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Arabian Journal of Geosciences ISSN 1866-7511Volume 8Number 10 Arab J Geosci (2015) 8:8481-8495DOI 10.1007/s12517-015-1834-3
Geochronologic, geochemical, and isotopicconstraints on petrogenesis of the dioriticrocks associated with Fe skarn in the Bisheharea, Eastern Iran
M. Nakhaei, S. A. Mazaheri,M. H. Karimpour, C. R. Stern,M. H. Zarrinkoub, S. S. Mohammadi &M. R. Heydarian shahri
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ORIGINAL PAPER
Geochronologic, geochemical, and isotopic constraintson petrogenesis of the dioritic rocks associated with Fe skarnin the Bisheh area, Eastern Iran
M. Nakhaei & S. A. Mazaheri & M. H. Karimpour & C. R. Stern &
M. H. Zarrinkoub & S. S. Mohammadi & M. R. Heydarian shahri
Received: 12 July 2014 /Accepted: 6 February 2015 /Published online: 6 March 2015# Saudi Society for Geosciences 2015
Abstract There are several intermediate (SiO2=57.4–61.2 wt.%) subvolcanic bodies in the Bisheh area of east-ern Iran. Petrochemical studies show that these bodies arecalc-alkaline and metaluminous (A/NK≥1.68, A/CNK≤0.99) diorite porphyries. They are enriched in large-ionlithophile elements (LILE) and have negative anomaliesof Nb, Ti, Ta, and P. Chondrite-normalized REE patternsexhibit light-rare-earth-elements (LREE) enrichment, withmildly fractionated REE patterns ((La/Yb)N<10). TheirNb/Yb versus Th/Yb ratios are similar to rocks formed inactive continental margins. Their isotopic (initial 87Sr/86Srratios is 0.70642 and initial εNd values is −1.49) and othergeochemical data suggest that the Bisheh diorite porphy-ries formed by melting of an enriched phlogopite-bearingmantle source combined with subsequent crustal contami-nation. High values of Rb, Ba, and Th support magmacontamination in the upper crust during magma evolution.Zr-U-Pb age dating for two diorite porphyries yield middleEocene (Bartonian) ages of 39.25±0.43 and 39.16±0.41 Ma. These bodies have intruded into Paleocene lime-stone and caused metasomatism with iron oxide skarnformations.
Keywords Birjand . Iran . Diorite porphyry . 87Sr/86Sr ratio .
Zr-U-Pb age dating
Introduction
The investigated area is situated in the eastern part of the Lutblock, in eastern Iran (Fig. 1). Some general work has beendone on magmatism and the tectonic factors affecting the Lutblock, but the conclusions of these studies are in some casescontradictory. Some researchers believe that Lut magmatismand mineralization formed by subduction (Arjmandzadehet al. 2010, 2011; Eftekharnejad 1973; Tirrul et al. 1983) whileothers consider extension in the early Tertiary period to beresponsible for the formation of basic to intermediate magmasand for the structural control leading to the development ofnumerous mineralized areas (Jung et al. 1983; Samani andAshtari 1992; Tarkian et al. 1983).
Westphal et al. (1986) suggest that in comparison to itspresent position, the Lut block underwent an anti-clockwiserotation of 30–90° relative to Eurasia as a result of India andAfghanistan colliding with Eurasia during the Tertiary period.According to Davoudzadeh et al. (1981), the Lut block hasundergone anti-clockwise rotational movement by as much as135° relative to its current position since the Triassic period.Accordingly, the present eastern border of the Lut block (orig-inally south to southwest facing) would have been part of theactive margin of the now-subducted Neo-Tethys Ocean(Dercourt et al. 1986; Golonka 2004). Plate kinematic recon-structions by Regard et al. (2005, 2010) and Allen et al. (2011)suggest the Lut block to be a relatively rigid continental frag-ment caught between two separate collisions, forming theZagros mountains in the west and the Himalaya in the east.
Abundant magmatic activity has at various times occurredin the Lut block, and different types of mineralization, such as
M. Nakhaei (*)Birjand University of Technology, Birjand, Irane-mail: [email protected]
S. A. Mazaheri :M. H. Karimpour :M. R. Heydarian shahriDepartment of Geology, Ferdowsi University of Mashhad,P.O. Box No. 91775-1436, Mashhad, Iran
C. R. SternDepartment of Geological Sciences, University of Colorado,CB-399, Boulder, CO, USA
M. H. Zarrinkoub : S. S. MohammadiDepartment of Geology, University of Birjand, Birjand, Iran
Arab J Geosci (2015) 8:8481–8495DOI 10.1007/s12517-015-1834-3
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porphyry Cu-Au deposits, epithermal, and a range of veintypes of mineralization and different types of iron oxide de-posits, have formed in association with this activity (see forexample Arjmandzadeh et al. 2011; Karimpour et al. 2005;Karimpour and Stern 2011; Malekzadeh Shafaroudi et al.2010; Richards et al. 2012; Mazloumi et al. 2008; KarimpourandMalekzadeh 2006; Yousefi sourani et al. 2008; Karimpour
and Stern 2011). Specifically, the Middle Eocene to EarlyOligocene (39–30 Ma) period was significant in terms ofmagmatism and mineralization (Karimpour et al. 2011;Karimpour and Stern 2011). The goal of this study is to high-light the geochronology, geochemistry, and isotopic ratios forsubvolcanic bodies of this age in the Bisheh area of the easternLut block.
