<?xml version="1.0" encoding="ISO-8859-1"?><article xmlns:mml="http://www.w3.org/1998/Math/MathML" xmlns:xlink="http://www.w3.org/1999/xlink" xmlns:xsi="http://www.w3.org/2001/XMLSchema-instance">
<front>
<journal-meta>
<journal-id>1405-3322</journal-id>
<journal-title><![CDATA[Boletín de la Sociedad Geológica Mexicana]]></journal-title>
<abbrev-journal-title><![CDATA[Bol. Soc. Geol. Mex]]></abbrev-journal-title>
<issn>1405-3322</issn>
<publisher>
<publisher-name><![CDATA[Sociedad Geológica Mexicana A.C.]]></publisher-name>
</publisher>
</journal-meta>
<article-meta>
<article-id>S1405-33222020000300013</article-id>
<article-id pub-id-type="doi">10.18268/bsgm2020v72n3a130220</article-id>
<title-group>
<article-title xml:lang="en"><![CDATA[The mineral deposits of Panama: Arc metallogenesis on the trailing edge of the Caribbean large igneous province]]></article-title>
<article-title xml:lang="es"><![CDATA[Los depósitos minerales de Panamá: metalogénesis de Arco en el borde posterior de la gran provincia ígnea del Caribe]]></article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Redwood]]></surname>
<given-names><![CDATA[Stewart D.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
</contrib-group>
<aff id="Af1">
<institution><![CDATA[,Consulting Economic Geologist  ]]></institution>
<addr-line><![CDATA[Panama ]]></addr-line>
<country>Panama</country>
</aff>
<pub-date pub-type="pub">
<day>00</day>
<month>00</month>
<year>2020</year>
</pub-date>
<pub-date pub-type="epub">
<day>00</day>
<month>00</month>
<year>2020</year>
</pub-date>
<volume>72</volume>
<numero>3</numero>
<copyright-statement/>
<copyright-year/>
<self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_arttext&amp;pid=S1405-33222020000300013&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_abstract&amp;pid=S1405-33222020000300013&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_pdf&amp;pid=S1405-33222020000300013&amp;lng=en&amp;nrm=iso"></self-uri><abstract abstract-type="short" xml:lang="en"><p><![CDATA[Abstract The mineral deposits of the Panama microplate are hosted by a composite volcano-plutonic island arc of Late Cretaceous to Quaternary age developed on an oceanic plateau, the Caribbean Large Igneous Province (CLIP), on the western, trailing edge of the Caribbean Plate. Large igneous provinces are formed by gold and chalcophile element-enriched, mantle plume-related magmas, which may explain the strong metal endowment of Panama of about 32 Mt copper and &gt;984 t gold. The progressive collision of the Panama arc with South America since the middle Eocene resulted in deformation and oroclinal bending of the arc and metallogenic belts. In western Panama, the copper-gold belts young from south to north away from the subduction zone, whereas in eastern Panama the belts young from north to south. An Early Arc of late Campanian to Eocene age (71-34 Ma) developed related to northerly subduction of the Farallon Plate. It has submarine Si-Mn-Fe exhalite deposits in the Nombre de Dios and Montijo belts with showings of Au-rich VMS Cu-Zn mineralization. The San Blas porphyry Cu-Au belt formed in eastern Panama (Rio Pito and other porphyry Cu-Au prospects), while the western continuation, offset by 200 km sinistrally to the Azuero Belt, hosts high sulphidation epithermal Au-Cu deposits (Cerro Quema and others) in porphyry lithocaps.The arc migrated to the northern Azuero-Soná belt in the middle to late Eocene with the formation of epithermal Au-Ag-Pb-Cu mineralization, and a porphyry Au prospect (Soná). A Middle Arc developed in the Oligocene to lower Miocene (31-18 Ma) related to the NE-dipping subduction of the Farallon Plate followed by the Nazca Plate. In eastern Panama, the arc formed intermediate sulphidation epithermal Au deposits in high grade breccias (Espiritu Santo de Cana mine) and carbonates (Rio Mogue prospect), and porphyry Cu mineralization (Ipeti). The eastern Panama arc shut down in the lower Miocene as a result of the change of the Nazca Plate convergence to strike slip. The Middle Arc in western Panama, on the northern side of the Central Cordillera, hosts the Petaquilla belt of porphyry Cu (the supergiant Cobre Panama porphyry Cu-Mo-Au-Ag deposit) and epithermal Au (Molejon) deposits, and probably the epithermal Au deposits of the Veraguas belt. The Later Arc of Miocene to Quaternary age (18-0 Ma) of the Central Cordillera of western Panama hosts low