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  5.     <title>UTas ePrints - Geology, Mineralization, Alteration, and Structural Evolution of the El Teniente Porphyry Cu-Mo Deposit</title>
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  13.     <meta content="Cannell, J." name="eprints.creators_name" />
  14. <meta content="Cooke, D.R." name="eprints.creators_name" />
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  30. <meta content="El Teniente is a typical porphyry Cu-Mo deposit-in terms of its alteration and sulfide assemblage zonation,
  31. association with felsic intrusions, and predominance of quartz vein-hosted copper mineralization. It is anomalous
  32. in size, with >94 million metric tons (Mt) of contained fine copper making it the worlds largest known
  33. porphyry Cu deposit. There is an intimate spatial and temporal association between all stages of mineralization
  34. and latest Miocene to early Pliocene felsic intrusions at Teniente.
  35. Most of the copper was emplaced during the late magmatic stage (5.9-4.9 Ma), contemporaneously with intrusion
  36. of the dacite porphyry dike and dacite pipes into a mafic to intermediate sill-stock complex. Mineralization
  37. of the late magmatic stage is mainly hosted by a quartz-anhydrite-dominated stockwork associated with
  38. K-feldspar alteration in the dacites and Na-K-feldspar, biotite, and propylitic alteration of the mafic intrusive
  39. package. Minor copper-mineralized hydrothermal biotite-cemented breccias formed at this time. The late
  40. magmatic stage was followed by two stages of mineralized phyllic alteration, referred to as the principal hydrothermal
  41. (4.9-4.8 Ma) and late hydrothermal (4.8-4.4 Ma) stages, during which thicker, Cu-rich veins were
  42. emplaced. A 1,200-m-wide breccia pipe, the Braden Breccia, formed during the late hydrothermal stage and
  43. appears to have destroyed a large amount of ore from the center of the deposit.
  44. The late magmatic and principal hydrothermal vein stages have predominantly concentric and radial vein
  45. orientations centered on the Braden Pipe. Most of the concentric veins are shallowly dipping, whereas the radial
  46. veins are subvertical. We present a model in which vein distributions were controlled by the local stress
  47. regime generated by the intrusion of a large, deep magma chamber that is interpreted to be the source of the
  48. dacites, the Braden Pipe, and ultimately, the copper and molybdenum mineralization. The late hydrothermal
  49. veins are steeply inward dipping and concentric to the Braden Pipe. In contrast to the late magmatic and principal
  50. hydrothermal vein stages, radial veins and shallow-dipping concentric veins are rare, consistent with formation
  51. during a stage of subsidence due to relaxation of intrusion-induced stresses. Resurgence of the magma
  52. chamber reactivated the steep concentric structures in a reverse sense, and a build up of magmatic and/or fluid
  53. pressure resulted in explosive brecciation and fluidization, producing the Braden Pipe. A predominantly late set of northeast-trending faults, associated with movements on the district-scale Teniente fault zone, is the only evidence for far-field stresses exceeding local stresses in the deposit." name="eprints.abstract" />
  54. <meta content="2005" name="eprints.date" />
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  65. <meta content="Acocella, V., Cifelli, F., and Funiciello, R., 2000, Analogue models of collapse calderas and resurgent domes: Journal of Volcanology and Geothermal Research,
  66. v. 104, p. 81-96.
  67. Atkinson, W.W., Souviron, S., Vehrs, T.I., and Faunes, A., 1996, Geology and mineral zoning of the Los Pelambres porphyry Cu deposit, Chile: Society of Economic Geologists Special Publication 5, p. 131-155.
  68. Burnham, C.W., 1979, Magmas and hydrothermal fluids, in Barnes, H.L., ed., Geochemistry of hydrothermal ore deposits: New York, Wiley-Interscience, p. 71-136.
  69. Camus, F., 1975, Geology of the El Teniente orebody with emphasis on wallrock alteration: ECONOMIC GEOLOGY, v. 70, p. 1341-1372.
  70. Camus, F., 2002, The Andean porphyry systems: Hobart, Tasmania, University of Tasmania, CODES Special Publication 4, p. 1-38.
  71. Cannell, J., 2004, El Teniente porphyry copper-molybdenum deposit, central Chile: Unpublished Ph.D. thesis, Hobart, University of Tasmania, 317 p.