Fig. 1 The structural map of Central-East Iran and its constituent crustalblocks (compiled from Alavi 1991; Berberian 1981; Haghipour andAghanabati 1989; Jackson and McKenzie 1984; Lindenberg et al.1984). AZF Abiz Fault, BDF Behabad Fault, BKF Biabanak Fault,CHF Chapedony Fault, DRF Doruneh Fault, GWF Gowk Fault, KBF
Kuhbanan Fault, KMF Kalmard Fault, MBF Minab Fault, NAFNostratabad Fault, NHF Nehbandan Fault, NNF Na’in Fault, RJFRafsanjan Fault, SBF Shahre-Babak Fault, TKF Taknar Fault, UZFUzbak-Kuh Fault, ZRF Zarand Fault, ZTZ Zagros Thrust Zone
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Geological setting
The Lut region constitutes a microcontinental block in easternIran (Fig. 1; see Davoudzadeh et al. 1981; Berberian and King1981; Alavi 1991). The western edge of the Lut block is cut offby the Nayband fault. Its northern termination is the depressionof Kavir-e-Namak and the Great Kavir fault. The Bazmanvolcanic complex and the Jaz Murian depression define thesouthern edge. The eastern edge is dissected by the Sistansuture zone. The Lut block has acted as a rigid continental
block since at least the early Mesozoic period, when it wasone of the Cimmerian continental fragments that drifted northfrom the Gondwana margin to open the Neo-Tethys Ocean(Dercourt et al. 1986; Golonka 2004; Hooper et al. 1994;Ramezani and Tucker 2003; Stampfli and Borel 2002).
The sedimentary strata in the Lut block are all younger thanthe Permian era and consist of shallow marine carbonateshales and sandstones. Pre-Jurassic metamorphic rocks andJurassic sediments are encroached on and intruded by differ-ent generations of Jurassic and Tertiary plutonic and volcanic
Fig. 2 Geological map of Bisheh area (Nakhaei, unpublished Ph.D. thesis)
Fig. 3 Field occurrence and thinsection texture of hornblendediorite porphyry. a Hornblendediorite porphyry in contact oflimestone and skarn (view tonorth). b Subhedral hornblendeand plagioclase phenocrysts witha microgranular groundmass inhornblende diorite porphyry,mineral abbreviations used areafter Whitney and Evans (2010)
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Tab
le1
Geochem
icaldataforhornblende
diorite
porphyry
ofBisheh
Samplelocatio
n59°06′50″
59°05′50″
59°07′1″
59°06′7″
59°06′8″
59°07′4″
59°09′8″
59°06′31″
59°07′1″
59°06′19″
59°06′8″
59°06′35″
59°06′18″
Feskarns
(Meinert1995)
31°44′03″
31°42′40″
31°44′5″
31°42′41″
31°42′31″
31°43′59″
31°44′11″
31°43′57″
31°44′5″
31°42′41″
31°42′41″
31°43′36″
31°43′39″
Sampleno.
N.B.137
NB46
NB179
N.B.82
N.B.61
NB173
NB171
NB131
NB178
NB86
NB181
NB145
NB121
Mean
Range
SiO
2(w
t.%)
58.86
58.98
59.99
59.01
57.68
57.35
59.93
58.62
58.47
60.51
58.39
58.83
61.17
59.3
47–75.6
TiO
20.74
0.63
0.57
0.58
0.75
0.77
0.57
0.59
0.64
0.6
0.75
0.8
0.63
0.8
0.1–3.1
Al 2O3
15.01
15.63
14.12
15.96
14.95
14.57
15.03
15.78
15.54
15.69
15.24
14.71
14.05
16.8
12.2–22.7
FeOt
8.1
8.63
8.3
8.4
8.93
7.79
8.69
8.5
8.75
8.49
8.53
7.87
7.72
2.8
0.5–6.5
MnO
0.12
0.19
0.14
0.07
0.08
0.14
0.12
0.14
0.14
0.14
0.1
0.14
0.16
0.1
0–0.6
MgO
3.14
3.69
3.69
2.56
3.18
3.14
2.18
3.76
2.87
2.42
3.21
3.24
2.94
30.2–7.9
CaO
6.58
6.76
5.49
8.57
8.11
6.77
6.52
4.64
6.1
6.04
6.71
5.75
6.5
7.2
0.9–22.4
Na 2O
2.43
2.8
2.4
2.5
2.62
2.64
2.69
2.62
2.51
2.47
2.49
3.08
3.16
40.6–7.5
K2O
2.86
0.71
2.73
0.14
1.12
2.35
1.93
2.94
2.48
1.97
2.6
3.46
1.24
2.1
0.2–5.6
P2O5
0.21
0.17
0.16
0.15
0.14
0.2
0.14
0.15
0.16
0.13
0.22
0.2
0.15
0.3
0–1.5
LOI
1.6
1.99
1.8
2.9
21.93
12.4
21.7
1.7
1.1
1.85
Total
99.65
100.1
99.39
100.8
99.5
99.4
98.8
100.1
99.66
100.1
99.78
99.34
99.57
Mg#
0.41
0.43
0.44
0.35
0.39
0.42
0.31
0.44
0.37
0.33
0.40
0.42
