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Boletín de la Sociedad Geológica Mexicana
Print version ISSN 1405-3322
Bol. Soc. Geol. Mex vol.57 n.3 Ciudad de México Dec. 2005
https://doi.org/10.18268/bsgm2005v57n3a5
Artículos
Magmatismo y tectónica en la Sierra Madre Occidental y su relación con la evolución de la margen occidental de norteamérica
Magmatism and tectonics of the Sierra Madre Occidental and its relation with the evolution of western North America
1Centro de Geociencias, Universidad Nacional Autónoma de México, Campus Juriquilla, Apartado postal 1-742, Querétaro, Qro., 76001, México
2Estación Regional del Noroeste, Instituto de Geología, Universidad Nacional Autónoma de México, L.D. Colosio y Madrid S/N, Campus Unison, Apartado Postal 1039, Hermosillo, Son., 83000, México
3School of Earth Sciences and Geography, Kingston University, Penrhyn Road, Kingston upon Thames, Surrey KT1 2EE, Inglaterra
La Sierra Madre Occidental (SMO) es el resultado de diferentes episodios magmáticos y tectónicos durante el Cretácico-Cenozoico, asociados a la subducción de la placa Farallón debajo de la placa de Norteamérica y a la apertura del Golfo de California. La estratigrafía de la SMO consta de cinco conjuntos ígneos principales: (1) rocas plutónicas y volcánicas del Cretácico Superior-Paleoceno y (2) rocas volcánicas andesíticas y, en menor medida, dacítico-riolíticas del Eoceno, tradicionalmente agrupadas en el denominado "Complejo Volcánico Inferior" (CVI); 3) ignimbritas silícicas emplazadas en su mayoría en dos pulsos, en el Oligoceno temprano (32-28 Ma) y el Mioceno temprano (24-20 Ma), y agrupadas en el Supergrupo Volcánico Superior; 4) coladas basáltico-andesíticas transicionales extravasadas después de cada pulso ignimbrítico, correlacionadas con las "Andesita-Basálticas del Sur de la Cordillera" (SCORBA por sus siglas en inglés); 5) volcanismo postsubducción constituido por coladas de basaltos alcalinos e ignimbritas emplazados en diferentes episodios del Mioceno tardío, Plioceno y Cuaternario, y que se relacionan con la separación de Baja California del continente. Los productos de todos estos episodios magmáticos, parcialmente superpuestos entre sí, cubren a su vez un basamento heterogéneo pobremente expuesto con edades del Precámbrico y Paleozoico en la parte norte (Sonora y Chihuahua) y del Mesozoico en el resto de la SMO.
La deformación Laramide afectó moderadamente a las rocas más antiguas del CVI (~101 a ~89 Ma) en Sinaloa y a rocas volcánicas del Maastrichtiano en Chihuahua central. En su fase final, durante el Paleoceno y Eoceno temprano, se desarrollaron fracturas de tensión ~E-W a ENE-WSW que hospedan los principales depósitos de pórfidos cupríferos de la SMO. La tectónica extensional inició por lo menos en el Oligoceno en toda la mitad oriental de la SMO, provocando la formación de grábenes limitados por fallas de alto ángulo que se han referido como el Basin andRange mexicano. En el Mioceno temprano y medio la extensión migró hacia el occidente. En Sonora central esta deformación llegó a exhumar la corteza inferior, mientras que en el resto de la SMO no rebasó el 20%. En el Mioceno tardío la extensión se concentró en la franja más occidental de la SMO, adyacente al Golfo de California, donde produjo sistemas de fallas NNW que limitan un conjunto de semigrábenes con vergencia tanto al ENE como al WSW con zonas de acomodo transversales. Es importante notar que buena parte de la extensión se dio mientras la subducción de la placa Farallón era todavía activa.
