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Magmatic Evolution of the Giant El Teniente Cu^Mo Deposit, Central Chile

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Magmatic Evolution of the Giant El Teniente Cu^Mo Deposit, Central Chile JOURNAL OF PETROLOGY VOLUME 52 NUMBERS 7 & 8 PAGES 1591^1617 2011 doi:10.1093/petrology/egq029 Magmatic Evolution of the Giant El Teniente Cu^Mo Deposit, Central Chile CHARLES R. STERN1*, M. ALEXANDRA SKEWES1 AND ALEJANDRA ARE¤VA LO 2 1DEPARTMENT OF GEOLOGICAL SCIENCES, UNIVERSITY OF COLORADO, BOULDER, CO 80309-0399, USA 2SUPERINTENDENCIA GEOLOGI¤ A, EL TENIENTE, CODELCO-CHILE, RANCAGUA, CHILE RECEIVED JULY 7, 2009; ACCEPTED MAY 6, 2010 ADVANCE ACCESS PUBLICATION JUNE 28, 2010 ElTeniente, the world’slargest Cu deposit, is hosted in Late Miocene volumes of more fractionated, but isotopically equivalent, Late and Pliocene plutons that intrude the older Teniente Volcanic Miocene and Pliocene felsic plutonic rocks that host the deposit Complex (or Farellones Fm; 14·2^6·5 Ma). The Late Miocene were derived from the roof of a large, long-lived, thermally and and Pliocene plutonic host rocks of the deposit include, sequentially, chemically stratified, open-system magma chamber, or magmatic the relatively large (450 km3) Teniente Mafic Complex laccolith plumbing system, recharged from below by mantle-derived magmas. (8 ·9 Æ1·4 Ma),the smaller (30 km3) Sewell equigranular tonal- Only when this system fully solidified did post-mineralization ite complex (7·05 Æ 0·14 Ma) and associated andesitic sills mafic olivine-hornblende-lamprophyre dikes (3·85 Æ 0·18 to (8 ·2 Æ 0·5to6·6 Æ 0·4 Ma), small dacitic porphyry stocks 2·9 Æ 0·6 Ma) pass through the system from the mantle to the sur- (51km3;6·09 Æ 0·18 Ma), the unusual Cu- and S-rich ‘Porphyry face. The significant progressive temporal isotopic evolution, to 3 87 86 A’anhydrite-bearing granitoid stock (51km ;5·67 Æ 0·19 Ma),the higher Sr/ Sr (from 0·7033 to 0·7049) and lower eNd (from Teniente Dacite Porphyry dike (51km3;5·28 Æ 0·10 Ma), minor þ6·2toÀ1·1), that occurred between the Late Oligocene and latite dikes (4·82 Æ 0·09 Ma),and finally a small dacite intrusion Pliocene in the vicinity of El Teniente for mafic mantle-derived (4 ·58 Æ 0·10 Ma).These plutonic rocks are all isotopically similar magmas, and by implication their sub-arc mantle-source region, 87 86 to each other ( Sr/ Sr ¼ 0·7039^0·7042; eNd ¼þ2·5toþ3·5) was due in part to increased mantle-source region contamination by and also to the Teniente Volcanic Complex extrusive rocks, but dis- subducted crust tectonically eroded off the continental margin. The tinct from both older Late Oligocene to Early Miocene volcanic post-mineralization olivine-hornblende-lamprophyres also imply ex- 87 86 rocks ( Sr/ Sr ¼ 0·7033^0·7039; eNd ¼þ3·8toþ 6·2) and tensive hydration of the mantle below this portion of the Andean arc younger Pliocene post-mineralization mafic dikes and lavas by the Pliocene, which may have played a role in producing oxidized 87 86 ( Sr/ Sr ¼ 0·7041^0·7049; eNd ¼þ1·1toÀ1·1). Multiple volatile-rich magmas and mineralization at El Teniente. Cu-mineralized magmatic^hydrothermal breccia pipes were emplaced into these plutonic rocks during the same time period as the felsic porphyry intrusions, between at least 6·31 Æ0·03 and KEY WORDS: Chilean Andes; copper deposits; ElTeniente; magmagen- 4·42 Æ 0·02 Ma.These mineralized breccia pipes, which formed by esis; petrochemistry exsolution of magmatic fluids from cooling plutons, have their roots below the deepest level of mining and exploration drilling and were derived from the same magma chamber as the felsic porphyries, INTRODUCTION 44 km below the paleosurface.Toproduce the 100 Â106 tonnes of The giant El Teniente Cu^Mo deposit, located in central Cu in the deposit requires a batholith-size (4600 km3) amount of Chile (348050S, 70821 0W; Fig. 1), is the world’s largest Cu de- magma with 100 ppm Cu. We suggest that both the mineralized posit, originally containing 100 million metric tonnes magmatic^hydrothermal breccias and the progressively smaller (Mt) of Cu (Skewes et al., 2002, 2005). The deposit is ß The Author 2010. Published by Oxford University Press. All *Corresponding author. Telephone: 303-492-7170. Fax: 303-492-2606. rights reserved. For Permissions, please e-mail: journals.permissions@ E-mail: [email protected] oup.com JOURNAL OF PETROLOGY VOLUME 52 NUMBERS 7 & 8 JULY & AUGUST 2011 Fig. 1. Location maps of El Teniente and the two other giant Late Miocene and Pliocene Cu deposits in the Andes of central Chile, Los Pelambres and R|¤o Blanco^Los Bronces, modified from Serrano et al. (1996). (a) Map showing tectonic features such as the location of the Chile Trench, which is the boundary between the Nazca and South American plates, and the depth in kilometers (100 and 150 km dashed lines) to the Benioff Zone below South America. The