0.40
ASI
0.78
0.88
0.83
0.80
0.73
0.75
0.81
0.99
0.86
0.91
0.79
0.76
0.76
Ba(ppm
)507
283
455
112
279
509
381
525
439
363
517
615
242
326
1–658
Rb
80.5
32.5
90.4
12.4
47.3
75.9
55.6
103.1
83.5
65.7
84.5
103.4
36.4
392–137
Sr470.1
542.6
360.4
293.5
732.7
481.5
284.3
422.4
376
331.8
487.3
539.4
343.9
505
20–981
Zr
152.3
129.7
135
116.2
102.7
162.9
100.9
149.5
131.6
120.6
167.1
169.9
134.9
141
66–227
Nb
11.7
6.3
8.2
8.6
7.1
13.4
68.7
7.9
8.2
13.2
13.4
5.6
93–21
Y21.5
19.1
25.2
1617.5
20.9
1722.5
22.2
16.3
21.1
20.8
19.5
2416–35
Cs
2.9
4.9
8.6
2.1
0.9
44.1
3.7
6.3
2.2
4.8
5.1
0.9
Ta0.9
0.4
0.7
0.3
0.5
0.9
0.6
0.6
0.6
0.6
11
0.5
Hf
3.8
3.3
3.7
2.6
34.1
3.2
3.7
3.7
3.4
3.9
4.8
3.4
Th
10.1
3.2
9.9
3.8
3.1
10.4
69.9
9.2
4.1
10.2
10.1
3.7
50–30
U2.3
82
0.8
0.7
2.6
1.5
22.1
1.1
2.5
2.4
0.7
Co
21.2
16.6
14.7
1414.7
20.1
13.3
14.2
16.1
1418.7
20.8
13
La
28.1
16.2
25.5
18.7
14.3
27.9
17.8
23.8
21.7
17.8
27.4
28.4
14.7
160–45
Ce
55.8
34.6
51.5
3328.5
56.6
39.1
51.9
48.2
36.7
59.8
58.9
3143
19–73
Pr6.47
3.94
5.88
4.07
3.43
6.42
4.17
5.74
5.23
4.11
6.44
6.54
3.67
Nd
24.3
16.7
21.1
14.5
13.7
26.1
16.8
24.2
22.1
16.9
27.3
27.8
14.6
Sm
5.06
3.26
4.7
3.35
3.17
4.71
3.31
4.45
4.17
3.24
4.75
5.01
3.14
Eu
1.25
0.99
1.09
1.07
1.01
1.21
0.87
10.95
0.97
1.2
1.21
0.98
Gd
4.55
3.27
4.61
3.41
3.06
4.17
3.24
4.12
4.13
3.01
4.46
4.41
3.39
Tb
0.64
0.55
0.69
0.45
0.51
0.65
0.52
0.65
0.65
0.49
0.67
0.69
0.58
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rocks (Mahmoudi et al. 2009). More than half of the exposedrocks within the Lut block are volcanic and plutonic rocks.The magmatic activity in the Lut block began during the mid-dle Jurassic period. Shah Kuh, Surkh Kuh, and Klateh Ahanigranitoids (Middle Jurassic, 165–162 Ma) are among theoldest rocks exposed within the Lut block (Esmaeily et al.2005; Tarkian et al. 1983; Karimpour et al. 2011).
Cenozoic calc-alkaline magmatism in the Lut block waswidespread and consisted predominantly of Eocene-Oligocene andesitic to dacitic volcanic rocks, with localsubvolcanic granodioritic to granitic plutons (Jung et al.1983). In a series of 1:250,000 geologic maps published bythe Geological Survey of Iran, few igneous rocks of Mioceneage were reported, and younger magmatism is restricted tolocal alkali basalt eruptive centers and flows of the Plioceneto Quaternary periods (see, for example, Pang et al. 2012;Saadat et al. 2010; Walker et al. 2009). Quaternary sanddunes, salt flats, and alluvial fans also cover large areas ofthe Lut block.
The study area is located 196 km south of Birjand in east-ern Iran, between 59°05′35″ to 59°07′13″E and 31°42′13″ to31°44′13″N. The primary rock units in the Bisheh district aresedimentary, subvolcanic, pyroclastic, and skarns (Fig. 2). Ju-rassic shale and sandstone are the oldest rocks in this region.They are discordantly overlain by brown Paleocene conglom-erate and massive cream to white limestone (Behrouzi andNazer 1992). Eocene volcanic rocks include andesites anddacitic tuffs. Subvolcanic bodies have intruded into all thesedimentary rocks and produced (especially in the limestone)skarn mineralization. Petrographic studies on Bishehsubvolcanic rocks show that they are hornblende quartz dio-rite porphyry, hornblende pyroxene diorite porphyry, horn-blende diorite porphyry, and pyroxene diorite porphyry(Fig. 2). Fieldwork and petrographic studies show that horn-blende diorite porphyry is the main body that has intruded intothe limestone, changing it to marble and skarn. In the north-west of the study area, Neogene conglomerates with a thick-ness of 40 to 50m discordantly overlie Eocene volcanic rocks.
