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Geochemical properties of soils surrounding the Deliklitaş Au deposit, Turkey
Accepted Manuscript Areal distributions and geochemical properties of soils surrounding the Deliklitaş Au deposit, Turkey Güllü Kirat, Nasuh Aydin PII:
S1464-343X(16)30152-2
DOI:
10.1016/j.jafrearsci.2016.05.006
Reference:
AES 2565
To appear in:
Journal of African Earth Sciences
Received Date: 20 January 2015 Revised Date:
19 April 2016
Accepted Date: 7 May 2016
Please cite this article as: Kirat, G., Aydin, N., Areal distributions and geochemical properties of soils surrounding the Deliklitaş Au deposit, Turkey, Journal of African Earth Sciences (2016), doi: 10.1016/ j.jafrearsci.2016.05.006. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.
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Güllü KIRAT1*, Nasuh AYDIN2
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Geochemical properties of soils surrounding the Deliklitaş Au deposit, Turkey
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([email protected])
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Phone: (+90)354 2421001/7921, Fax: (+90)354 2421005
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2
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Engineering ([email protected])
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Bozok University, Faculty of Architecture and Engineering, Department of Geological Engineering
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Balıkesir University, Faculty of Architecture and Engineering, Department of Geological
* Corresponding author
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ABSTRACT
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The Deliklitaş gold deposit is in northwest Turkey, where a renowned gold province
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containing many major hydrothermal deposits related to Tertiary volcanic rocks. Because of
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the limited outcrops in the region, one of the most effective ways to prospect for new deposits
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is soil sampling. In this study, 183 soil samples were systematically collected from the area
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around the Deliklitaş Au deposit. Metal content of the samples, and their relationships and
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distribution according to distance away from the ore body were statistically investigated. The
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analysis of metals and metalloids in soil samples yielded the following metal ranges: Au from
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0.005 to0.54 mg/kg (average 0.04); Ag from 0.03 to2.66 (average 0.22); As from 3.4 to315
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(average 30.3); Sb from 0.15 to19.25 (average 1.62); Cu from 2.5 to35 (average 11.73); Pb
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from 17.4 to545 (average 73.76) and from Zn 14 to1240 mg/kg of soil (average 106.71). For
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the areal distribution of metals 50%, 70%, 90% and 95% of the cumulative data were used for
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contouring element contents in the soils, using 50% as the baseline value and 95% as the
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anomalous value. Eigen values, Varimax Rotation method with Kaiser Normalization tested
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and determined the suitability of the number of data sets. Factor numbers were determined as
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3, according to Eigen values determined for the soil samples. Factor 1 refers to ore minerals
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of epithermal system, Factor 2 refers to main rock sources of Pb and Zn and Factor 3 refers to
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environmental effects. Ag–Au, Pb–Zn and Sb–As pairs show high correlation in the cluster
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analysis indicating element relations. Please add an overarching sentence here, on
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implications etc.
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Key Words: Epithermal, Soil, Pearson correlations, Eigen value.
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1. Introduction The Deliklitaş Au deposit is approximately 23 km northwest of Balikesir city in
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western Turkey (Fig. 1). The western and northern parts of the area are topographically
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elevated, but the southeastern portion has a flat topography. Some highest peaks in the area
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are: Yaylak Hill and Eyrek Hill (Fig. 2). The elevated parts of the Deliklitaş area consist of
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altered andesites cut by hydrothermal quartz veins.
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The northwestern part of Turkey is a well-known gold province containing many
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hydrothermal Au deposits related to Tertiary volcano-plutonic systems. Epithermal gold
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deposits are economically and the most important types of gold deposits in the region where
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several operating gold mines such as Efemçukuru, Kızıltepe–Kepez, Ovacık and Küçükdere
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(Balıkesir region) occur. Epithermal Au (± Ag) deposits include quartz veins and
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disseminated types near the Earth’s surface (≤1.5 km) in volcanic, sedimentary, and
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metamorphic rocks. The deposits commonly occur in association with hot springs frequently
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in young volcanic centres. The ores are dominated principally by precious metals (Au, Ag),
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but some deposits also contain variable amounts of base metals such as Cu, Pb, and Zn
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(Taylor, 2007).
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Volcanogenic epithermal Au–Ag deposits commonly occur in the Circum-Pacific
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orogenic belt associated with magmatic arcs ranging in age from Cretaceous to Recent
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(Corbett and Leach, 1998; Hedenquist et al., 1990). Epithermal systems form at shallower
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crustal levels than porphyry type deposits (Corbett, 2002). Low-sulfidation epithermal
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deposits are dominated by adularia – sericite alteration and low sulphur Au–Ag
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mineralization. The former is originated by acidic hypogene fluids while the latter is formed
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by neutral reduced fluids (Berger and Henley, 2011; Hedenquist, 1987; Hedenquist et al.,
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1996; Henley and Berger, 2011). Examples of Low-sulfidation epithermal deposits include
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Baguio (Philippines), Cripple Creek (USA), Creede (USA), Round Mountain (USA),
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McLaughlin (USA), Hishikari (Japan), Kelian (Indonesia), Ladolam and Porgera (Papua New
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Guinea) (Carman, 2003; Sherlock, 2005). The origins of low-sulfidation type of ore deposits
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are explained by various genetic models (Corbett, 2002; Hedenquist et al., 2000; Simmons et
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al., 2005). The low-sulfidation type ore deposits originate either from reduced or neutral
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diluted fluids caused by deep circulating meteoric fluid systems mixed with magmatic water
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characterized by sulphur reduced to H2S (Corbett and Leach, 1998; Hayba et al., 1985).
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Depending on the mixing rate of hydrothermal fluids and meteoric water at shallow depths,
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different types of alteration or Au ore bodies are produced (Lee et al., 2014) Most epithermal gold deposits hosted in Mesozoic–Cainozoic sub aerial volcanic
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rocks formed at shallow depths include those in the USA (John, 2001), Jacinto in Cuba
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(Simon et al., 1999), the Hishikari and Nansatsu epithermal deposits in Japan, Golden Cross
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in New Zealand, Chinkuashih in Taiwan, Zijinshan and Bitian in Fujian, China (Simmons and
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Brown, 2006) (Zhai et al., 2009).
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Andean type low-sulfidation epithermal deposits are small. Large Andean type
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deposits include the Jurassic Fruta del Norte deposit in Ecuador (Henderson, 2009), and the
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Palaeocene El Peñón deposit of northern Chile (Warren et al., 2004, 2007). The Late Jurassic
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to Early Cretaceous deposits of the Deseado and Patagonian Massifs (Dietrich et al., 2011;
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Fernández et al., 2008) also fall in this system. The low-sulfidation deposits mentioned above
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occur at elevations below 2400 m.a.s.l., in predominantly in rhyolitic volcanic and
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volcaniclastic rocks, lack spatial and temporal association with porphyry systems (Sillitoe,
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2010) occurring in extensional tectonic settings without associated contractional deformation
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and surface uplift during mineralization. However, there are also examples of epithermal
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deposits containing low-sulfidation mineralization that occur in larger magmatic-
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hydrothermal systems in arc segments also containing porphyry style or high-sulfidation
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epithermal mineralization. Examples of these deposits include Cerro de Pasco (Peru:
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Baumgartner et al., 2008), Marmato and Buriticá (Colombia: Tassinari et al., 2008; Lesage,
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2011), all Mid to Late Miocene in age. The low-sulfidation nature of epithermal deposits in
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some compressional arc settings attributed to more reactive, locally reducing host or basement
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rock characteristics (e.g., The Marmato epithermal gold deposits: Tassinari et al., 2008). Thus,
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as shown earlier (Sillitoe and Hedenquist, 2003) low-sulfidation deposits are associated with
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overall compressional arc and extensional rift settings.
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The occurrence together of Ag, As, Au, Cu, Pb, Zn and Sb in soils near epithermal
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deposits is related to the primary sulphide minerals. The metals and non-metals are partly
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concentrated in the residual sulphide minerals, in soil and river sediments and by clinging to
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jarosite-type phases, anglesite, scorodite, dissolved sulphates, clay minerals and Fe3+
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hydroxides (Ashley, et al., 2004). The mobilities of Cu and Zn are effective in this
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environment. Cu is absorbed by carbonates, clays, oxides and organic matter (Pendias, 2001).
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Pb forms soluble complex ions with sulphates, bicarbonates and carbonates (Sposito, 1989).
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Zn is absorbed by clay minerals, oxides and organic matter, or might translocate by ion
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exchange (Wilson et al., 2008).
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Some workers have investigated and modelled the trace element change in soils near
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Au deposits their results indicate that the lower soil zone is more significant than the upper soil zone (Burt, et al., 2005, Wilson, et al., 2008).
In this study, the geological and
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geochemical properties of soils collected around the Deliklitaş Au deposit were studied and
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statistically analysed show that Au is closely associated with Ag and As.
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2. Geology
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The main lithotectonic/stratigraphic units in the study area include Late Oligocene-
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Early Miocene volcanic rocks (Hallaçlar volcanic rocks) and Quaternary alluvium (Fig. 2 and
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3).