  72. Cannell, J., Cooke, D.R., Stein, H.J., and Markey, R.J., 2003, New paragenetically constrained Re-Os molybdenite ages for El Teniente Cu-Mo porphyry deposit, central Chile [abs]: Society for Geology Applied to mineral Deposits (SGA), Athens, 2003, Abstracts with Programs, v. 1, p.
  73. 255-258.
  74. Charrier, R., Baeza, O., Elgueta, S., Flynn, J.J., Gans, P., Kay, S.M., Munoz, N., Wyss, A.R., and Zurita, E., 2002, Evidence for Cenozoic extensional basin development and tectonic inversion south of the flat-slab segment,
  75. southern central Andes, Chile (33degrees-36degrees S.L.): Journal of South American Earth Sciences, v. 15, p. 117-139.
  76. Cuadra, P., 1986, Geocronologia K-Ar del yacimiento El Teniente y areas adyacentes: Revista Geologica de Chile, v. 27, p. 3-26.
  77. Duarte, P.O., 2000, Caracterizacion geologica y geotecnica del porfido dacitico El Teniente: Unpublished Honours thesis, Santiago, Universidad de Chile, 80 p.
  78. Engel, A.E., and Engel, C.G., 1960, Progressive metamorphism and granitization of the major paragneiss, northwest Adirondack Mountains, New York: Geological Society of America Bulletin, v. 71, p. 1-57.
  79. Faunes, A., 1981, Caracterizacion de la mineralogi­a metalica y alteracion en un sector del Stock Tonalitico del yacimiento El Teniente: Unpublished Honours thesis, Santiago, Universidad de Chile, 175 p.
  80. Garrido, I., Riveros, M., Cladouhos, T., Espineira, D., and Allmendinger, R., 1994, Modelo geologico estructural del yacimiento El Teniente: Congreso Geologico Chileno, 7th, Concepcion, 1994, Actas, v. 2, p. 1553-1558.
  81. Garwin, S., 2002, The geological setting of intrusion-related hydrothermal systems near the Batu Hijau porphyry Cu-Au deposit, Sumbawa, Indonesia: Society of Economic Geologists Special Publication 9, p. 333-366.
  82. Godoy, E., Yanez, G., and Vera, E., 1999, Inversion of an Oligocene volcanotectonic basin and uplifting of its superimposed Miocene magmatic arc in the Chilean Central Andes: First seismic and gravity evidences: Tectonophysics,
  83. v. 306, p. 217-236.
  84. Gustafson, L.B., and Hunt, J.P., 1975, The porphyry copper deposit at El Salvador, Chile: ECONOMIC GEOLOGY, v. 70, p. 857-912.
  85. Guzman, C.G., 1991, Alteracion y mineralizacion de los Porfidos Dioriticos del sector central, yacimiento El Teniente: Unpublished honours thesis, Santiago, Universidad de Chile, 143 p.
  86. Heidrick, T.L., and Titley, S.R., 1982, Fracture and dike patterns in Laramide plutons and their structural and tectonic implications; American Southwest, in Titley S.R., ed., Advances in geology of porphyry Cu deposits,
  87. southwestern North America: Tucson, University of Arizona Press, p. 73-91.
  88. Holliday, J.R., Wilson, A.J., Blevin, P.L., Tedder, I.J., Dunham, P.D., and Pfitzner, M., 2002, Porphyry Au-copper mineralization in the Cadia district, eastern Lachlan fold belt, New South Wales, and its relationship to shoshonitic magmatism: Mineralium Deposita, v. 37, p. 100-116.
  89. Howell, F.H., and Molloy, J. S., 1960, Geology of the Braden orebody, Chile, South America: ECONOMIC GEOLOGY, v. 55, p. 863-905.
  90. Kay, S.M., and Kurtz, A., 1995, Magmatic and tectonic characterization of the El Teniente region: Internal report, Superintendencia de Geologia, El
  91. Teniente, CODELCO, 180 p.
  92. Kay, S., Mpodozis, C., and Coira, B., 1999, Neogene magmatism, tectonism, and mineral deposits of the central Andes (22 degrees to 33 degrees latitude): Society of
  93. Economic Geologists Special Publication 7, p. 27-59.
  94. Kirkham, R.V., and Sinclair, W.D., 1988, Comb quartz layers in felsic intrusions and their relationship to porphyry deposits: Canadian Institute of Mining and Metallurgy, v. 39, p. 50-71.