Sample description and petrography of the subvolcanicbodies
Three hundred fifty samples were collected from outcrops and20 boreholes in the Bisheh area. As previously stated, themain subvolcanic bodies that have caused skarnification arehornblende diorite porphyry. These units mainly crop out inthe southern and central parts of the study area and have arather monotonous appearance in the field that includes darkgray (Fig. 3a) and fine-grained specimens. These rocks con-tain phenocrysts of plagioclase (40 to 45 %) and hornblende(10 to 12%) in a fine-grained plagioclase–hornblende ground-mass (Fig. 3b). Accessory minerals are sphene and apatite.T
able1
(contin
ued)
Samplelocatio
n59°06′50″
59°05′50″
59°07′1″
59°06′7″
59°06′8″
59°07′4″
59°09′8″
59°06′31″
59°07′1″
59°06′19″
59°06′8″
59°06′35″
59°06′18″
Feskarns
(Meinert1995)
31°44′03″
31°42′40″
31°44′5″
31°42′41″
31°42′31″
31°43′59″
31°44′11″
31°43′57″
31°44′5″
31°42′41″
31°42′41″
31°43′36″
31°43′39″
Sampleno.
N.B.137
NB46
NB179
N.B.82
N.B.61
NB173
NB171
NB131
NB178
NB86
NB181
NB145
NB121
Mean
Range
Dy
4.05
3.36
4.31
2.7
2.98
3.71
3.05
3.86
3.87
2.92
3.73
4.05
3.3
Ho
0.77
0.69
0.86
0.68
0.64
0.73
0.65
0.81
0.83
0.57
0.74
0.76
0.74
Er
2.22
2.04
2.66
1.6
1.76
2.11
1.81
2.27
2.2
1.63
2.25
2.22
2.23
Tm
0.36
0.31
0.38
0.23
0.26
0.32
0.31
0.35
0.36
0.25
0.33
0.34
0.31
Yb
1.93
2.08
2.64
1.6
1.73
2.07
1.89
2.31
2.35
1.57
2.06
2.19
2.24
Lu
0.33
0.32
0.4
0.27
0.28
0.31
0.29
0.34
0.34
0.25
0.31
0.33
0.36
(Tb/Yb)N
9.82
5.25
6.51
7.08
5.57
9.09
6.35
6.94
6.22
7.64
8.74
8.96
4.42
(Tb/Yb)N
1.46
1.16
1.15
1.34
1.29
1.38
1.21
1.24
1.21
1.37
1.38
1.42
1.19
Eu/Eu*
0.80
0.92
0.72
0.96
0.99
0.83
0.81
0.71
0.70
0.95
0.8
0.79
0.92
Ba/Rb
6.29
8.7
5.03
8.92
5.89
6.70
6.85
5.09
5.25
5.52
6.11
5.94
6.64
Rb/Sr
0.171
0.059
0.250
0.043
0.064
0.157
0.195
0.244
0.222
0.198
0.173
0.191
0.105
LOIloss
onignitio
n,Mg#
=100Mg/(M
g+Fetotal)in
atom
icratio
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The phenocryst sizes of plagioclase and hornblende are most-ly in the ranges of ~600–700 and ~300–700 μm, respectively.
Analytical methods
Whole-rock chemistry
The primary major element compositions of 13 samples weredetermined by wavelength-dispersive x-ray fluorescence(XRF) spectrometry, using fused discs and the Phillips PW1410 XRF spectrometer at Ferdowsi University, Mashhad,Iran. LOI was obtained by routine heating procedures. Thesesamples were analyzed for trace elements using inductivelycoupled plasma-mass spectrometry (ICP-MS), following alithium metaborate/tetraborate fusion and nitric acid total di-gestion in the Acme Analytical Laboratories, Vancouver, Brit-ish Columbia, Canada.
Zircon U-Pb dating
Zircon grains were separated from two hornblende diorite por-phyries (samples N.B.121 and N.B.86) using conventionalheavy liquid and magnetic techniques. The internal structuresof the zircon grains were examined using cathodoluminescenceimages, taken at the Institute of Earth Sciences, Academia Sinica,Taipei, to select suitable positions for subsequent analysis. ZirconU-Pb isotopic analyses were performed by laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS),using an Agilent 7500s machine and a New Wave UP213 laserablation system, equipped at the Dr. Shen-su Sun memorial lab-oratory in the Department of Geosciences, National Taiwan Uni-versity, Taiwan and following the analytical procedures of Chiuet al. (2009). The U-Th-Pb isotopic ratios were calculated usingGLITTER 4.0 (GEMOC) software, and common Pb wascorrected using the function proposed by Anderson (2002).The weighted mean U-Pb ages were calculated and concordiaplots were constructed using Isoplot v.3.0 (Ludwig 2003).
