hydrothermal systems, due to its large ionic radius. But, trivalent Eu will become the stable species when the system cools or becomes extremely oxidized [75]. The positive Eu anomalies in the Qatruyeh hematite ores reflect cooling of the Eu-enriched hydrothermal fluid subsequent to iron ore deposition.

The difference in Cl contents among layered magnetite, massive magnetite, and hematite can be explained by metal-ligand complexation. Zhu and Sverjensky [76] demonstrated that partitioning of F and Cl between minerals and hydrothermal fluids is a strong function of temperature, pressure, pH, and fluid composition. Chloride solutions are very adequate to transport enough metals to form deposits [77]. According to these authors, the Cl/F ratio increases with increasing temperature and pressure. The Cl⁻ ion is a high intermediate Lewis acid ligand and will affect the solubility of divalent metals (e.g., Fe²⁺) in hydrothermal solutions, forming a range of iron minerals such as sulfides (pyrite and chalcopyrite) and carbonates (siderite) [78–80], as observed in the Qatrureh area. Most experimental studies indicate that FeCl⁺ and FeCl₂ are the main complexes involved in the hydrothermal transport of ferrous iron, especially at high temperatures (>300°C). At the Qatruyeh, Cl concentration in the hematite ores relative to layered magnetite decreases with respect to increasing pH and decreasing temperature due to interaction between dolomitic marbles and primitive acidic-high temperature hydrothermal fluids. Therefore, a higher pH of the fluids should indicate higher concentrations of Cl in the layered magnetite relative to hematite. High Cl value records related to Fe in the Qatruyeh iron ores are good evidences for mentioned complexes in Cl-F-Fe triangular diagram (Figure 15(a)). From these data, it is clear that lower pH, higher concentrations of chloride complex as a ligand, or higher temperatures usually increase the capability of hydrothermal fluids to carry sufficient Fe and REE to explain the observed -enrichments in all layered magnetite relative to massive magnetite and hematite ores in Cl-F- trigonal diagram (Figure 15(b)).

Figure 15: Triangular plots for determination of ligand-metal complexes in iron ores at the Qatruyeh area. (a) Fe-Cl-F triangular plots and (b) -Cl-F triangular plots.

Field observations and microscopic studies indicate two different alternative genetic concepts for ore mineralization in the Qatruyeh area. A syn-metamorphic or premetamorphic origin for the massive magnetite is supported by our observations on pebbles of the Jurassic Deh Vazir conglomerate. Magnetite recrystallization and the presence of ductile deformation textures are clear evidence for origin of layered magnetite and hematite ores later to peak of Cimmerian metamorphism followed the continental collision events.

Fluid inclusion study has proven to be an important tool for constraining the physicochemical conditions of hydrothermal mineralization [81]. The microthermometric results and the moderate salinity of the studied fluid inclusions suggest that mineralization at the Qatruyeh occurred under mesothermal conditions. At the Qatruyeh area similar to other mesothermal deposits, ore forming system is accompanied by both replacement and brecciated textures with the latter more common in shallower deposits and well developed alteration patterns [62], with sodic-calcite alteration in depth and the propylitic-hematitization haloes in shallower depths [11, 53, 62]. Hematite and quartz (± pyrite ± chalcopyrite) veins accompanied the late stage of each main ore mineralization in the Qatruyeh area.

The fluid inclusion study data also indicate that the ore forming fluids at the Qatruyeh were CO₂-bearing, low to moderately saline, NaCl-MgCl₂-CaCl₂-H₂O rich fluids. The source of the fluids (magmatic or metamorphic origin) could not be unequivocally determined from the available data; nevertheless, the distribution of fluid inclusions in ()-salinity diagram [34], with lines of constant fluid density imply cooling and increasing of pH, boiling, and fluid mixing, may play an important role in the iron ore deposition in the area (Figure 16). Cooling and increasing of pH are the main factors affecting precipitation of layered magnetite minerals. However, other processes such as fluid mixing and boiling also seem to be effective on such a precipitation. The precipitation of layered magnetite ores and actinolite was occurred by cooling and an increasing of pH due to reaction of ore bearing fluids with dolomitic-marble rocks. For example, in a simplified reaction:

Figure 16: The most important factors for iron precipitation at Qatruyeh area in homogenization temperature ()-salinity diagram [34].