  95. Koide, H., and Bhattacharji, S., 1975, Formation of fractures around magmatic intrusions and their role in ore localization: ECONOMIC GEOLOGY, v. 70, p. 781-799.
  96. Kurtz, A., Kay, S.M., Charrier, R., and Farrar, E., 1997, Geochronology of Miocene plutons and exhumation history of the El Teniente region, central Chile (34-35 degrees S): Revista Geologica de Chile, v. 24, p. 75-90.
  97. Le Bel, L., 1979, Magmatic and hydrothermal micas in the environment of the Cerro Verde-Santa Rosa porphyry Cu, Peru, in Robert, J. L., ed., Les Micas; Chimie et cristallochimie: Paris, Masson, p. 35-41.
  98. Lindgren, W., and Bastin, E.S., 1922, Geology of the Braden mine, Rancagua, Chile: ECONOMIC GEOLOGY, v. 17, p. 863-905.
  99. Lindsay, D.D., Zentilli, M., and Rojas de la Rivera, J., 1995, Evolution of an active ductile to brittle shear system controlling mineralization at Chuquicamata porphyry copper deposit, northern Chile: International Geology
  100. Reviews, v. 37, p. 945-958.
  101. Lowell, D., and Guilbert, J.M., 1970, Lateral and vertical alteration-mineralization zoning in porphyry ore deposits: ECONOMIC GEOLOGY, v. 65, p. 373-408.
  102. Maksaev, V., Munizaga, F., McWilliams, M., Fanning, M., Mathur, R., Ruiz, J., and Thiele, K., 2002, El Teniente porphyry Cu deposit in the Chilean Andes: New geochronological time frame and duration of hydrothermal activity [abs]: Geological Society of America Abstracts with Programs, v. 34, no. 6, p 336.
  103. Maksaev, V., Munizaga, F., McWilliams, M., Fanning, M., Mathur, R., Ruiz, J., and Zentilli, M., 2004, New chronology for El Teniente, Chilean Andes, from U-Pb, 40Ar/39Ar, Re-Os, and fission-track dating: Implications for the evolution of a supergiant porphyry Cu-Mo deposit: Society of Economic Geologists Special Publication 11, p. 15-54.
  104. Ossandon, G., 1974, Petrografay alteracion del Porfido Dacitico, yacimiento El Teniente: Unpublished honours thesis, Santiago, Universidad de Chile, 112 p.
  105. Reich, M.H., 2000, Estudio petrografico, mineraloquimico y geoquimico de los cuerpos intrusivos de Sewell y La Huifa en el sector del yacimiento El Teniente, VI Region, Chile: Unpublished Honours thesis, Concepcion, Universidad de Concepcion, 95 p.
  106. Rivera, O., and Cembrano, J., 2000, Modelo de formacion de cuencas volcano-tectonicas en zonas de transferencia oblicuas a la cadena Andina: el caso de las cuencas Oligo-Miocenos de Chile central y su relacion con estructuras WNW-NW (33 degrees 00'-34 degrees 30' LS) [abs]: Congresso Geologico Chileno, 9th, Puerto Varas, Chile, 2000, Actas, 5 p.
  107. Rivera, O., and Falcon, M., 2000, Las Formaciones Farellones, Coya-Machali y Abanico en los aldredores del yacimiento El Teniente: Sequencias de cuencas volcano-tectonicas transversales del Oligo-Mioceno
  108. de Chile central (33 degrees 45'-34 degrees 30' LS): Congresso Geologico Chileno, 9th, Puerto Varas, Chile, 2000, Actas, 5 p.
  109. Riveros, M., 1989, Geologia del porfido latitico sector sur yacimiento El Teniente: Unpublished Honours thesis, Santiago, Universidad de Chile, 133 p.
  110. Rojas, A., 2002, Petrografia y geoquimica del porfido dacitico Teniente,
  111. yacimiento El Teniente, Provincia de Cachapoal, VI Region, Chile: Unpublished Honours thesis, Concepcion, Universidad de Concepcion, 118 p.