Fig. 4 Chemical characterization of least-altered igneous rocks of Bishehassociated with Fe-Cu skarns. a Total alkalis vs. silica classification(Middlemost 1994). b Aluminum saturation index (Maniar and Piccoli1989). c SiO2–(Na2O+K2O) diagram (Middlemost 1994). The alkaline
and sub-alkaline division is after Irvine and Baragar (1971). dA.R.–SiO2
diagram, A.R.=(Al2O3+CaO+Na2O+K2O)/(Al2O3+CaO−Na2O−K2O). The solid line represents the division among calc-alkaline, alkaline,and peralkaline (Geng et al. 2009)
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Sr and Nd isotopes
Sr and Nd isotopic analyses were performed on a six-collectorFinnigan MAT 261 thermal-ionization mass spectrometer atthe University of Colorado, Boulder, Colorado, United States.87Sr/86Sr ratios were determined using four-collector staticmode measurements. Several measurements of SRM-987
during the study period yielded a mean of 87Sr/86Sr=0.71032±2 (error is the 2σ mean). Measured 87Sr/86Sr ratioswere corrected to SRM-987=0.71028.Measured 143Nd/144Ndwas normalized to 146Nd/144Nd=0.7219. Analyses were con-ducted as dynamic mode, three-collector measurements. Sev-eral measurements of the La Jolla Nd standard during thestudy period yielded a mean of 143Nd/144Nd=0.511838±8(error is the 2σ mean).
Results
Major and trace elements
Broad correlation between igneous composition and skarntype with respect to their metal elements has been de-scribed by several researchers in different deposits aroundthe world (Kuşcu et al. 2002; Meinert 1992, 1993, 1995,1997; Moore et al. 2012; Newberry and Swanson 1986;Newberry 1987; Oyman 2010; Pinto-Linares et al. 2008;Ray et al. 2000; Ray et al. 1996; Yücel-Öztürk et al. 2005).The representative whole-rock major and trace elementanalyses for 13 hornblende diorite porphyries are listed inTable 1. The chemical classification of these subvolcanicrocks is consistent with their mineralogy and similar toother intrusives that are associated with worldwide ironskarns (Table 1). They are intermediate in composition(Table 1 and Fig. 4a), metaluminous (Maniar and Piccoli1989), and I-type (Chappell and White 1974, 2001)(Fig. 4b). The total alkali contents (Na2O+K2O) vary from2.64 to 6.54 wt.%, showing characteristics attributed to thesub-alkaline series (Fig. 4c). The low A.R. values of 1.24–1.93 [A.R.=(Al2O3+CaO+Na2O+K2O)/(Al2O3+CaO−Na2O−K2O)] (Geng et al. 2009) indicate calc-alkalinecharacteristics (Fig. 4d).
Fig. 5 Temperature evaluation based on TiO2 and P2O5 after Harrisonand Watson (1984) and Green and Pearson (1986), respectively
Fig. 6 a MORB-normalized trace element and b chondrite-normalized REE patterns for the studied rocks (MORB values—Pearce 1983; chondritevalues—Boynton 1984)
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TiO2 and P2O5 can be used to infer Fe-Ti oxides and apatitesaturation temperature (Harrison andWatson 1984; Green andPearson 1986). Porphyry samples in this study had a TiO2 andP2O5 content of 0.57 to 0.8 wt.% and 0.13 to 0.22 wt.%,respectively, indicating high temperatures (about 800–900 °C) (Fig. 5).
Bisheh dioritic rocks show coherent patterns on a MORBnormalized trace element plot, with pronounced negative Nb,Ta, and Ti anomalies (Fig. 6a). These rocks have 81.2 to142.6 ppm of total REE and display coherent REE patterns,characterized by the relative enrichment of LREE and nearly
flat HREE ((La/Yb)N=4.42 to 9.82; (Tb/Yb)N=1.15–1.46;Table 1) and weak negative Eu anomalies (average Eu/Eu*=0.83) (Fig. 6b).