An increase in pH will move the reaction to the right side, resulting in the precipitation of magnetite and actinolite [78].

Boiling results in the production of vapor and loss of H₂O, and other volatile species occur. Salinity variations (from 3.5 to 15 wt.% NaCl equiv.) in the fluid inclusions data can be produced by boiling. This accompaniment to cooling would result in production of a relatively high-density liquid phase. Figure 16 shows that the density of mineralizing fluid at the Qatruyeh ranged from 0.6 to 0.93 g cm⁻³. In addition, some fluid inclusions that contain relatively high concentrations of CO₂ in quartz can be constructed assuming a model involving a fluid rising adiabatically and mixing with metamorphic fluids.

10. Conclusions

Based on ore mineral types and alteration assemblages, the mineralization processes have been divided into the following stages: (I) layered magnetite ore stage, (II) sulfide ore stage, and (III) hematite ore stage. Stage I involved the formation of the layered magnetite ore, high temperature hydrothermal activity, replacement textures, and assemblages of actinolite + quartz + titanite+ siderite + paragonite ± tourmaline. Stage II partially overlapped with stage I and includes hematite ores with epidote + chlorite + sericite + quartz ± magnetite assemblages. Propylitic zones with associated hematite ores and brecciated textures are shown by low-temperature oxidizing- hydrothermal fluids in shallow levels due to cooling and fluid mixing at this stage. Stage III involved the formation of hematite and quartz veins and some minor sulfide minerals as chalcopyrite and pyrite. Therefore, the evolution of hydrothermal fluids varies due to fluid-dolomitic-marble interaction from acidic to alkaline affinity during iron mineralization.

The low-grade magnetite ores and diorites whole rock REE patterns are comparable to each other, indicating that the bulk of REE concentration in low-grade magnetite is inherited from precursor diorite during the replacement process that was obvious in ore textures. Besides, trace elements geochemical investigation of the metamorphosed carbonate host rocks shows that

(1)HFSEs, such as Th, Hf, Zr, and Ta, were immobile during hydrothermal alteration and iron mineralization.(2)REEs were moderately mobile, whereas large ion lithophile elements such as Ba, Sr, Rb, and Cs were depleted during the alteration and iron mineralization.

From the available data, it is not obvious whether the massive magnetite formed from an iron-rich melt or through metasomatism but the presence of magnetite pebbles in the Jurassic Deh Vazir conglomerate indicates that a part of ore mineralization occurred syngenetic or premetamorphic.

Fluid inclusion data suggest that low to moderate saline fluid (3.5 to 15 wt.% NaCl equiv.) was possibly responsible for the development of low-grade magnetite ore that indicates episodes of hydrothermal activities in mesothermal systems for Fe occurrences in this region. The microthermometric data reflect variable amounts of magmatic fluids and low salinity metamorphic fluids. The temperature during the main mineralization event was between 300° and 410°C. Increase in pH due to reaction of ore fluids with dolomitic-marble rocks and effervescence can be effective mechanisms of ore precipitation. In addition, mixing with cooler probably metamorphic fluids had the effect of decreasing the salinity and temperature of the equilibrated magmatic fluid, making it more buoyant and capable of moving out from the apophyses into the host rocks, causing metasomatic reactions and precipitating low-grade magnetite ores from chloride-bearing hydrothermal fluids.

Conflict of Interests

The authors declare that there is no conflict of interests regarding the publishing of this paper.

Acknowledgments

The authors would like to thank the research council of Shiraz University for financing this research (Grant no. 88-GR-SC-83). They express gratitude to professor Nigel. J. Cook (University of Adelaide) who provided many insightful and constructive comments that greatly improved the paper. They would like also to thank professor Warren. C. Day (US Geological Survey) for criticism of an early version of the paper.

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