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2.1. Hallaçlar Volcanic Rocks
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The Hallaçlar volcanic rocks (Fig. 2 and 3) (400 m thick) are composed of white to
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dirty yellow, red and brown coloured andesitic to dacitic rocks, lava flows, silicified rocks,
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and their alteration products. The andesite and dacites are strongly affected by hydrothermal
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alteration in the Deliklitaş area, typically resulting in extensive alteration and silicification.
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Altered volcanic rocks are further subdivided into: slightly altered volcanic rocks, a
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moderately to weakly argillaceous zone and a silicified zone. The lava flows are characterised
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by plagioclase, biotite, clinopyroxene, feldspar, and some opaque phenocrysts found in a fine-
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grained plagioclase- and clinopyroxene-rich matrix.
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The age of the Hallaçlar volcanic unit is Upper Oligocene–Early Miocene
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(Krushensky, 1976). The upper parts of the Hallaçlar volcanic units are silicified, kaolinitized
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and affected by pyrite mineralisation (Demirel, et al., 2004). Petrographic study of the lavas
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of the Hallaçlar volcanic unit indicates that the lavas have a matrix of volcanic vitreous
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matter with plagioclase and biotite microliths containing oligoclase and andesine type
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plagioclases, hornblende, biotite, augite and rare quartz phenocrysts; and the lavas are locally
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silicified (Ercan, 1986).
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Hallaçlar volcanic rocks are overlain discordantly by the lava flows and tuffs of a
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younger volcanic phase in the study area. Despite that these lavas and tuffs were already
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known from outcrops exposed around Pelit village, it was found during this study that these
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rocks outcrop widely to the east of the study area and are here called “Dedetepe Formation”
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after Krushensky (1976) who first described these rocks in this area. The lavas of the
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Dedetepe Formation are more acidic than those of the Hallaçlar volcanic rocks and are made
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of dacite, rhyodacite and rhyolites. The lavas are of various colours, weathered in some places
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and locally silicified. The tuffs are predominant in the formation and they usually display
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horizontal layering. Agglomerate intercalations are observed locally (Ercan, 1986).
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2.2. Alluvium In Deliklitaş area, the alluvium contains unconsolidated pebbles, sand, silt and muds,
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deposited along the present-day drainage system and formed the basin fill of the tectonically
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active Ovacık basin. The initial opening of the Ovacık basin was directly controlled by a pull-
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apart along a step over between the right-lateral Turplu Fault and the Ovacık Fault (Fig. 3).
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3. Hydrothermal alteration
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All the mineral deposits near the study area are related to volcanic hydrothermal
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systems. Hydrothermal solutions destroyed the original textures of the volcanic rocks. Deposit
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types are commonly epithermal and porphyry style mineralizations. NW–SE to E–W-trending
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phreatic breccias are important in the Deliklitaş region. Massive silicification, vuggy quartz,
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late-stage blanket-like chalcedonic and opaline quartz, argillic alteration characterises the
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alteration halos of the deposit. The intense hydrothermal alteration is contemporaneous with
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extensional and strike-slip faulting. In the Deliklitaş deposit, porphyritic dikes are usually
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altered; this alteration zonation matches the propylitic alteration zonation described by
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Gustafson and Hunt (1975).
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4. Materials and methods
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One hundred and Eighty-three (183) soil samples were collected in the study area (Fig.
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2). Samples e of about 1-1.5 kg were collected at 25-30 cm depth using hammer. All the
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samples were placed in plastic bags, were sieved through a -200 mesh Sieve after drying at
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60oC.
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The samples were analysed at ALS Chemex Laboratory, Canada by the Au-AA24
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method for Au and the Me-MS61 method for multielements (after extracted using microwave
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digestion system) using ICP-MS (Inductively Coupled Plasma-Mass spectrometry) (Lisowiec
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et. al., 2007).
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5. Results and Discussion
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The maximum, minimum, standard deviation and arithmetic mean values of metal and
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metalloid concentrations in the 183 soil samples are shown in Table 1. The soils contain
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0.005–0.54 mg/kg Au having an arithmetic mean value of 0.04 mg/kg. The concentration
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values for Ag in these samples are 0.03 to2.66 mg/kg and the arithmetic mean is 0.22 mg/kg. The concentration values of some elements have wide ranges, for instance; As ranges
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from 3.4 to 315 mg/kg (median 19.7), Sb from 0.15 to 9.25 mg/kg (median 1.18), Cu from 2.5
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to 5 mg/kg (median 11.2), and Pb from 17.4 to 545 mg/kg (median 51.2). Zn values are
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between 14 and 1240 mg/kg having an arithmetic mean of 106.7 mg/kg and standard
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deviation of 121.8; the highest value among the analysed elements (Table 1).
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The data set for the element concentrations of the soil samples (Table 2) is large; the
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relationships in element distributions were examined by the calculationof Pearson correlation
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coefficients. The Pearson correlation coefficients (rs) for p ≤ 0.01 and p ≤ 0.05 were
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determined as follows: Pb–Zn 0.72, As–Sb 0.71, Au–Ag 0.47, As–Zn 0.43, Au–As 0.40, Au–
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Zn 0.36, As–Pb 0.34, and Ag–Zn 0.31 (Table 2). According to these values, Au concentration
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is closely related to Ag, As and Zn. Therefore these elements are used as pathfinder elements
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for Au in Deliklitaş deposit.
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Results of analysis were evaluated with STATISTICA 1.8 for Windows. Cluster
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analysis clumps the samples separately then joins the closest two clusters, in multiple steps.
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Three groups composed of Ag–Au, Pb–Zn and Sb–As were obtained from the cluster analysis
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(dendrogram) and the relationship between elements weakens from +1 to −1. According to
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this analysis, a stronger group is formed by each pair of Ag–Au, Pb–Zn, and Sb–As with
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higher concentrations. For lower concentrations, Pb–Zn joins to the Ag–Au group and Cu
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joins Sb–As group for low concentrations. The close association of Ag and Au, Pb and Zn and
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Sb and As mean that these elements be considered for future exploration of other Au deposits
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in the area (Fig. 4).
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Factor analysis was done by using SPSS 15.0 to prepare correlation matrix of soil data.
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Eigen values were determined by Kaiser Normalisation and Varimax rotation method, in the
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process the suitability of data size was tested and approved. There are three Eigen values
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greater than 1 for soil samples, thus, the factor number were determined as 3. For soils: Factor
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1 refers to ore minerals of the epithermal system, factor 2 refers to main rock source of Pb and
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Zn and factor 3 refers to the environmental impact (Table 3). This indicates that the spread of
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metals in the main rocks and soil samples is transported physically and by natural
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disintegration. After the rotation, the variance that the 1st factor expresses is 25%, the 2nd
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factor expresses 24% and 3rd factor expresses 22% (Table 3). The Extraction Method was
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used for principal component analysis and Rotation Method was used for Varimax with
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Kaiser normalization. Contour maps of surface metal concentrations provide an effective manner of
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presenting results in contamination studies (Rubio, et al., 2000). During the calculation of the
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areal distribution of elements in Deliklitaş soils by SURFER 9 (Golden Software), 50%, 70%,
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90% and 95% of cumulative data were used for contouring. First, the 50% value is regarded
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as baseline value and 95% value as a strong anomaly (Yaylalı-Abanuz and Tüysüz, 2011).
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The areal distribution of Ag contents show that most samples in the study area contain
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a baseline value of Ag (0.5 mg/kg), but Ag is enriched in the south and east of the study area
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with the anomalous value of 2 mg/kg. Baseline and anomalous values of As were 100 mg/kg
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and 280 mg/kg, respectively. The outer northwest part of the study area shows anomalous As
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values. Baseline values of Au in the soil samples are determined as 0.2 mg/kg. The outer
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north and northwest parts of the study area shows anomalous Au values (Fig. 5).
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In the areal distribution of element plots, Pb and Zn have anomalous values
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everywhere except the central study area. Anomalous values of Pb and Zn in the soil samples
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are determined as 420 mg/kg and 950 mg/kg respectively; the baseline value of Pb is 200
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mg/kg, and the baseline Zn value is 350 mg/kg (Fig. 5).
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The normal (baseline) value of Cu in Deliklitaş area soil samples is approximately 15
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mg/kg, and the maximum value of Cu is 35 mg/kg. The distribution of Cu in Deliklitaş soils
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changes in a narrow zone (Fig. 5).
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Baseline and anomalous values of Sb were 7 mg/kg and 18 mg/kg, respectively. The outer western part of the study area shows anomalous Sb values (Fig. 5). Baseline oncentrations of elements in soils depends on the mineralogical composition
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of the principal material and on the weathering processes that have led to its formation (De
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Temmerman et al., 2003), and on soil particle size, organic matter and clay content (Tume et
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al., 2006). The natural concentration of elements in soil varies, making it inappropriate to use
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universal baseline levels for assessing the extent and risks of trace metal contamination in a
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particular soil type (Horckmans et al., 2005). Therefore, although natural baseline
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concentrations in soil have been investigated in many countries such as Poland (Anderson et
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al., 1994), many countries in Europe (De Vos et al., 2006), China (Chen et al., 1991) and the
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USA (Ma et al., 1997), it is necessary to estimate local baseline concentrations and spatial
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distribution characteristics of elements in soil (Su and Yang, 2008).