Los estudios geoquímicos y petrológicos indican que las rocas de la SMO forman un conjunto típicamente calcial-calino, caracterizado por concentraciones de potasio intermedias a altas y enriquecimiento relativamente bajo en Fe. El volcanismo del Eoceno tardío al Mioceno es claramente bimodal con los miembros silícicos dominantes sobre los máficos. Las relaciones iniciales de 87Sr/86Sr están comprendidas, en su mayoría, en el rango de 0.7041 a 0.7070, y los valores iniciales de eNd entre +2.3 y -3.2, intermedios entre los del manto y de la corteza. Con base en los datos isotópicos de rocas volcánicas y xenolitos de algunos pocos sitios de la SMO se han propuesto modelos contrastantes para la génesis del volcanismo silícico. Por una parte las ignimbritas silícicas se han relacionado a un proceso de cristalización fraccionada de magmas máficos del manto con poca o nula intervención de la corteza; por otra parte, se ha considerado que estas rocas son en gran medida el resultado de fusión parcial de la corteza calentada por el arribo de basaltos del manto. Diferentes evidencias sugieren que en la mayoría de los casos ambos procesos hayan ocurrido en la SMO y que la petrogénesis de las ignimbritas es dominada por procesos de mezcla y asimilación-cristalización fraccionada a gran escala inducida por el emplazamiento de cantidades significativas de magmas máficos procedentes del manto.
Los datos geofísicos indican la presencia de una corteza que alcanza los 55 km de espesor en el núcleo relativamente no extendido de la parte norte de la SMO, mientras que más al este el espesor es de ~40 km. El espesor anómalo de la parte central de la SMO sugiere la presencia de una corteza inferior fuertemente intrusionada por magmas máficos. En la franja costera del Golfo de California los espesores son de ~25 km, lo que implica una extensión superior a 100%. El manto superior por debajo de la SMO se caracteriza por una amplia anomalía de baja velocidad, típica del manto aste-nosférico, que se extiende desde la provincia Basin and Range de Estados Unidos.
La revisión de la historia magmática y tectónica de la SMO presentada en este trabajo indica que esta provincia geológica es el resultado de la evolución del sistema de subducción Cretácico-Cenozoico del occidente de Norteamérica. En particular la SMO, como gran provincia ígnea silícica oligo-miocénica, está ligada a los eventos ocurridos en el ocaso de la subducción de la placa Farallón y puede verse como el precursor de la apertura del Golfo de California. El mecanismo responsable de los pulsos ignimbríticos se relaciona esencialmente con la remoción de la placa Farallón desde la base de la placa de Norteamérica después del término de la orogenia Laramide. Este proceso involucra el aumento rápido del ángulo de subducción y, posiblemente, el despegue de la parte más profunda de la placa subducida como consecuencia del arribo de litósfera oceánica cada vez más joven y flotante en la paleotrinchera y, finalmente, la interacción directa entre las placas Pacífico y Norteamérica.
Palabras clave: Sierra Madre Occidental; Golfo de California; magmatismo continental; grandes provincias ígneas silícicas; tectónica extensional; dinámica de la subducción
The Sierra Madre Occidental (SMO) is the result of Cretaceous-Cenozoic magmatic and tectonic episodes related to the subduc-tion of the Farallon plate beneath North America and to the opening of the Gulf of California. The stratigraphy of the SMO consists of five main igneous complexes: (1) Late Cretaceous to Paleocene plutonic and volcanic rocks and (2) Eocene andesites and lesser rhyolites, traditionally grouped into the so-called "Lower Volcanic Complex" (LVC); (3) silicic ignimbrites mainly emplaced during twopulses of Oligocene (~32-28Ma) and early Miocene (~24-20Ma) ages and grouped into the "Upper Volcanic Supergroup"; 4) transitional basaltic-andesitic lavas that erupted after each ignimbritic pulse and correlated with the Southern Cordillera Basaltic-Andesite (SCORBA) of the southwestern USA; and 5) postsubduction volcanism consisting of alkaline basalts and ignimbrites emplaced in the late Miocene, Pliocene and Pleistocene, directly related to the separation of Baja California from the Mexican mainland. The products of all these magmatic episodes, partially overlapped, cover a poorly exposed, heterogeneous basement with Precambrian to Paleozoic ages in the northern part (Sonora and Chihuahua) and Mesozoic ages beneath the rest of the SMO.