Zircon U-Pb dating
Two samples of hornblende diorite porphyry were dated. Thezircons were mostly euhedral, colorless, and transparent andrevealed long to short prismatic forms. Zircon CL imaging isan effective way for distinguishing magmatic from metamor-phic zircon (Vavra et al. 1996). The CL characteristics of
Fig. 7 Representative cathodoluminescence (CL) images of zircons from the Bisheh hornblende diorite porphyry with identified analytical number
Fig. 8 a U–Pb concordia diagrams of studied hornblende diorite porphyry, b TuffZirc graphics calculating the age of zircons
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Table 2 Results of U-Pb SHRIMP study of zircons from hornblende diorite porphyry (sample no. N.B.121 and no. N.B.86)
U-Th-Pb ratio Ages (Ma)
Spot Th/U 207Pb/235U ±1σ 206Pb/238U ±1σ 207Pb/206Pb ±1σ 208Pb/232Th ±1σ 206Pb/238U
±1σ
Sample no.N.B.121
01 0.365 0.03955 0.00341 0.0063 0.00016 0.04555 0.00293 0.0022 0.0001 40 1
02 0.3571 0.0436 0.003 0.00612 0.00016 0.05166 0.00241 0.0022 0.00009 39 1
03 0.4032 0.04657 0.00399 0.00612 0.00017 0.05518 0.00341 0.00204 0.0001 39 1
03C 0.3802 0.03453 0.00663 0.00622 0.00025 0.04029 0.00632 0.00206 0.00018 40 2
04 0.3436 0.03723 0.00411 0.00612 0.00017 0.0441 0.0038 0.00229 0.00012 39 1
05 0.4237 0.04443 0.00274 0.00623 0.00016 0.0517 0.00208 0.00227 0.00008 40 1
06 0.3559 0.04223 0.00485 0.00624 0.00018 0.04913 0.00441 0.00215 0.00014 40 1
07 0.4065 0.04356 0.00384 0.00626 0.00017 0.05049 0.00327 0.00236 0.00011 40 1
08 0.3636 0.04451 0.00384 0.00611 0.00017 0.05288 0.0033 0.00234 0.00011 39 1
09 0.361 0.04548 0.00517 0.00621 0.00018 0.05308 0.0047 0.00223 0.00014 40 1
10 0.3425 0.03873 0.00341 0.00633 0.00017 0.04435 0.00288 0.00215 0.00011 41 1
11 0.4098 0.03982 0.00335 0.00601 0.00015 0.04807 0.00312 0.00191 0.00006 38.6 1
13 0.369 0.03726 0.0039 0.0058 0.00015 0.04656 0.00397 0.00185 0.00013 37.3 1
14 0.3759 0.04325 0.00346 0.00611 0.00016 0.05133 0.00296 0.00235 0.0001 39 1
15 0.4098 0.03892 0.00262 0.00602 0.00014 0.04687 0.00233 0.00192 0.00006 38.7 0.9
16 0.4902 0.04251 0.00291 0.00613 0.00016 0.05026 0.00233 0.00202 0.00007 39 1
17 0.4082 0.04377 0.00389 0.00609 0.00017 0.05212 0.00338 0.00213 0.0001 39 1
18 0.4 0.03771 0.00248 0.00605 0.00015 0.04517 0.00202 0.00192 0.00007 38.9 1
19 0.3333 0.04012 0.00435 0.00613 0.00018 0.04747 0.00394 0.00225 0.00013 39 1
20 0.4386 0.0439 0.00281 0.00614 0.00015 0.05188 0.00225 0.00209 0.00008 39.5 1
20C 0.4255 0.03859 0.00266 0.00607 0.00014 0.04609 0.00243 0.00201 0.00011 39 0.9
Sample no.N.B.86
01 0.32 0.03824 0.00372 0.00611 0.00017 0.04536 0.00332 0.00196 0.00011 39 1
02 0.44 0.04181 0.00326 0.00619 0.00016 0.04896 0.00273 0.00206 0.00008 40 1
03 0.27 0.03892 0.00410 0.00616 0.00018 0.04583 0.00367 0.00209 0.00013 40 1
04 0.38 0.04109 0.00171 0.00601 0.00014 0.04958 0.00114 0.00200 0.00006 38.6 0.9
05 0.63 0.03800 0.00270 0.00586 0.00014 0.04704 0.00248 0.00186 0.00005 37.7 0.9
05W 0.38 0.03848 0.00364 0.00575 0.00016 0.04850 0.00353 0.00182 0.00008 37 1
06 0.28 0.03938 0.00229 0.00626 0.00015 0.04561 0.00174 0.00204 0.00008 40.2 1
07 0.52 0.04260 0.00256 0.00608 0.00015 0.05081 0.00200 0.00201 0.00007 39.1 1
08 0.45 0.04090 0.00306 0.00609 0.00016 0.04870 0.00255 0.00195 0.00008 39 1
09 0.31 0.03939 0.00285 0.00601 0.00015 0.04751 0.00254 0.00191 0.00009 38.6 0.9
10 0.46 0.04653 0.00573 0.00617 0.00023 0.05473 0.00498 0.00255 0.00015 40 1
11 0.35 0.04431 0.00414 0.00632 0.00018 0.05088 0.00351 0.00202 0.00011 41 1
12 0.40 0.04602 0.00370 0.00618 0.00017 0.05400 0.00307 0.00209 0.00009 40 1
13 0.36 0.05919 0.00318 0.00620 0.00016 0.06929 0.00225 0.00331 0.00012 40 1
14 0.47 0.03667 0.00301 0.00616 0.00016 0.04315 0.00258 0.00209 0.00008 40 1
15 0.52 0.04196 0.00205 0.00617 0.00015 0.04931 0.00143 0.00208 0.00007 39.7 1
16 0.39 0.04006 0.00281 0.00607 0.00016 0.04784 0.00229 0.00205 0.00008 39 1
17 0.41 0.04422 0.00281 0.00614 0.00016 0.05224 0.00218 0.00206 0.00008 39 1
18 0.75 0.04013 0.00123 0.00608 0.00013 0.04791 0.00071 0.00199 0.00006 39.1 0.8
19 0.32 0.04007 0.00236 0.00591 0.00015 0.04915 0.00185 0.00210 0.00009 38 1