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6. Conclusion The characteristics of the Deliklitaş (Balıkesir) gold deposit such as wall-rock,
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alteration types, structural and textural specifications have been investigated. Gold and silver
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are the main ores, however As, Sb, Zn, Pb and Cu also occur in trace amounts in the
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mineralized system. The major alteration types are propylitic and extensive argillic alteration,
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silicification and quartz veining.
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The results of this study show that soil geochemistry is efficient in the exploration for
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mineral deposits. The Au in soil samples collected from the Deliklitaş deposit is closely
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associated with Ag, As, Cu, Sb, Zn and Pb elements. The concentration values of these
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elements have wide ranges, 0.005–0.54 mg/kg Au, 0.03–2.66 mg/kg Ag, 3.4–315 mg/kg As,
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0.15–19.25 mg/kg Sb, 2.5–35 mg/kg Cu, 17.4–545 mg/kg Pb and 14-1240 mg/kg Zn.
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Pearson correlation analysis was performed on all the elements. The level of
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significance (p≤0.05 and p≤0.01) of multielement correlations for soil samples was
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determined. Statistical evaluations and interpretation of data indicate that Au is closely
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associated with Ag and As.
Factor analysis generates three factors that account for 72.81% of all the variances.
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Results show that Factor 1 is responsible for the enrichment of Au, Ag, As, Sb, Pb and Cu;
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Factor 2 is responsible for the enrichment of Pb and Zn and Factor 3 is responsible for the
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enrichment of Ag. Factor 1 reflects the geochemical characteristics of Au mineralization. Zinc
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shows a different behaviour owing to its mobility. Cluster dendrogram analysis shows similar
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element relations. According to this analysis, a stronger group is formed by each pair of Ag
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and Au, Pb and Zn, and Sb and As with higher concentrations.
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Au, Ag, As, Sb, Cu, Pb and Zn show widespread anomalies in the area of
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mineralization.. Au and As are show high anomaly contrasts and strong anomalies. Therefore
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Ag and As can be used as pathfinder elements for exploration of gold deposits near the study
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area.
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Acknowledgements
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G. K. and N. A. would like to express appreciation to GRC Madencilik Ltd., Turkey for their
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generous financial support for the project while working as GRC Exploration Manager.
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References
256
Anderson, S., Odegärd, S., Vogt, R.D., Seip, H.M., 1994. Background levels of heavy metals
257
in Polish forest soils. Ecological Engineering 3, 245–253. Ashley, P.M., Lottermoster, B.G., Collins, J.A., Grant, C.D., 2004. Environmental
259
geochemistry of the derelict Webbs Concols mine, New South, Australia, Environmental
260
Geology, 46, pp. 591-604.
RI PT
258
261
Baumgartner, R., Fontbote, L., Vennemann, T., 2008. Mineral zoning and geochemistry of
262
epithermal polymetallic Zn–Pb–Ag–Cu–Bi mineralization at Cerro de Pasco, Peru. Econ.
263
Geol. 103, 493–537.
Berger, B.R., Henley, R.W., 2011. Magmatic-vapour expansion and the formation of high
265
sulfidation gold deposits: structural controls on hydrothermal alteration and ore
266
mineralization. Ore Geol. Rev. 39, pp. 75–90.
268
Burt, R., Chiaretti, J.V., Prevost, D.J., 2005. Trace element of selected soil in western Nevada
M AN U
267
SC
264
and eastern California. Soil Survey Horizons, 46, pp. 120-131.
269
Carman, G.D., 2003. Geology, mineralization and hydrothermal evolution of the Ladolam
270
gold deposit, Lihir Island, Papua New Guinea. Soc. Econ. Geol. Spec. Publ. 10, pp. 247–
271
284.
Chen, J.S., Wei, F.S., Zheng, C.J., Wu, Y.Y., Adriano, D.C., 1991. Background
273
concentrations of elements in soils of China. Water, Air and Soil Pollution, 57–58, 699–
274
712.
TE D
272
Corbett, G.J., Leach, T.M., 1998. Geothermal environment for southwest Pacific Rim gold–
276
copper systems. In: Corbett, G.J., Leach, T.M. (Eds.), Southwest Pacific Rim Gold-
277
Copper Systems: Structure, Alteration, and Mineralization. Economic Geology Special
278
Publication, 6, pp. 11–30.
280 281 282
Corbett, G.J., 2002. Epithermal gold for explorationists. Australian Institute of Geoscientists
AC C
279
EP
275
News No. 67 (8 pp.).
De Temmerman, L., Vanongeval, L., Boon, W., Hoenig, G., 2003. Heavy metal content of arable soils in northern Belgium. Water, Air and Soil Pollution, 148, 61–73.
283
Demirel, Z., Yıldırım, T., Burçak, M., 2004. Preliminary study on the occurrence of
284
geothermal systems in the tectonic compressional regions: An example from the Derman
285
geothermal field in the Biga Peninsula, Turkey. Journal of Asian Earth Sciences, 22, pp.
286
495–501.
287
De Vos, W., Tarvainen, T., Salminen, R., Reeder, S., De Vivo, B., Demetriades, A., Pirs, S.,
288
Batista, M.J., Marsina, K., Ottesen, R.T., O'Connor, P.J., Bidoves, M., Lima, A., Siewers,
ACCEPTED MANUSCRIPT U., Smith, B., Taylor, H., Shaw, R., Salpeteur, I., Gregorauskiene, V., Halamic, J.,
290
Slaninka, I., Lax, K., Gravesen, P., Birke, M., Breward, N., Ander, E.L., Jordan, G., Duris,
291
M., Klein, P., Locutura, J., Bel-Lan, A., Pasieczan, A., Lis, J., Mazreku, A., Gilucis, A.,
292
Heitzmann, P., Klaver, G., Petersell, V., 2006. Geochemical Atlas of Europe. Part 2.
293
Interpretation of Geochemical Maps, Additional Tables, Figures, Maps, and Related
294
Publications. Geological Survey of Finland, Espoo, 600p. -ISBN 951-690-956-6.)
RI PT
289
295
Dietrich, A., Gutierrez, R., Nelson, E., Layer, P., 2011. Geology of the epithermal Ag–Au
296
Huevos Verdes vein system and San José district, Deseado massif, Patagonia, Argentina.
297
Mineral. Deposita, 1–17.
300 301
Research and Exploration. 107, pp. 119-140. Gustafson, L.B.,
Bulletin of the Mineral
SC
299
Ercan, T., 1986. Cainozoic volcanism in the Central Anatolia.
Hunt, J.P., 1975. The porphyry copper deposit at El Salvador, Chile:
Economic Geology, v. 70, pp.. 857–912.
M AN U
298
302
Fernández, R.R., Blesa, A., Moreira, P., Echeveste, H., Mykietiuk, K., Andrada de Palomera,
303
P., Tessone, M., 2008. Los depósitos de oro y plata vinculados al magmatismo jurásico de
304
la Patagonia: revisión y perspectivas para la exploración. Rev. Assoc. Geol. Argent. 63,
305
665–681.
Hayba, D.O., Bethke, P.M., Heald, P., Foley, N.K., 1985. Geologic, mineralogic, and
307
geochemical characteristics of volcanic-hosted epithermal precious-metal deposits. In:
308
Berger, B.R., Bethke, P.M. (Eds.), Geology and Geochemistry of Epithermal Systems.
309
Reviews in Economic Geology, 2, pp. 129–168.
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306
Henderson, R.D., 2009. Fruta del Norte Project Ecuador NI 43-101 Technical Report. p. 135
311
Hedenquist, J.W., 1987. Mineralization associated with volcanic-related hydrothermal
312
systems in the circum-Pacific basin. In: Horn, M.K. (Ed.), The 4th Circum-Pacific Energy
313
and Mineral Resources Conference, Singapore, Transactions. American Association of
314
Petroleum Geologists, pp. 513–524.
316 317 318
AC C
315
EP
310
Hedenquist, J.W., Arribas, A., Gonzalez-Urien, E., 2000. Exploration for epithermal gold deposits. Soc. Econ. Geol. Rev. 13, 245–277. Hedenquist, J.W., Izawa, E., Arribas, A., White, N.C., 1996. Epithermal gold deposits: styles, characteristics, exploration. Resour. Geol. Spec. Publ. 1, 18.
319
Hedenquist, J.W., White, N.C., Siddeley, G. (Eds.), 1990. Epithermal gold mineralization of
320
the Circum-Pacific—geology, geochemistry, origin and exploration. Journal of
321
Geochemical Exploration Special Issue, vols. I and II (447 pp. and 474 pp.).
ACCEPTED MANUSCRIPT 322
Henley, R.W., Berger, B.R., 2011. Magmatic-vapour expansion and the formation of high
323
sulfidation gold deposits: chemical controls on alteration and mineralization. Ore Geol.
324
Rev. 39, 63–74. Horckmans, L., Swennen, R., Deckers, J., Maquil, R., 2005. Local background concentrations
326
of trace elements in soils: a case study in the Grand Ducky of Luxembourg. Catena 59,
327
279–304.
RI PT
325
328
John, D.A., 2001. Miocene and early Pliocene epithermal gold–silver deposits in the northern
329
Great Basin, western USA: characteristics, distribution, and relationship to magmatism.
330
Economic Geology 96, 1827–1853.