  112. Rytuba, J.J., 1994, Evolution of volcanic and tectonic features in caldera settings and their importance in localization of ore deposits: ECONOMIC GEOLOGY,
  113. v. 89, p. 1687-1696.
  114. Serrano, L., Vargas, R., Stambuk, V., Aguilar, C., Galeb, M., Holmgren, C., Contreras, A., Godoy, S., Vela, I., Skewes M.A., and Stern C.R., 1996, The late Miocene to early Pliocene Rio Blanco-Los Bronces copper deposit,
  115. Central Chilean Andes: Society of Economic Geologists Special Publication 5, p. 119-130.
  116. Shannon, J.R., Walker, B.M., Carten, R.B., and Geraght, E.P., 1982, Unidirectional solidification textures and their significance in determining relative
  117. ages of intrusions at the Henderson mine, Colorado: Geology, v. 10, p. 293-297.
  118. Sillitoe, R.H., 1985, Ore-related breccias in volcanoplutonic arcs: ECONOMIC GEOLOGY, v. 80, p. 1467-1514.
  119. -2000, Gold-rich porphyry deposits: Descriptive and genetic models and their role in exploration and discovery: Reviews in Economic Geology, v. 13, p. 315-345.
  120. Skewes, A., Arevalo, A., Floody, R., Zuniga, P.H., and Stern, C.R., 2002, The giant El Teniente breccia deposit: Hypogene copper distribution and emplacement: Society of Economic Geologists Special Publication 9, p.
  121. 299-332.
  122. Thiele, R., Beccar, I., Levi, B., Nystrom, J., and Vergara, M., 1991, Tertiary Andean volcanism in a caldera-graben setting: Geologische Rundschau, v. 80, p. 179-186.
  123. Titley, S.R., 1990, Evolution and style of fracture permeability in intrusioncentered hydrothermal systems, in Titley S.R., ed., The role of fluids in crustal processes: Washington DC, National Acadamic Press, p. 50-63.
  124. Tosdal, R.M., and Richards, J.P., 2001, Magmatic and structural controls on the development of porphyry Cu plus or minus Mo plus or minus Au deposits: Reviews in Economic
  125. Geology, v. 14, p. 157-181.
  126. Villalobos, J., 1975, Alteracion hidrotermal en las andesitas del yacimiento El Teniente, Chile: Unpublished Ph.D. thesis, Santiago, Universidad de Chile,
  127. 125 p.
  128. Zuniga, P., 1982, Alteracion y mineralizacion hipogenas en el sector oeste del yacimiento El Teniente: Unpublished Honours thesis, Santiago, Universidad de Chile, 107 p." name="eprints.referencetext" />
  129. <meta content="Cannell, J. and Cooke, D.R. and Walshe, J.L. and Stein, Holly J. (2005) Geology, Mineralization, Alteration, and Structural Evolution of the El Teniente Porphyry Cu-Mo Deposit. Economic Geology, 100 (5). pp. 979-1003. ISSN 0361-0128" name="eprints.citation" />
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  133. <meta content="Cannell, J." name="DC.creator" />
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  135. <meta content="Walshe, J.L." name="DC.creator" />
  136. <meta content="Stein, Holly J." name="DC.creator" />
  137. <meta content="260100 Geology" name="DC.subject" />
  138. <meta content="El Teniente is a typical porphyry Cu-Mo deposit-in terms of its alteration and sulfide assemblage zonation,
  139. association with felsic intrusions, and predominance of quartz vein-hosted copper mineralization. It is anomalous
  140. in size, with >94 million metric tons (Mt) of contained fine copper making it the worlds largest known
  141. porphyry Cu deposit. There is an intimate spatial and temporal association between all stages of mineralization
  142. and latest Miocene to early Pliocene felsic intrusions at Teniente.