Cu deposits occur just east of the locus of subduction of the Juan Ferna¤ ndez Ridge. This also marks the boundary between the Andean Flat-Slab segment, below which the subduction angle is very low, as indicated by the depths to the upper boundary of the subducted slab, and the Southern Volcanic Zone (SVZ) of active volcanoes (m), below which the subduction angle is steeper. The map also shows the location of the Central Volcanic Zone (CVZ) and some of the Late Eocene and Early Oligocene Cu deposits in northern Chile. (b) Simplified regional geology of central Chile. In this schematic map, both the Coya-Machali (Abanico) and Farellones Formations are included together in the belt of Late Tertiary volcanic rocks. hosted in Late Miocene and Pliocene igneous rocks (Figs 2 ‘preserves a record of alternating igneous activity and ore and 3). The chronology of the formation of these igneous deposition that affords convincing evidence of the intimate rocks, both in and around the deposit, is reasonably well genetic connection between igneous rocks and ore de- determined (Fig. 4; Cuadra, 1986; Kurtz et al., 1997; posits’. As a contribution to the understanding of this gen- Maksaev et al., 2004), and the published petrochemical etic connection, we present the results of a petrochemical database for understanding the regional magmatic evolu- study of the igneous rocks within the El Teniente deposit. tion at the latitude of El Teniente is among the most de- tailed in the southern Andes (Stern & Skewes, 1995; Nystrom et al., 2003; Kay et al., 2005; Mun‹ oz et al., 2006). GEOLOGICAL BACKGROUND However, the petrochemistry and genesis of the igneous El Teniente, along with Los Pelambres (328S;425 Mt of rocks within the El Teniente deposit have received less at- Cu; Atkinson et al., 1996) and R|¤o Blanco^Los Bronces tention than those surrounding the deposit. It is clear, (338S; 450 Mt of Cu; Warnaars et al., 1985; Serrano et al., from the overlap of the isotopic ages of both the igneous 1996; Frikken et al., 2005), formed during Miocene and rocks (8·9 Æ1·4to4·58 Æ 0·10 Ma; Fig. 4) and the multiple Pliocene times in the Andes of central Chile (Fig. 1), and alteration and mineralization events in the deposit are among the youngest and largest Cu^Mo deposits in (6·31 Æ0·03 to 4·42 Æ0·02 Ma), that there is a direct genet- the Andes. They are copper-, sulfur-, iron-, calcium-, mo- ic relation between igneous activity and mineralization. lybdenum- and boron-rich, but gold-poor deposits that This was originally recognized by Lindgren & Bastin share important features. These include their large tonnage (1922), who identified several periods of intrusion and min- and high hypogene copper grade, and the fact that most eralization at El Teniente, and concluded that this deposit of the copper mineralization occurs as primary hypogene 1592 STERN et al. EVOLUTION OF EL TENIENTE CU^MO DEPOSIT Fig. 2. Geological map of the area surrounding the El Teniente copper deposit, modified from Morel & Spro« hnle (1992) and Skewes et al.(2002, 2005).The Braden breccia pipe is located at the intersection of the Teniente Fault Zone, which trends NE^SW between the Teniente River and Agua Amarga fault, and the NW^SE-trending Puquios^Codegua fault. ore. Another distinctive feature that each of these three (Fig. 1a): the Flat-Slab segment to the north, below which deposits has in common is the presence of large magmat- the angle of subduction has decreased significantly since ic^hydrothermal breccias, both mineralized and unminer- the Miocene and where volcanism is now absent, and the alized (Skewes & Stern, 1994, 1995, 1996). The genesis of Southern Volcanic Zone (SVZ), below which the subduc- these magmatic^hydrothermal breccias has been attribu- tion angle is steeper and volcanism is active. The formation ted to the exsolution of high-temperature magmatic fluids of the three deposits is closely associated in time with the from cooling plutons (Warnaars et al., 1985; Skewes & changing geometry of subduction that has produced this Stern, 1994, 1995, 1996; Vargas et al., 1999; Skewes et al., segmentation of the Andes (Stern, 1989, 2004; Skewes & 2002, 2003). Stern, 1994, 1995; Stern & Skewes, 1995, 2005; Rosenbaum The three deposits in central Chile occur across the et al., 2005). As with the older copper deposits in northern boundary between two major Andean tectonic segments Chile, such as Chuquicamata and El Salvador (Fig. 1a), 1593 JOURNAL OF PETROLOGY VOLUME 52 NUMBERS 7 & 8 JULY & AUGUST 2011 Fig. 3. Geological map of level Teniente 5 (2284 m above sea level) in the mine, modified from Skewes et al. (2002, 2005).The Dacitic Porphyries, north of the Sewell Tonalite, are mapped as a distal portion of this pluton, although they are younger (Maksaev et al., 2004) and have an inde- pendent origin (Guzma¤ n, 1991; Hitschfeld, 2006).
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