332
Krushensky, R.D., 1976. Neogene calc-alkaline extrusive and intrusive rocks of the Karalar–
SC
331
Yeşiller area, northwest Anatolia, Turkey. Bulletin of Volcanology 40, 336–360. Lee, G., Koh, S., Pirajno, F., 2014. Evolution of hydrothermal fluids of HS and LS type
334
epithermal Au–Ag deposits in the Seongsan hydrothermal system of the Cretaceous
335
Haenam volcanic field, South Korea. Ore Geology Reviews, Volume 61, Pages 33–51.
336
Lesage, G., 2011. Geochronology, Petrography, Geochemical Constraints, and Fluid
337
Characterization of the Buriticá Gold Deposit, Antioquia Department, Colombia, Masters
338
Abstracts International.
M AN U
333
Lisowiec, N., Halley, S.H., Ryan, L., 2007. Using Deposit-scale Alteration and Geochemical
340
Signatures to Explore for Analogue Deposits: a Case Study From the Mt Wright Gold
341
Project, Queensland. Geochemical Case Histories & Geochemical Exploration Methods.
342
p. 969-972.
345 346
EP
344
Ma, L.Q., Tan, F., Harris, W., 1997. Concentrations and distributions of eleven metals in Florida soils. Journal of Environmental Quality 26, 769–775. MTA, 2002. Geological map of Turkey, scale 1:500.000. General Directorate of Mineral Research and Exploration (MTA), Ankara.
AC C
343
TE D
339
347
Pendias, A., 2001. Trace elements in soils and plants. Third Edition, CRC Press, NY.
348
Rubio, B., Nombela, M.A., Vilas, F., 2000. Geochemistry of major and trace elements in
349
sediments of the Ria de Vigo (NW Spain): an assessment of metal pollution. Marine
350
Pollution Bulletin 40, 968-980.
351
Sherlock, R.L., 2005. The relationship between the McLaughlin gold–mercury deposit and
352
active hydrothermal systems in the Geysers–Clear Lake area, northern Coast Ranges,
353
California. Ore Geol. Rev. 26, 349–382.
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Simon, G., Kesler, S.E., Russell, N., Hall, C.M., Bell, D., Pinero, E., 1999. Epithermal gold
355
mineralization in an old volcanic arc: the Jacinto deposit, Camaguey district, Cuba.
356
Economic Geology 94, 487–506. Sillitoe, R.H., 2010. Porphyry copper systems. Econ. Geol. 105, 3–41.
358
Sillitoe, R.H., Hedenquist, J.W., 2003. Linkages between volcano tectonic settings, ore-fluid
359
compositions, and epithermal precious metal deposits. In: Simmons, S.F., Graham, I.
360
(Eds.), Volcanic, Geothermal, and Ore-Forming Fluids: Rulers and Witnesses of Processes
361
Within the Earth. Special Publication–Society of Economic Geologists 10, pp. 315–343.
362
Simmons, S.F., Brown, K.L., 2006. Gold in magmatic hydrothermal solutions and the rapid formation of a giant ore deposit. Science 314, 288–291.
SC
363
RI PT
357
Simmons, S.F., White, N.C., John, D.A., 2005. Geologic characteristics of epithermal
365
precious and base metal deposits. Economic Geology 100th Anniversary Volume, pp.
366
485–522.
M AN U
364
367
Sposito, G., 1989. The chemistry of soils, New York, Oxford University Press.
368
Su, Y., Yang, R., 2008. Background concentrations of elements in surface soils and their
369
changes as affected by agriculture use in the desert-oasis ecotone in the middle of Heihe
370
River Basin, North-west China. Journal of Geochemical Exploration 98, 57–64. Tassinari, C.C.G., Pinzon, F.D., Buena Ventura, J., 2008. Age and sources of gold
372
mineralization in the Marmato mining district, NW Colombia: a Miocene–Pliocene
373
epizonal gold deposit. Ore Geol. Rev. 33, 505–518.
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Taylor, B.E., 2007. Epithermal gold deposits, in Goodfellow, W.D., ed., Mineral Deposits of
375
Canada: A Synthesis of Major Deposit-Types, District Metallogeny, the Evolution of
376
Geological Provinces, and Exploration Methods: Geological Association of Canada,
377
Mineral Deposits Division, Special Publication No. 5, p. 113-139.
EP
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Tume, P., Bech, J., Longan, L., Tume, L., Reverter, F., Sepulveda, B., 2006. Trace elements
379
in natural surface soils in Sant Climent (Catalonia, Spain). Ecological Engineering 27,
380
145–152.
AC C
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381
Warren, I., Simmons, S.F., Mauk, J.L., 2007. Whole-rock geochemical techniques for
382
evaluating hydrothermal alteration, mass changes, and compositional gradients associated
383
with epithermal Au–Ag mineralization. Econ. Geol. 102 (5), 923–948.
384
Warren, I., Zuluaga, J.I., Robbins, C.H., Wulftange, W.H., Simmons, S.F., 2004. Geology and
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geochemistry of epithermal Au–Ag mineralization in the El Peñón district, northern Chile.
386
In: Sillitoe, R.H., Perello, J., Vidal, C.E. (Eds.), Andean Metallogeny: New Discoveries,
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Concepts, and Updates. Society of Economic Geologists Special Publication 11, pp. 113–
388
139.
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Wilson, M.A., Burt, R., Indorante, S.J., Jenkins, A.B., Chiaretti, J.V., Ulmer, M.G., Scheyer,
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J.M., 2008. Geochemistry in the modern soil survey program, Environ Monit Assess. 139,
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151-171. Yaylalı-Abanuz, G., Tüysüz, N., 2011. Statistical evaluation of the geochemical data from
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Akoluk epithermal gold area (Ulubey–Ordu), NE Turkey. Geochemical Journal, Vol. 45,
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pp. 209 to 219.
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Zhai, W., Sun, X., Sun, W., Su, L., He, X., Wu, Y., 2009. Geology, geochemistry, and genesis
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of Axi: A Paleozoic low-sulfidation type epithermal gold deposit in Xinjiang, China. Ore
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Geology Reviews 36, 265–281
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ACCEPTED MANUSCRIPT Table 1 Descriptive statistics for geochemical data of 183 soil samples. Maximum Minimum Arithmetic Mean Standard Deviation Medium
Au 0.54 0.0005
Ag 2.66 0.03
As 315 3.4
Sb 19.25 0.15
Cu 35 2.5
Pb 545 17.4
Zn 1240 14
0.04
0.22
30.3
1.62
11.7
73.8
107
0.07 0.01
0.28 0.10
35.3 19.7
1.85 1.18
5.4 11.2
79.5 51.2
122 69
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Table 2 Correlation coefficients for elements in the soil samples. Au
As
Sb
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Rotation Sums of Squared Loadings Cumulative % of Cumulative % of Variance % Total Variance %
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2.81 40.15 40.15 1.78 25.39 1 1.30 18.64 58.79 1.73 24.72 2 0.98 14.02 72.81 1.59 22.70 3 0.87 12.41 85.22 4 0.54 7.65 92.87 5 0.29 4.12 96.99 6 Extraction Method: Principal Component Analysis.
Au Ag As Sb Cu Pb Zn 426
Zn
Table 3 Factor loading in soils of Deliklitaş. Component Initial Eigenvalues
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Pb
1 0.47** 1 0.40** 0.20** 1 0.15* 0.10 0.71** 1 0.05 0.03 0.17* 0.27** 1 0.26** 0.26** 0.34** 0.23** 0.10 1 0.36** 0.31** 0.43** 0.22** 0.12 0.72** Correlation is significant at the 0.01 level (2-tailed). Correlation is significant at the 0.05 level (2-tailed).
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Cu
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Ag
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Component Factor 1 Factor 2 0.13 0.16 −0.04 0.16 0.78 0.23 0.89 0.07 0.56 0.08 0.13 0.92 0.16 0.88
Factor 3 0.83 0.82 0.35 0.12 −0.15 0.12 0.24
25.39 50.11 72.81
1
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427 Fig. 1. Location map of the study area
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Deliklitaş
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Yaylak H.
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436 437 438 439
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Eyrek H.
Kocaçayır Location
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Fig. 2. Geological and location map of the Deliklitaş Au deposit and surrounding area,
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showing soil sample locations.
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Fig. 3. Simplified geologic map of the main lithotectonic/stratigraphic units in the region.
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Note the study area is located at the southern end of a widely exposed alteration zone (MTA,
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2002).
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Ag Au
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Zn Pb Sb As
Cu
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Fig. 4. Dendrogram showing element groups in soil samples on which cluster analysis was
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applied.
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Fig. 5. Contour diagrams showing Au, As, Sb, Ag, Zn, Pb and Cu distributions in soil
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samples.
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ACCEPTED MANUSCRIPT Highlights (revision) The major alteration types are propylithic, extensive argillic and silicification
•
Deliklitaş Au deposit is closely associated with Ag, As, Cu, Sb, Zn and Pb elements
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Statistical evaluations indicate that Au is closely associated with Ag and As.
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Factor analysis account for 72.81% of the total variances.