  143. Most of the copper was emplaced during the late magmatic stage (5.9-4.9 Ma), contemporaneously with intrusion
  144. of the dacite porphyry dike and dacite pipes into a mafic to intermediate sill-stock complex. Mineralization
  145. of the late magmatic stage is mainly hosted by a quartz-anhydrite-dominated stockwork associated with
  146. K-feldspar alteration in the dacites and Na-K-feldspar, biotite, and propylitic alteration of the mafic intrusive
  147. package. Minor copper-mineralized hydrothermal biotite-cemented breccias formed at this time. The late
  148. magmatic stage was followed by two stages of mineralized phyllic alteration, referred to as the principal hydrothermal
  149. (4.9-4.8 Ma) and late hydrothermal (4.8-4.4 Ma) stages, during which thicker, Cu-rich veins were
  150. emplaced. A 1,200-m-wide breccia pipe, the Braden Breccia, formed during the late hydrothermal stage and
  151. appears to have destroyed a large amount of ore from the center of the deposit.
  152. The late magmatic and principal hydrothermal vein stages have predominantly concentric and radial vein
  153. orientations centered on the Braden Pipe. Most of the concentric veins are shallowly dipping, whereas the radial
  154. veins are subvertical. We present a model in which vein distributions were controlled by the local stress
  155. regime generated by the intrusion of a large, deep magma chamber that is interpreted to be the source of the
  156. dacites, the Braden Pipe, and ultimately, the copper and molybdenum mineralization. The late hydrothermal
  157. veins are steeply inward dipping and concentric to the Braden Pipe. In contrast to the late magmatic and principal
  158. hydrothermal vein stages, radial veins and shallow-dipping concentric veins are rare, consistent with formation
  159. during a stage of subsidence due to relaxation of intrusion-induced stresses. Resurgence of the magma
  160. chamber reactivated the steep concentric structures in a reverse sense, and a build up of magmatic and/or fluid
  161. pressure resulted in explosive brecciation and fluidization, producing the Braden Pipe. A predominantly late set of northeast-trending faults, associated with movements on the district-scale Teniente fault zone, is the only evidence for far-field stresses exceeding local stresses in the deposit." name="DC.description" />
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  275.     <h1 class="ep_tm_pagetitle">Geology, Mineralization, Alteration, and Structural Evolution of the El Teniente Porphyry Cu-Mo Deposit</h1>
  276.     <p style="margin-bottom: 1em" class="not_ep_block"><span class="person_name">Cannell, J.</span> and <span class="person_name">Cooke, D.R.</span> and <span class="person_name">Walshe, J.L.</span> and <span class="person_name">Stein, Holly J.</span> (2005) <xhtml:em>Geology, Mineralization, Alteration, and Structural Evolution of the El Teniente Porphyry Cu-Mo Deposit.</xhtml:em> Economic Geology, 100 (5). pp. 979-1003. ISSN 0361-0128</p><p style="margin-bottom: 1em" class="not_ep_block"></p><table style="margin-bottom: 1em" class="not_ep_block"><tr><td valign="top" style="text-align:center"><a href="http://eprints.utas.edu.au/1908/1/Cannell_Cooke_et_al_ECON_GEOL_2005.pdf"><img alt="[img]" src="http://eprints.utas.edu.au/style/images/fileicons/application_pdf.png" border="0" class="ep_doc_icon" /></a></td><td valign="top"><a href="http://eprints.utas.edu.au/1908/1/Cannell_Cooke_et_al_ECON_GEOL_2005.pdf"><span class="ep_document_citation">PDF</span></a> - Full text restricted - Requires a PDF viewer<br />4Mb</td><td><form method="get" accept-charset="utf-8" action="http://eprints.utas.edu.au/cgi/request_doc"><input value="2403" name="docid" accept-charset="utf-8" type="hidden" /><div class=""><input value="Request a copy" name="_action_null" class="ep_form_action_button" onclick="return EPJS_button_pushed( '_action_null' )" type="submit" /> </div></form></td></tr></table><p style="margin-bottom: 1em" class="not_ep_block">Official URL: <a href="http://dx.doi.org/10.2113/100.5.979">http://dx.doi.org/10.2113/100.5.979</a></p><div class="not_ep_block"><h2>Abstract</h2><p style="padding-bottom: 16px; text-align: left; margin: 1em auto 0em auto">El Teniente is a typical porphyry Cu-Mo deposit-in terms of its alteration and sulfide assemblage zonation,&#13;