20 0.28 0.03789 0.00216 0.00595 0.00014 0.04623 0.00183 0.00190 0.00010 38.2 0.9
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zircon reflected the content of trace elements in zircon, inparticular rare earth elements (REE), U, and Th concentrations(Hanchar and Miller 1993). Most of the zircons had distinctcores (dark CL) and rims (bright CL) (Fig. 7), which reflecteddifferences regarding U and Th contents. In addition to shapeand zoning, Th/U ratio was a suitable feature for the determi-nation of magmatic and metamorphism zircons (Rubatto et al.2001; Rubatto 2002; Williams 2001; Williams et al. 1996;Rubatto and Gebauer 2000). These zoning features and Th/U ratios demonstrated that the zircon has a magmatic origin.Based on 21 analyzed points for N.B.121 and N.B.86, themean age value (weighted mean) was 39.25±0.43 and 39.16±0.41 Ma, respectively (error in the two sigma levels). Basedon U-Th-Pb zircon age dating, the Bisheh hornblende dioriteporphyry was formed during the middle Eocene (Bartonian)period. The zircon dating results are presented as Concordiaand TuffZirc graphics in Fig. 8 and summarized in Table 2.
Sr and Nd isotopes
Sr and Nd isotope data for a representative sample is providedin Table 3. Their initial 87Sr/86Sr and 143Nd/144Nd ratios were0.70614 and 0.51251, respectively, when recalculated to anage of 39.16 Ma, consistent with the new radiometric results(Table 3). Initial ɛNd isotope values for the Bisheh hbl-dioriteporphyry was −1.49.
The initial 87Sr/86Sr and εNd values of Hbl-diorite porphyryNB-86 are plotted in Fig. 9. Also in this figure, initial 87Sr/86Srratio and the εNd value range of a pyroxene diorite porphyry(44.07 Ma) (Nakhaei, unpublished PhD thesis) that has beenexposed in this area, along with other plutonic-subvolcanicbodies that are close to Bisheh, have also been plotted.
Discussion
Source features
The isotopic value for the Bisheh dioritic porphyry NB-86can be considered as indicative of lithospheric mantle
melting. The trace-element characteristics of these rockscan be used to characterize their mantle source. The MORBnormalized trace element pattern (Pearce 1983) of all sam-ples shows a negative anomaly for Nb, Ti, and Ta (Fig. 6a).The negative anomaly of these elements can be explained bythe presence of a residual TNT phase (Ti-Nb-Ta, e.g., rutile,ilmenite, and perovskite) during the melting of the source(Reagan and Gill 1989). Furthermore, Bisheh subvolcanicbodies were enriched with Rb, Ba, and Th, indicating thatthey had experienced interaction with the continental crust(Kuşcu et al. 2002). The residual phases of accessory min-erals such as zircon, allanite, and titanite in the source can beapplied to account for thedepletionof zirconiumandyttrium.These data are consistentwith numerous examples fromcon-tinental and continental-margin settings (Delaloye andBingöl 2000).
The chondrite-normalized rare earth element pattern ofthe studied rocks shows a high ratio of light rare earthelements (LREE) to heavy rare earth elements (HREE),with (La/Yb)N ratios ranging from 4.4 to 9.8 (Fig. 6b).The rocks do not exhibit conspicuous Eu anomalies (Eu/Eu*=0.7–0.99). Weakly negative Eu anomalies in somesamples can be derived from the breakdown of plagioclaseduring hydrothermal alteration because Eu is more mobilethan other REEs (Ling and Liu 2002; Warmada et al.2005).
In the Y+Nb and Y+Nb versus Rb diagrams (Fig. 10a, b),all the samples have been plotted in the VAG field and in theNb/Yb versus Th/Yb diagram (Fig. 11); dioritic rocks areplotted in active continental margins.
Experimental studies have demonstrated that Mg# is auseful index for discriminating the source of melts derivedfrom crust or mantle. Melts from subducted oceanic slab orfrom lower crustal mafic rocks are characterized by lowMg#
(<4), regardless of melting degrees, whereas those withMg#
>4 can only be obtained with a mantle component involved(Rapp andWatson 1995). The dioritic rocks from the BishehhaveMg# (0.33–0.44; Table 1), which is consistent with der-ivation frommantle melts contaminated by continental crust(Fig. 12).