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Au, Ag, As, Sb, Cu, Pb and Zn show widespread anomalies in the mineralization area
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S1464-343X(16)30152-2
DOI:
10.1016/j.jafrearsci.2016.05.006
Reference:
AES 2565
To appear in:
Journal of African Earth Sciences
Received Date: 20 January 2015 Revised Date:
19 April 2016
Accepted Date: 7 May 2016
Please cite this article as: Kirat, G., Aydin, N., Areal distributions and geochemical properties of soils surrounding the Deliklitaş Au deposit, Turkey, Journal of African Earth Sciences (2016), doi: 10.1016/ j.jafrearsci.2016.05.006. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.
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Güllü KIRAT1*, Nasuh AYDIN2
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Geochemical properties of soils surrounding the Deliklitaş Au deposit, Turkey
3 4 5
1
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([email protected])
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Phone: (+90)354 2421001/7921, Fax: (+90)354 2421005
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2
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Engineering ([email protected])
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Bozok University, Faculty of Architecture and Engineering, Department of Geological Engineering
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Balıkesir University, Faculty of Architecture and Engineering, Department of Geological
* Corresponding author
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ABSTRACT
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The Deliklitaş gold deposit is in northwest Turkey, where a renowned gold province
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containing many major hydrothermal deposits related to Tertiary volcanic rocks. Because of
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the limited outcrops in the region, one of the most effective ways to prospect for new deposits
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is soil sampling. In this study, 183 soil samples were systematically collected from the area
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around the Deliklitaş Au deposit. Metal content of the samples, and their relationships and
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distribution according to distance away from the ore body were statistically investigated. The
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analysis of metals and metalloids in soil samples yielded the following metal ranges: Au from
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0.005 to0.54 mg/kg (average 0.04); Ag from 0.03 to2.66 (average 0.22); As from 3.4 to315
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(average 30.3); Sb from 0.15 to19.25 (average 1.62); Cu from 2.5 to35 (average 11.73); Pb
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from 17.4 to545 (average 73.76) and from Zn 14 to1240 mg/kg of soil (average 106.71). For
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the areal distribution of metals 50%, 70%, 90% and 95% of the cumulative data were used for
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contouring element contents in the soils, using 50% as the baseline value and 95% as the
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anomalous value. Eigen values, Varimax Rotation method with Kaiser Normalization tested
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and determined the suitability of the number of data sets. Factor numbers were determined as
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3, according to Eigen values determined for the soil samples. Factor 1 refers to ore minerals
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of epithermal system, Factor 2 refers to main rock sources of Pb and Zn and Factor 3 refers to
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environmental effects. Ag–Au, Pb–Zn and Sb–As pairs show high correlation in the cluster
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analysis indicating element relations. Please add an overarching sentence here, on
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implications etc.
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Key Words: Epithermal, Soil, Pearson correlations, Eigen value.
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1. Introduction The Deliklitaş Au deposit is approximately 23 km northwest of Balikesir city in
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western Turkey (Fig. 1). The western and northern parts of the area are topographically
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elevated, but the southeastern portion has a flat topography. Some highest peaks in the area
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are: Yaylak Hill and Eyrek Hill (Fig. 2). The elevated parts of the Deliklitaş area consist of
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altered andesites cut by hydrothermal quartz veins.
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The northwestern part of Turkey is a well-known gold province containing many
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hydrothermal Au deposits related to Tertiary volcano-plutonic systems. Epithermal gold
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deposits are economically and the most important types of gold deposits in the region where
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several operating gold mines such as Efemçukuru, Kızıltepe–Kepez, Ovacık and Küçükdere
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(Balıkesir region) occur. Epithermal Au (± Ag) deposits include quartz veins and
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disseminated types near the Earth’s surface (≤1.5 km) in volcanic, sedimentary, and
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metamorphic rocks. The deposits commonly occur in association with hot springs frequently
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in young volcanic centres. The ores are dominated principally by precious metals (Au, Ag),
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but some deposits also contain variable amounts of base metals such as Cu, Pb, and Zn
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(Taylor, 2007).
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Volcanogenic epithermal Au–Ag deposits commonly occur in the Circum-Pacific
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orogenic belt associated with magmatic arcs ranging in age from Cretaceous to Recent
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(Corbett and Leach, 1998; Hedenquist et al., 1990). Epithermal systems form at shallower
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crustal levels than porphyry type deposits (Corbett, 2002). Low-sulfidation epithermal
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deposits are dominated by adularia – sericite alteration and low sulphur Au–Ag
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mineralization. The former is originated by acidic hypogene fluids while the latter is formed
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by neutral reduced fluids (Berger and Henley, 2011; Hedenquist, 1987; Hedenquist et al.,
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1996; Henley and Berger, 2011). Examples of Low-sulfidation epithermal deposits include
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Baguio (Philippines), Cripple Creek (USA), Creede (USA), Round Mountain (USA),
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McLaughlin (USA), Hishikari (Japan), Kelian (Indonesia), Ladolam and Porgera (Papua New
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Guinea) (Carman, 2003; Sherlock, 2005). The origins of low-sulfidation type of ore deposits
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are explained by various genetic models (Corbett, 2002; Hedenquist et al., 2000; Simmons et
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al., 2005). The low-sulfidation type ore deposits originate either from reduced or neutral
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diluted fluids caused by deep circulating meteoric fluid systems mixed with magmatic water
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characterized by sulphur reduced to H2S (Corbett and Leach, 1998; Hayba et al., 1985).
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Depending on the mixing rate of hydrothermal fluids and meteoric water at shallow depths,
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different types of alteration or Au ore bodies are produced (Lee et al., 2014) Most epithermal gold deposits hosted in Mesozoic–Cainozoic sub aerial volcanic
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rocks formed at shallow depths include those in the USA (John, 2001), Jacinto in Cuba
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(Simon et al., 1999), the Hishikari and Nansatsu epithermal deposits in Japan, Golden Cross
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in New Zealand, Chinkuashih in Taiwan, Zijinshan and Bitian in Fujian, China (Simmons and
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Brown, 2006) (Zhai et al., 2009).
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Andean type low-sulfidation epithermal deposits are small. Large Andean type
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deposits include the Jurassic Fruta del Norte deposit in Ecuador (Henderson, 2009), and the
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Palaeocene El Peñón deposit of northern Chile (Warren et al., 2004, 2007). The Late Jurassic
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to Early Cretaceous deposits of the Deseado and Patagonian Massifs (Dietrich et al., 2011;
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Fernández et al., 2008) also fall in this system. The low-sulfidation deposits mentioned above
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occur at elevations below 2400 m.a.s.l., in predominantly in rhyolitic volcanic and
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volcaniclastic rocks, lack spatial and temporal association with porphyry systems (Sillitoe,
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2010) occurring in extensional tectonic settings without associated contractional deformation
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and surface uplift during mineralization. However, there are also examples of epithermal
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deposits containing low-sulfidation mineralization that occur in larger magmatic-
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hydrothermal systems in arc segments also containing porphyry style or high-sulfidation
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epithermal mineralization. Examples of these deposits include Cerro de Pasco (Peru:
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Baumgartner et al., 2008), Marmato and Buriticá (Colombia: Tassinari et al., 2008; Lesage,
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2011), all Mid to Late Miocene in age. The low-sulfidation nature of epithermal deposits in
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some compressional arc settings attributed to more reactive, locally reducing host or basement
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rock characteristics (e.g., The Marmato epithermal gold deposits: Tassinari et al., 2008). Thus,
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as shown earlier (Sillitoe and Hedenquist, 2003) low-sulfidation deposits are associated with
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overall compressional arc and extensional rift settings.
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The occurrence together of Ag, As, Au, Cu, Pb, Zn and Sb in soils near epithermal
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deposits is related to the primary sulphide minerals. The metals and non-metals are partly
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concentrated in the residual sulphide minerals, in soil and river sediments and by clinging to
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jarosite-type phases, anglesite, scorodite, dissolved sulphates, clay minerals and Fe3+
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hydroxides (Ashley, et al., 2004). The mobilities of Cu and Zn are effective in this
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environment. Cu is absorbed by carbonates, clays, oxides and organic matter (Pendias, 2001).
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Pb forms soluble complex ions with sulphates, bicarbonates and carbonates (Sposito, 1989).
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Zn is absorbed by clay minerals, oxides and organic matter, or might translocate by ion
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exchange (Wilson et al., 2008).
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Some workers have investigated and modelled the trace element change in soils near
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Au deposits their results indicate that the lower soil zone is more significant than the upper soil zone (Burt, et al., 2005, Wilson, et al., 2008).
In this study, the geological and
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geochemical properties of soils collected around the Deliklitaş Au deposit were studied and
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statistically analysed show that Au is closely associated with Ag and As.
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2. Geology
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The main lithotectonic/stratigraphic units in the study area include Late Oligocene-
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Early Miocene volcanic rocks (Hallaçlar volcanic rocks) and Quaternary alluvium (Fig. 2 and
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3).
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2.1. Hallaçlar Volcanic Rocks
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The Hallaçlar volcanic rocks (Fig. 2 and 3) (400 m thick) are composed of white to
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dirty yellow, red and brown coloured andesitic to dacitic rocks, lava flows, silicified rocks,
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and their alteration products. The andesite and dacites are strongly affected by hydrothermal
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alteration in the Deliklitaş area, typically resulting in extensive alteration and silicification.