  277. association with felsic intrusions, and predominance of quartz vein-hosted copper mineralization. It is anomalous&#13;
  278. in size, with &gt;94 million metric tons (Mt) of contained fine copper making it the worlds largest known&#13;
  279. porphyry Cu deposit. There is an intimate spatial and temporal association between all stages of mineralization&#13;
  280. and latest Miocene to early Pliocene felsic intrusions at Teniente.&#13;
  281. Most of the copper was emplaced during the late magmatic stage (5.9-4.9 Ma), contemporaneously with intrusion&#13;
  282. of the dacite porphyry dike and dacite pipes into a mafic to intermediate sill-stock complex. Mineralization&#13;
  283. of the late magmatic stage is mainly hosted by a quartz-anhydrite-dominated stockwork associated with&#13;
  284. K-feldspar alteration in the dacites and Na-K-feldspar, biotite, and propylitic alteration of the mafic intrusive&#13;
  285. package. Minor copper-mineralized hydrothermal biotite-cemented breccias formed at this time. The late&#13;
  286. magmatic stage was followed by two stages of mineralized phyllic alteration, referred to as the principal hydrothermal&#13;
  287. (4.9-4.8 Ma) and late hydrothermal (4.8-4.4 Ma) stages, during which thicker, Cu-rich veins were&#13;
  288. emplaced. A 1,200-m-wide breccia pipe, the Braden Breccia, formed during the late hydrothermal stage and&#13;
  289. appears to have destroyed a large amount of ore from the center of the deposit.&#13;
  290. The late magmatic and principal hydrothermal vein stages have predominantly concentric and radial vein&#13;
  291. orientations centered on the Braden Pipe. Most of the concentric veins are shallowly dipping, whereas the radial&#13;
  292. veins are subvertical. We present a model in which vein distributions were controlled by the local stress&#13;
  293. regime generated by the intrusion of a large, deep magma chamber that is interpreted to be the source of the&#13;
  294. dacites, the Braden Pipe, and ultimately, the copper and molybdenum mineralization. The late hydrothermal&#13;
  295. veins are steeply inward dipping and concentric to the Braden Pipe. In contrast to the late magmatic and principal&#13;
  296. hydrothermal vein stages, radial veins and shallow-dipping concentric veins are rare, consistent with formation&#13;
  297. during a stage of subsidence due to relaxation of intrusion-induced stresses. Resurgence of the magma&#13;
  298. chamber reactivated the steep concentric structures in a reverse sense, and a build up of magmatic and/or fluid&#13;
  299. pressure resulted in explosive brecciation and fluidization, producing the Braden Pipe. A predominantly late set of northeast-trending faults, associated with movements on the district-scale Teniente fault zone, is the only evidence for far-field stresses exceeding local stresses in the deposit.</p></div><table style="margin-bottom: 1em" border="0" cellpadding="3" class="not_ep_block"><tr><th valign="top" class="ep_row">Item Type:</th><td valign="top" class="ep_row">Article</td></tr><tr><th valign="top" class="ep_row">Keywords:</th><td valign="top" class="ep_row">porphyry copper molybdenum structure paragenesis geochronology</td></tr><tr><th valign="top" class="ep_row">Subjects:</th><td valign="top" class="ep_row"><a href="http://eprints.utas.edu.au/view/subjects/260100.html">260000 Earth Sciences &gt; 260100 Geology</a></td></tr><tr><th valign="top" class="ep_row">Collections:</th><td valign="top" class="ep_row">UNSPECIFIED</td></tr><tr><th valign="top" class="ep_row">ID Code:</th><td valign="top" class="ep_row">1908</td></tr><tr><th valign="top" class="ep_row">Deposited By:</th><td valign="top" class="ep_row"><span class="ep_name_citation"><span class="person_name">Mrs Katrina Keep</span></span></td></tr><tr><th valign="top" class="ep_row">Deposited On:</th><td valign="top" class="ep_row">19 Sep 2007</td></tr><tr><th valign="top" class="ep_row">Last Modified:</th><td valign="top" class="ep_row">29 Jan 2008 20:32</td></tr><tr><th valign="top" class="ep_row">ePrint Statistics:</th><td valign="top" class="ep_row"><a target="ePrintStats" href="/es/index.php?action=show_detail_eprint;id=1908;">View statistics for this ePrint</a></td></tr></table><p align="right">Repository Staff Only: <a href="http://eprints.utas.edu.au/cgi/users/home?screen=EPrint::View&amp;eprintid=1908">item control page</a></p>
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