Table 3 Rb-Sr and Sm-Nd isotopic data of hbl-diorite porphyry (N.B.86)
Sample Rb (ppm) Sr (ppm) 87Rb/86Sr 87Sr/86Sr m (2σ) R0(Sr) Sm (ppm) Nd (ppm) 147Sm/144Nd 143Nd/144Nm (2σ) R0(Nd) εNd I
NB-86 49 279 0.50756 0.70642 0.70614 3.301 15.92 0.1254462 0.51254 0.51251 −1.49
Errors are reported as 2σ (95 % confidence limit)
R0(Sr) initial ratio of 87 Sr/86 Sr for the sample, calculated using 87 Rb/86 Srm and (87 Sr/86 Sr)m and an age of 39.16Ma (hbl-diorite porphyry) (age basedon zircon); R0(Nd) initial ratio of 143 Nd/144Nd, calculated using 147 Sm/144Nd and (143Nd/144 Nd)m and an age of 39.16Ma (hbl-diorite porphyry) (agebased on zircon); εNd I initial εNd value; m measured
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Experimental studies have shown that melts formed un-der high-pressure conditions tend to have higher Al2O3/(Fe2O3+MgO+TiO2) and Al2O3/(CaO+Na2O+K2O) ra-tios than those formed under low pressure conditions.Mantle-crust interaction occurs in the area between the highand low pressure curves (Patiňo Douce 1999). The dioriticrocks of this study have intermediate Al2O3/(Fe2O3+MgO+TiO2) and Al2O3/(CaO+Na2O+K2O) ratios and plotbetween the HP and LP curves (Fig. 13); thus, mantle-crustinteraction could have been involved during the evolutionof dioritic rocks.
The hornblende diorites porphyry have a relativity highK2O content (mean 2.04 wt.%), low Ba/Rb ratios (5.03–8.92), but high Rb/Sr (0.04–0.25) ratios (Table 1), suggest-ing the existence of phlogopite in their mantle source
(Furman and Graham 1999) or magma contamination inthe upper crust.
The initial 87Sr/86Sr of Bisheh hornblende diorite por-phyry was 0.70614 and the (143Nd/144Nd)i isotope compo-sitions and εNd value of these rocks was 0.51251 and−1.49, respectively (Table 3). Initial εNd values in somesubvolcanic-intrusive bodies close to our study area, suchas Maher-Abad (Malekzadeh Shafaroudi et al. 2010),Khopik (Malekzadeh Shafaroudi et al. 2010), Kuh Shah(Abdi and Karimpour 2012), Dehsalm (Karimpour et al.2012), and Chah-Shaljami (Arjmandzadeh et al. 2011),are shown in Fig. 9 for comparison. These different valuesmight be due to either variation in source composition orthe contamination rate of mantle-derived magma by crustalmaterial.
Fig. 10 Tectonic discriminationdiagrams of aY+Nb vs. Rb and bYb+Ta vs. Rb (Pearce et al. 1984)
Fig. 9 (87Sr/86Sr)i–εNd(t)diagram. Data source: the fieldsfor asthenospheric andlithospheric mantle melting arefrom Wilson (1989) and Daviesand von Blanckenburg (1995 andreferences therein)
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Conclusions
Tertiary intrusive-subvolcanic rocks have intruded intoPaleocene limestone and formed skarn with iron miner-alization. Petrographic studies show that hornblende di-orite porphyry is the most important unit that has con-tributed in skarnification. Hornblende diorite porphyryin the Bisheh area is related to volcanic arc typemagmatism, as evidenced by low ASI, prominent Nb,P, Ti, Y, Yb, Ta negative anomalies, and a high Th/Ta
ratio. The age of two hornblende diorite porphyries,based on zircon U-Pb age dating, were established ashailing from the middle Eocene period (39.25±0.43 and39.16±0.41 Ma). The geochemical characteristics of theBisheh hornblende diorite porphyry with relatively highMg#, Na2O enrichment (Table 1), depletion in HFSEs,as well as relatively high initial 87Sr/86Sr ratios and lowεNd values, suggest that their primary magmas wouldhave been derived from partial melting of the enrichedlithospheric mantle, modified during upraise through thecontinental crust.
Fig. 13 Major element diagrams for the dioritic rocks. The dashed linesare reaction curves that model the compositions of melt produced byhydridization of high-Al olivine tholeiite with metagreywacke. The areabetween the high- and low-pressure curves encompasses the range ofdepths at which mantle–crust interaction takes place (Patiňo Douce 1999)
Fig. 12 Mg# vs. SiO2 for the diorites porphyry from Bisheh compared toexperimentally produced high-pressure partial melts of garnet-amphibolite and eclogite (Kelemen 1995), mantle melts (basalts), andQuaternary volcanic rocks from the Andean southern Southern VolcanicZone (SSVZ, Lopez-Escobar et al. 1993). It also shows the fields of purecrustal partial melts obtained in experimental studies by dehydrationmelting of low-K basaltic rocks at 8–16 kbar and 1000–1050 °C (Rappand Watson 1995), of moderately hydrous (1.7–2.3 wt.% H2O) mediumto high-K basaltic rocks at 7 kbar and 825–950 °C (Sisson et al. 2005)
Fig. 11 Th/Yb versus Nb/Yb diagram (after Pearce 2008)
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Acknowledgment The authors are grateful to Professor Sun-LinChung from the Department of Geosciences, National Taiwan University,for supporting the researchers in the use of U-Th-Pb zircon age dating.
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