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Altered volcanic rocks are further subdivided into: slightly altered volcanic rocks, a
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moderately to weakly argillaceous zone and a silicified zone. The lava flows are characterised
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by plagioclase, biotite, clinopyroxene, feldspar, and some opaque phenocrysts found in a fine-
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grained plagioclase- and clinopyroxene-rich matrix.
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The age of the Hallaçlar volcanic unit is Upper Oligocene–Early Miocene
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(Krushensky, 1976). The upper parts of the Hallaçlar volcanic units are silicified, kaolinitized
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and affected by pyrite mineralisation (Demirel, et al., 2004). Petrographic study of the lavas
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of the Hallaçlar volcanic unit indicates that the lavas have a matrix of volcanic vitreous
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matter with plagioclase and biotite microliths containing oligoclase and andesine type
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plagioclases, hornblende, biotite, augite and rare quartz phenocrysts; and the lavas are locally
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silicified (Ercan, 1986).
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Hallaçlar volcanic rocks are overlain discordantly by the lava flows and tuffs of a
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younger volcanic phase in the study area. Despite that these lavas and tuffs were already
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known from outcrops exposed around Pelit village, it was found during this study that these
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rocks outcrop widely to the east of the study area and are here called “Dedetepe Formation”
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after Krushensky (1976) who first described these rocks in this area. The lavas of the
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Dedetepe Formation are more acidic than those of the Hallaçlar volcanic rocks and are made
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of dacite, rhyodacite and rhyolites. The lavas are of various colours, weathered in some places
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and locally silicified. The tuffs are predominant in the formation and they usually display
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horizontal layering. Agglomerate intercalations are observed locally (Ercan, 1986).
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2.2. Alluvium In Deliklitaş area, the alluvium contains unconsolidated pebbles, sand, silt and muds,
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deposited along the present-day drainage system and formed the basin fill of the tectonically
135
active Ovacık basin. The initial opening of the Ovacık basin was directly controlled by a pull-
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apart along a step over between the right-lateral Turplu Fault and the Ovacık Fault (Fig. 3).
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3. Hydrothermal alteration
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All the mineral deposits near the study area are related to volcanic hydrothermal
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systems. Hydrothermal solutions destroyed the original textures of the volcanic rocks. Deposit
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types are commonly epithermal and porphyry style mineralizations. NW–SE to E–W-trending
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phreatic breccias are important in the Deliklitaş region. Massive silicification, vuggy quartz,
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late-stage blanket-like chalcedonic and opaline quartz, argillic alteration characterises the
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alteration halos of the deposit. The intense hydrothermal alteration is contemporaneous with
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extensional and strike-slip faulting. In the Deliklitaş deposit, porphyritic dikes are usually
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altered; this alteration zonation matches the propylitic alteration zonation described by
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Gustafson and Hunt (1975).
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4. Materials and methods
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One hundred and Eighty-three (183) soil samples were collected in the study area (Fig.
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2). Samples e of about 1-1.5 kg were collected at 25-30 cm depth using hammer. All the
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samples were placed in plastic bags, were sieved through a -200 mesh Sieve after drying at
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60oC.
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The samples were analysed at ALS Chemex Laboratory, Canada by the Au-AA24
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method for Au and the Me-MS61 method for multielements (after extracted using microwave
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digestion system) using ICP-MS (Inductively Coupled Plasma-Mass spectrometry) (Lisowiec
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et. al., 2007).
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5. Results and Discussion
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The maximum, minimum, standard deviation and arithmetic mean values of metal and
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metalloid concentrations in the 183 soil samples are shown in Table 1. The soils contain
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0.005–0.54 mg/kg Au having an arithmetic mean value of 0.04 mg/kg. The concentration
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values for Ag in these samples are 0.03 to2.66 mg/kg and the arithmetic mean is 0.22 mg/kg. The concentration values of some elements have wide ranges, for instance; As ranges
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from 3.4 to 315 mg/kg (median 19.7), Sb from 0.15 to 9.25 mg/kg (median 1.18), Cu from 2.5
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to 5 mg/kg (median 11.2), and Pb from 17.4 to 545 mg/kg (median 51.2). Zn values are
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between 14 and 1240 mg/kg having an arithmetic mean of 106.7 mg/kg and standard
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deviation of 121.8; the highest value among the analysed elements (Table 1).
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The data set for the element concentrations of the soil samples (Table 2) is large; the
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relationships in element distributions were examined by the calculationof Pearson correlation
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coefficients. The Pearson correlation coefficients (rs) for p ≤ 0.01 and p ≤ 0.05 were
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determined as follows: Pb–Zn 0.72, As–Sb 0.71, Au–Ag 0.47, As–Zn 0.43, Au–As 0.40, Au–
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Zn 0.36, As–Pb 0.34, and Ag–Zn 0.31 (Table 2). According to these values, Au concentration
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is closely related to Ag, As and Zn. Therefore these elements are used as pathfinder elements
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for Au in Deliklitaş deposit.
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Results of analysis were evaluated with STATISTICA 1.8 for Windows. Cluster
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analysis clumps the samples separately then joins the closest two clusters, in multiple steps.
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Three groups composed of Ag–Au, Pb–Zn and Sb–As were obtained from the cluster analysis
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(dendrogram) and the relationship between elements weakens from +1 to −1. According to
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this analysis, a stronger group is formed by each pair of Ag–Au, Pb–Zn, and Sb–As with
178
higher concentrations. For lower concentrations, Pb–Zn joins to the Ag–Au group and Cu
179
joins Sb–As group for low concentrations. The close association of Ag and Au, Pb and Zn and
180
Sb and As mean that these elements be considered for future exploration of other Au deposits
181
in the area (Fig. 4).
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Factor analysis was done by using SPSS 15.0 to prepare correlation matrix of soil data.
183
Eigen values were determined by Kaiser Normalisation and Varimax rotation method, in the
184
process the suitability of data size was tested and approved. There are three Eigen values
185
greater than 1 for soil samples, thus, the factor number were determined as 3. For soils: Factor
186
1 refers to ore minerals of the epithermal system, factor 2 refers to main rock source of Pb and
187
Zn and factor 3 refers to the environmental impact (Table 3). This indicates that the spread of
188
metals in the main rocks and soil samples is transported physically and by natural
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disintegration. After the rotation, the variance that the 1st factor expresses is 25%, the 2nd
190
factor expresses 24% and 3rd factor expresses 22% (Table 3). The Extraction Method was
191
used for principal component analysis and Rotation Method was used for Varimax with
192
Kaiser normalization. Contour maps of surface metal concentrations provide an effective manner of
194
presenting results in contamination studies (Rubio, et al., 2000). During the calculation of the
195
areal distribution of elements in Deliklitaş soils by SURFER 9 (Golden Software), 50%, 70%,
196
90% and 95% of cumulative data were used for contouring. First, the 50% value is regarded
197
as baseline value and 95% value as a strong anomaly (Yaylalı-Abanuz and Tüysüz, 2011).
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The areal distribution of Ag contents show that most samples in the study area contain
199
a baseline value of Ag (0.5 mg/kg), but Ag is enriched in the south and east of the study area
200
with the anomalous value of 2 mg/kg. Baseline and anomalous values of As were 100 mg/kg
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and 280 mg/kg, respectively. The outer northwest part of the study area shows anomalous As
202
values. Baseline values of Au in the soil samples are determined as 0.2 mg/kg. The outer
203
north and northwest parts of the study area shows anomalous Au values (Fig. 5).
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In the areal distribution of element plots, Pb and Zn have anomalous values
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everywhere except the central study area. Anomalous values of Pb and Zn in the soil samples
206
are determined as 420 mg/kg and 950 mg/kg respectively; the baseline value of Pb is 200
207
mg/kg, and the baseline Zn value is 350 mg/kg (Fig. 5).
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The normal (baseline) value of Cu in Deliklitaş area soil samples is approximately 15
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mg/kg, and the maximum value of Cu is 35 mg/kg. The distribution of Cu in Deliklitaş soils
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changes in a narrow zone (Fig. 5).
212 213
Baseline and anomalous values of Sb were 7 mg/kg and 18 mg/kg, respectively. The outer western part of the study area shows anomalous Sb values (Fig. 5). Baseline oncentrations of elements in soils depends on the mineralogical composition
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of the principal material and on the weathering processes that have led to its formation (De
215
Temmerman et al., 2003), and on soil particle size, organic matter and clay content (Tume et
216
al., 2006). The natural concentration of elements in soil varies, making it inappropriate to use
217
universal baseline levels for assessing the extent and risks of trace metal contamination in a
218
particular soil type (Horckmans et al., 2005). Therefore, although natural baseline
219
concentrations in soil have been investigated in many countries such as Poland (Anderson et
220
al., 1994), many countries in Europe (De Vos et al., 2006), China (Chen et al., 1991) and the
221
USA (Ma et al., 1997), it is necessary to estimate local baseline concentrations and spatial
222
distribution characteristics of elements in soil (Su and Yang, 2008).
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6. Conclusion The characteristics of the Deliklitaş (Balıkesir) gold deposit such as wall-rock,
225
alteration types, structural and textural specifications have been investigated. Gold and silver
226
are the main ores, however As, Sb, Zn, Pb and Cu also occur in trace amounts in the
227
mineralized system. The major alteration types are propylitic and extensive argillic alteration,
228
silicification and quartz veining.