The oldest rocks of the LVC (~101 to ~89 Ma) in Sinaloa, and Maastrichtian volcanics of the LVC in central Chihuahua are af-fected by moderate contractile deformation ascribed to the Laramide orogeny. In the final stages of this deformation cycle, during the Paleocene and Early Eocene, ~E-W to ENE-WSW-trending tension fractures formed within the LVC, along which world-class porphyry copper deposits of the SMO were emplaced. Extensional tectonics began as early as the Oligocene in the whole eastern half of the SMO, forming grabens bounded by high-angle normal faults, traditionally referred to as the southern (or Mexican) Basin and Range province. In the early to middle Miocene, extension migrated westward. In northern Sonora the deformation was sufficiently intense to exhume lower crustal rocks, whereas in the rest of SMO crustal extension did not exceed 20%. In the late Miocene time, extension became focussed in the westernmost part of the SMO, adjacent to the Gulf of California, where NNW normal fault systems produced both ENE and WSW tilt domains separated by transverse accomodation zones. It is worth noting that most of the extension occurred when subduction of the Farallon was still active off Baja California.
Geochemical data show that the SMO rocks form a typical calc-alkaline rhyolite suite with intermediate to high Kand relatively low Fe content. late Eocene to Miocene volcanism is clearly bimodal, but silicic compositions are dominant. Initial 87Sr/86Sr ratios mostly range between 0.7041 and 0.7070, and initialeNd values are generally intermediate between crustandmantle values (+2.3 and -3.2). Based on isotopic data of volcanic rocks and crustal xenoliths from a few sites in the SMO, contrasting models for the genesis of the silicic volcanism have been proposed. A considerable body ofwork led by Ken Cameron and others considered the mid-Tertiary SMO silicic magmas to have formed by fractional crystallization of mantle-derived mafic magmas with little (<15%) or noparticipation of the crust. In contrast, other workers have suggested the rhyolites, taken to the extreme case, could be entirely the result of partial melting of the crust in response to thermal and material input from basaltic underplating. Several lines of evidence suggest that SMO ignimbrite petrogenesis involved large-scale mixing and assimilation-fractional crystallization processes of crustal and mantle-derived melts.
Geophysical data indicate that the crust in the unextended core of the northern SMO is ~55 km-thick, but thins to ~40 km to the east. The anomalous thickness in the core of the SMO suggests that the lower crust was largely intruded by mafic magmas. In the westernmost SMO adjacent to the Gulf of California crustal thickness is ~25 km, implying over 100% of extension. However structures at the surface indicate no more than about 50%. The upper mantle beneath the SMO is characterized by a low velocity anomaly, typical of the asthenosphere, which also occurs beneath the Basin and Range province of western U.S.
The review of the magmatic and tectonic history presented in this work suggests that the SMO is the result of the Cretaceous- Cenozoic evolution of the western North America subduction system. In particular, the Oligo-Miocene SMO is viewed as a silicic large igneous province formed as the precursor to the opening of the Gulf of California during the final stages of the subduction of the Farallon plate. The mechanism responsible for the generation of the ignimbrite pulses seems related to the removal of the Farallon plate from the base of the North American plate after the end of the Laramide orogeny. The rapid increase in the subduction angle due to slab roll-back resulted in extension of the continental margin and, possibly, the detachment of the deeper part of the subducted slab as younger and buoyant oceanic lithosphere arrived at the paleotrench, eventually leading to direct interaction between the Pacific and North American plates.
Key words: Sierra Madre Occidental; Gulf of California; continental magmatism; silicic large igneous provinces; extensional tectonics; subduction dynamics
Agradecimientos
Parte de los resultados reportados en este trabajo para el norte y el sur de la SMO son producto de los proyectos CONACyT I29887 T (M. Valencia) y P-0152 T (L. Ferrari). El Centro de Geociencias, UNAM, apoyó trabajo de campo relacionado con este proyecto en Chihuahua, Zacatecas y Jalisco durante 2004. Agradecemos a la Sociedad Geológica Mexicana y los editores de este volumen por haber estimulado la realización de este trabajo, así como las revisiones exahustivas de Chris Henry y Ángel Nieto Samaniego y la revisión informal de Enrique González Torres y Gabriel Chávez Cabello que contribuyeron a mejorar la claridad del trabajo final.
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Recibido: 04 de Febrero de 2005; Revisado: 23 de Octubre de 2005; Aprobado: 25 de Noviembre de 2005
Este es un artículo publicado en acceso abierto bajo una licencia Creative Commons