sulphidation epithermal Au vein and breccia-hosted deposits (Capira, Remance, Santa Rosa), high sulphidation epithermal Au deposits (Cerro Lloron, Rio Liri), and porphyry Cu deposits (the supergiant Cerro Colorado porphyry Cu-Mo-Au-Ag deposit and the Cerro Chorcha porphyry Cu-Au deposit). Uplift of the young porphyries in the western part of the belt is related to the subduction of the Cocos aseismic oceanic ridge. Deposits formed by Quaternary weathering include lateritic bauxite and iron ore in the Chiriqui-Veraguas belt; heavy mineral Fe-Ti sands in beach/marine placer deposits in the Gulf of Panama; and extensive placer Au deposits in Northern Darien, Darien, Chepo, Coclé, Veraguas, western Azuero-Soná, and many other small deposits.]]></p></abstract>
<abstract abstract-type="short" xml:lang="es"><p><![CDATA[Resumen Los depósitos minerales de la microplaca de Panamá están hospedados en un arco de isla volcáno-plutónico de edad Cretácico tardío al Cuaternario desarrollado en una meseta oceánica, la Gran Provincia Ígnea del Caribe, en el borde occidental de la Placa del Caribe. Las grandes provincias ígneas están formadas por magmas enriquecidos en oro y elementos calcófilos en una columna de convección del manto, lo que puede explicar la fuerte dotación de metal de Panamá de 32 Mt de cobre y &gt;984 t de oro. La colisión progresiva del arco de Panamá con América del Sur desde el Eoceno medio provocó la deformación y la flexión oroclinal del arco y los cinturones metalogénicos. Un Arco Temprano de edad Campaniano tardío al Eoceno (71-34 Ma) se desarrolló por la subducción hacia el norte de la placa Farallón. Tiene depósitos exhálativos submarinos de Si-Mn-Fe en los cinturones Nombre de Dios y Montijo y ocurrencias de mineralización tipo VMS de Cu-Zn rico en Au. El cinturón de Cu-Au de pórfido de San Blas se formó en el este de Panamá (Río Pito), mientras que la continuación occidental, desplazada por 200 km a la izquierda al Cinturón de Azuero, hospeda depósitos epitermales de Au-Cu de alta sulfuración (Cerro Quema) en litocapas de pórfido. El arco migró al cinturón norte de Azuero-Soná en el Eoceno medio a tardío y tiene mineralización epitermal Au-Ag-Pb-Cu y un prospecto de pórfido de Au (Soná). Un Arco Mediano se desarrolló en el Oligoceno al Mioceno inferior (31-18 Ma) relacionado con la subducción al NE de la Placa de Farallón seguida de la Placa de Nazca. En el este de Panamá, el arco formó depósitos de Au epitermales de sulfuración intermedia en brechas de alto grado (Espíritu Santo de Cana) y carbonatos (Rio Mogue), y mineralización de pórfido de Cu (Ipeti). El arco del este de Panamá se terminó en el Mioceno inferior como resultado del cambio de la convergencia de la Placa de Nazca a un margen de falla de rumbo. El Arco Mediano en el oeste de Panamá, en el lado norte de la Cordillera Central, tiene el cinturón de pórfido de Cu de Petaquilla (Cobre Panamá) y depósitos epitermales de Au (Molejón), y probablemente los epitermales de Au del cinturón de Veraguas. El Arco Tardío del Mioceno a Cuaternaria (18-0 Ma) de la Cordillera Central del oeste de Panamá tiene depósitos de vetas y brechas epitermales de Au de baja sulfuración (Capira, Remance, Santa Rosa), depósitos de Au epitermales de alta sulfuración (Cerro Llorón, Río Liri) y depósitos de pórfido Cu-Mo±Au (Cerro Colorado, Cerro Chorcha). El levantamiento de los pórfidos jóvenes en la parte occidental del cinturón está relacionado con la subducción de la cresta oceánica asísmica de Cocos. Los depósitos formados por la meteorización cuaternaria incluyen bauxita laterítica y mineral de hierro en el cinturón de Chiriquí-Veraguas; arenas de minerales pesados de Fe-Ti en depósitos de playa / placer marino en el Golfo de Panamá; y extensos depósitos aluviales de Au.]]></p></abstract>
<kwd-group>
<kwd lng="en"><![CDATA[epithermal gold]]></kwd>
<kwd lng="en"><![CDATA[porphyry copper]]></kwd>
<kwd lng="en"><![CDATA[manganese]]></kwd>
<kwd lng="en"><![CDATA[metallogenic belts]]></kwd>
<kwd lng="en"><![CDATA[Caribbean Large Igneous Province (CLIP)]]></kwd>
<kwd lng="es"><![CDATA[oro epitermal]]></kwd>
<kwd lng="es"><![CDATA[pórfido de cobre]]></kwd>
<kwd lng="es"><![CDATA[manganeso]]></kwd>
<kwd lng="es"><![CDATA[cinturónes metalógenicos]]></kwd>
<kwd lng="es"><![CDATA[Provincia Ígnea Grande del Caribe (CLIP)]]></kwd>
</kwd-group>
</article-meta>
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