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The results of this study show that soil geochemistry is efficient in the exploration for
230
mineral deposits. The Au in soil samples collected from the Deliklitaş deposit is closely
231
associated with Ag, As, Cu, Sb, Zn and Pb elements. The concentration values of these
232
elements have wide ranges, 0.005–0.54 mg/kg Au, 0.03–2.66 mg/kg Ag, 3.4–315 mg/kg As,
233
0.15–19.25 mg/kg Sb, 2.5–35 mg/kg Cu, 17.4–545 mg/kg Pb and 14-1240 mg/kg Zn.
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Pearson correlation analysis was performed on all the elements. The level of
235
significance (p≤0.05 and p≤0.01) of multielement correlations for soil samples was
236
determined. Statistical evaluations and interpretation of data indicate that Au is closely
237
associated with Ag and As.
Factor analysis generates three factors that account for 72.81% of all the variances.
239
Results show that Factor 1 is responsible for the enrichment of Au, Ag, As, Sb, Pb and Cu;
240
Factor 2 is responsible for the enrichment of Pb and Zn and Factor 3 is responsible for the
241
enrichment of Ag. Factor 1 reflects the geochemical characteristics of Au mineralization. Zinc
242
shows a different behaviour owing to its mobility. Cluster dendrogram analysis shows similar
243
element relations. According to this analysis, a stronger group is formed by each pair of Ag
244
and Au, Pb and Zn, and Sb and As with higher concentrations.
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Au, Ag, As, Sb, Cu, Pb and Zn show widespread anomalies in the area of
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mineralization.. Au and As are show high anomaly contrasts and strong anomalies. Therefore
247
Ag and As can be used as pathfinder elements for exploration of gold deposits near the study
248
area.
249 250
Acknowledgements
251
G. K. and N. A. would like to express appreciation to GRC Madencilik Ltd., Turkey for their
252
generous financial support for the project while working as GRC Exploration Manager.
253 254
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References
256
Anderson, S., Odegärd, S., Vogt, R.D., Seip, H.M., 1994. Background levels of heavy metals
257
in Polish forest soils. Ecological Engineering 3, 245–253. Ashley, P.M., Lottermoster, B.G., Collins, J.A., Grant, C.D., 2004. Environmental
259
geochemistry of the derelict Webbs Concols mine, New South, Australia, Environmental
260
Geology, 46, pp. 591-604.
RI PT
258
261
Baumgartner, R., Fontbote, L., Vennemann, T., 2008. Mineral zoning and geochemistry of
262
epithermal polymetallic Zn–Pb–Ag–Cu–Bi mineralization at Cerro de Pasco, Peru. Econ.
263
Geol. 103, 493–537.
Berger, B.R., Henley, R.W., 2011. Magmatic-vapour expansion and the formation of high
265
sulfidation gold deposits: structural controls on hydrothermal alteration and ore
266
mineralization. Ore Geol. Rev. 39, pp. 75–90.
268
Burt, R., Chiaretti, J.V., Prevost, D.J., 2005. Trace element of selected soil in western Nevada
M AN U
267
SC
264
and eastern California. Soil Survey Horizons, 46, pp. 120-131.
269
Carman, G.D., 2003. Geology, mineralization and hydrothermal evolution of the Ladolam
270
gold deposit, Lihir Island, Papua New Guinea. Soc. Econ. Geol. Spec. Publ. 10, pp. 247–
271
284.
Chen, J.S., Wei, F.S., Zheng, C.J., Wu, Y.Y., Adriano, D.C., 1991. Background
273
concentrations of elements in soils of China. Water, Air and Soil Pollution, 57–58, 699–
274
712.
TE D
272
Corbett, G.J., Leach, T.M., 1998. Geothermal environment for southwest Pacific Rim gold–
276
copper systems. In: Corbett, G.J., Leach, T.M. (Eds.), Southwest Pacific Rim Gold-
277
Copper Systems: Structure, Alteration, and Mineralization. Economic Geology Special
278
Publication, 6, pp. 11–30.
280 281 282
Corbett, G.J., 2002. Epithermal gold for explorationists. Australian Institute of Geoscientists
AC C
279
EP
275
News No. 67 (8 pp.).
De Temmerman, L., Vanongeval, L., Boon, W., Hoenig, G., 2003. Heavy metal content of arable soils in northern Belgium. Water, Air and Soil Pollution, 148, 61–73.
283
Demirel, Z., Yıldırım, T., Burçak, M., 2004. Preliminary study on the occurrence of
284
geothermal systems in the tectonic compressional regions: An example from the Derman
285
geothermal field in the Biga Peninsula, Turkey. Journal of Asian Earth Sciences, 22, pp.
286
495–501.
287
De Vos, W., Tarvainen, T., Salminen, R., Reeder, S., De Vivo, B., Demetriades, A., Pirs, S.,
288
Batista, M.J., Marsina, K., Ottesen, R.T., O'Connor, P.J., Bidoves, M., Lima, A., Siewers,
ACCEPTED MANUSCRIPT U., Smith, B., Taylor, H., Shaw, R., Salpeteur, I., Gregorauskiene, V., Halamic, J.,
290
Slaninka, I., Lax, K., Gravesen, P., Birke, M., Breward, N., Ander, E.L., Jordan, G., Duris,
291
M., Klein, P., Locutura, J., Bel-Lan, A., Pasieczan, A., Lis, J., Mazreku, A., Gilucis, A.,
292
Heitzmann, P., Klaver, G., Petersell, V., 2006. Geochemical Atlas of Europe. Part 2.
293
Interpretation of Geochemical Maps, Additional Tables, Figures, Maps, and Related
294
Publications. Geological Survey of Finland, Espoo, 600p. -ISBN 951-690-956-6.)
RI PT
289
295
Dietrich, A., Gutierrez, R., Nelson, E., Layer, P., 2011. Geology of the epithermal Ag–Au
296
Huevos Verdes vein system and San José district, Deseado massif, Patagonia, Argentina.
297
Mineral. Deposita, 1–17.
300 301
Research and Exploration. 107, pp. 119-140. Gustafson, L.B.,
Bulletin of the Mineral
SC
299
Ercan, T., 1986. Cainozoic volcanism in the Central Anatolia.
Hunt, J.P., 1975. The porphyry copper deposit at El Salvador, Chile:
Economic Geology, v. 70, pp.. 857–912.
M AN U
298
302
Fernández, R.R., Blesa, A., Moreira, P., Echeveste, H., Mykietiuk, K., Andrada de Palomera,
303
P., Tessone, M., 2008. Los depósitos de oro y plata vinculados al magmatismo jurásico de
304
la Patagonia: revisión y perspectivas para la exploración. Rev. Assoc. Geol. Argent. 63,
305
665–681.
Hayba, D.O., Bethke, P.M., Heald, P., Foley, N.K., 1985. Geologic, mineralogic, and
307
geochemical characteristics of volcanic-hosted epithermal precious-metal deposits. In:
308
Berger, B.R., Bethke, P.M. (Eds.), Geology and Geochemistry of Epithermal Systems.
309
Reviews in Economic Geology, 2, pp. 129–168.
TE D
306
Henderson, R.D., 2009. Fruta del Norte Project Ecuador NI 43-101 Technical Report. p. 135
311
Hedenquist, J.W., 1987. Mineralization associated with volcanic-related hydrothermal
312
systems in the circum-Pacific basin. In: Horn, M.K. (Ed.), The 4th Circum-Pacific Energy
313
and Mineral Resources Conference, Singapore, Transactions. American Association of
314
Petroleum Geologists, pp. 513–524.
316 317 318
AC C
315
EP
310
Hedenquist, J.W., Arribas, A., Gonzalez-Urien, E., 2000. Exploration for epithermal gold deposits. Soc. Econ. Geol. Rev. 13, 245–277. Hedenquist, J.W., Izawa, E., Arribas, A., White, N.C., 1996. Epithermal gold deposits: styles, characteristics, exploration. Resour. Geol. Spec. Publ. 1, 18.
319
Hedenquist, J.W., White, N.C., Siddeley, G. (Eds.), 1990. Epithermal gold mineralization of
320
the Circum-Pacific—geology, geochemistry, origin and exploration. Journal of
321
Geochemical Exploration Special Issue, vols. I and II (447 pp. and 474 pp.).
ACCEPTED MANUSCRIPT 322
Henley, R.W., Berger, B.R., 2011. Magmatic-vapour expansion and the formation of high
323
sulfidation gold deposits: chemical controls on alteration and mineralization. Ore Geol.
324
Rev. 39, 63–74. Horckmans, L., Swennen, R., Deckers, J., Maquil, R., 2005. Local background concentrations
326
of trace elements in soils: a case study in the Grand Ducky of Luxembourg. Catena 59,
327
279–304.
RI PT
325
328
John, D.A., 2001. Miocene and early Pliocene epithermal gold–silver deposits in the northern
329
Great Basin, western USA: characteristics, distribution, and relationship to magmatism.
330
Economic Geology 96, 1827–1853.
332
Krushensky, R.D., 1976. Neogene calc-alkaline extrusive and intrusive rocks of the Karalar–
SC
331
Yeşiller area, northwest Anatolia, Turkey. Bulletin of Volcanology 40, 336–360. Lee, G., Koh, S., Pirajno, F., 2014. Evolution of hydrothermal fluids of HS and LS type
334
epithermal Au–Ag deposits in the Seongsan hydrothermal system of the Cretaceous
335
Haenam volcanic field, South Korea. Ore Geology Reviews, Volume 61, Pages 33–51.
336
Lesage, G., 2011. Geochronology, Petrography, Geochemical Constraints, and Fluid
337
Characterization of the Buriticá Gold Deposit, Antioquia Department, Colombia, Masters
338
Abstracts International.
M AN U
333
Lisowiec, N., Halley, S.H., Ryan, L., 2007. Using Deposit-scale Alteration and Geochemical
340
Signatures to Explore for Analogue Deposits: a Case Study From the Mt Wright Gold
341
Project, Queensland. Geochemical Case Histories & Geochemical Exploration Methods.
342
p. 969-972.
345 346
EP
344
Ma, L.Q., Tan, F., Harris, W., 1997. Concentrations and distributions of eleven metals in Florida soils. Journal of Environmental Quality 26, 769–775. MTA, 2002. Geological map of Turkey, scale 1:500.000. General Directorate of Mineral Research and Exploration (MTA), Ankara.
AC C
343
TE D
339
347
Pendias, A., 2001. Trace elements in soils and plants. Third Edition, CRC Press, NY.
348
Rubio, B., Nombela, M.A., Vilas, F., 2000. Geochemistry of major and trace elements in
349
sediments of the Ria de Vigo (NW Spain): an assessment of metal pollution. Marine
350
Pollution Bulletin 40, 968-980.
351
Sherlock, R.L., 2005. The relationship between the McLaughlin gold–mercury deposit and
352
active hydrothermal systems in the Geysers–Clear Lake area, northern Coast Ranges,
353
California. Ore Geol. Rev. 26, 349–382.
ACCEPTED MANUSCRIPT 354
Simon, G., Kesler, S.E., Russell, N., Hall, C.M., Bell, D., Pinero, E., 1999. Epithermal gold
355
mineralization in an old volcanic arc: the Jacinto deposit, Camaguey district, Cuba.
356
Economic Geology 94, 487–506. Sillitoe, R.H., 2010. Porphyry copper systems. Econ. Geol. 105, 3–41.
358
Sillitoe, R.H., Hedenquist, J.W., 2003. Linkages between volcano tectonic settings, ore-fluid
359
compositions, and epithermal precious metal deposits. In: Simmons, S.F., Graham, I.
360
(Eds.), Volcanic, Geothermal, and Ore-Forming Fluids: Rulers and Witnesses of Processes
361
Within the Earth. Special Publication–Society of Economic Geologists 10, pp. 315–343.
362
Simmons, S.F., Brown, K.L., 2006. Gold in magmatic hydrothermal solutions and the rapid formation of a giant ore deposit. Science 314, 288–291.
SC
363
RI PT
357
Simmons, S.F., White, N.C., John, D.A., 2005. Geologic characteristics of epithermal
365
precious and base metal deposits. Economic Geology 100th Anniversary Volume, pp.
366
485–522.
M AN U
364
367
Sposito, G., 1989. The chemistry of soils, New York, Oxford University Press.
368
Su, Y., Yang, R., 2008. Background concentrations of elements in surface soils and their
369
changes as affected by agriculture use in the desert-oasis ecotone in the middle of Heihe
370
River Basin, North-west China. Journal of Geochemical Exploration 98, 57–64. Tassinari, C.C.G., Pinzon, F.D., Buena Ventura, J., 2008. Age and sources of gold
372
mineralization in the Marmato mining district, NW Colombia: a Miocene–Pliocene
373
epizonal gold deposit. Ore Geol. Rev. 33, 505–518.
TE D
371
Taylor, B.E., 2007. Epithermal gold deposits, in Goodfellow, W.D., ed., Mineral Deposits of
375
Canada: A Synthesis of Major Deposit-Types, District Metallogeny, the Evolution of
376
Geological Provinces, and Exploration Methods: Geological Association of Canada,
377
Mineral Deposits Division, Special Publication No. 5, p. 113-139.
EP
374
Tume, P., Bech, J., Longan, L., Tume, L., Reverter, F., Sepulveda, B., 2006. Trace elements
379
in natural surface soils in Sant Climent (Catalonia, Spain). Ecological Engineering 27,
380
145–152.
AC C
378
381
Warren, I., Simmons, S.F., Mauk, J.L., 2007. Whole-rock geochemical techniques for
382
evaluating hydrothermal alteration, mass changes, and compositional gradients associated
383
with epithermal Au–Ag mineralization. Econ. Geol. 102 (5), 923–948.
384
Warren, I., Zuluaga, J.I., Robbins, C.H., Wulftange, W.H., Simmons, S.F., 2004. Geology and
385
geochemistry of epithermal Au–Ag mineralization in the El Peñón district, northern Chile.
386
In: Sillitoe, R.H., Perello, J., Vidal, C.E. (Eds.), Andean Metallogeny: New Discoveries,
ACCEPTED MANUSCRIPT 387
Concepts, and Updates. Society of Economic Geologists Special Publication 11, pp. 113–
388
139.
389
Wilson, M.A., Burt, R., Indorante, S.J., Jenkins, A.B., Chiaretti, J.V., Ulmer, M.G., Scheyer,
390
J.M., 2008. Geochemistry in the modern soil survey program, Environ Monit Assess. 139,
391
151-171. Yaylalı-Abanuz, G., Tüysüz, N., 2011. Statistical evaluation of the geochemical data from
393
Akoluk epithermal gold area (Ulubey–Ordu), NE Turkey. Geochemical Journal, Vol. 45,
394
pp. 209 to 219.
RI PT
392
Zhai, W., Sun, X., Sun, W., Su, L., He, X., Wu, Y., 2009. Geology, geochemistry, and genesis
396
of Axi: A Paleozoic low-sulfidation type epithermal gold deposit in Xinjiang, China. Ore
397
Geology Reviews 36, 265–281
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ACCEPTED MANUSCRIPT Table 1 Descriptive statistics for geochemical data of 183 soil samples. Maximum Minimum Arithmetic Mean Standard Deviation Medium
Au 0.54 0.0005
Ag 2.66 0.03
As 315 3.4
Sb 19.25 0.15
Cu 35 2.5
Pb 545 17.4
Zn 1240 14
0.04
0.22
30.3
1.62
11.7
73.8
107
0.07 0.01
0.28 0.10
35.3 19.7
1.85 1.18
5.4 11.2
79.5 51.2
122 69
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Table 2 Correlation coefficients for elements in the soil samples. Au
As
Sb
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Rotation Sums of Squared Loadings Cumulative % of Cumulative % of Variance % Total Variance %
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2.81 40.15 40.15 1.78 25.39 1 1.30 18.64 58.79 1.73 24.72 2 0.98 14.02 72.81 1.59 22.70 3 0.87 12.41 85.22 4 0.54 7.65 92.87 5 0.29 4.12 96.99 6 Extraction Method: Principal Component Analysis.
Au Ag As Sb Cu Pb Zn 426
Zn
Table 3 Factor loading in soils of Deliklitaş. Component Initial Eigenvalues
425
Pb
1 0.47** 1 0.40** 0.20** 1 0.15* 0.10 0.71** 1 0.05 0.03 0.17* 0.27** 1 0.26** 0.26** 0.34** 0.23** 0.10 1 0.36** 0.31** 0.43** 0.22** 0.12 0.72** Correlation is significant at the 0.01 level (2-tailed). Correlation is significant at the 0.05 level (2-tailed).
423 424
Cu
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Ag
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Component Factor 1 Factor 2 0.13 0.16 −0.04 0.16 0.78 0.23 0.89 0.07 0.56 0.08 0.13 0.92 0.16 0.88
Factor 3 0.83 0.82 0.35 0.12 −0.15 0.12 0.24
25.39 50.11 72.81
1
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428
SC
427 Fig. 1. Location map of the study area
430
Deliklitaş
431
Yaylak H.
432 433 434
436 437 438 439
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Eyrek H.
Kocaçayır Location
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Fig. 2. Geological and location map of the Deliklitaş Au deposit and surrounding area,
444
showing soil sample locations.
445
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Fig. 3. Simplified geologic map of the main lithotectonic/stratigraphic units in the region.
448
Note the study area is located at the southern end of a widely exposed alteration zone (MTA,
449
2002).
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Ag Au
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Zn Pb Sb As
Cu
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-1
451 452 453
Fig. 4. Dendrogram showing element groups in soil samples on which cluster analysis was
454
applied.
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Fig. 5. Contour diagrams showing Au, As, Sb, Ag, Zn, Pb and Cu distributions in soil
458
samples.
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ACCEPTED MANUSCRIPT Highlights (revision) The major alteration types are propylithic, extensive argillic and silicification
•
Deliklitaş Au deposit is closely associated with Ag, As, Cu, Sb, Zn and Pb elements
•
Statistical evaluations indicate that Au is closely associated with Ag and As.
•
Factor analysis account for 72.81% of the total variances.
•
Au, Ag, As, Sb, Cu, Pb and Zn show widespread anomalies in the mineralization area
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