<?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>S1405-33222005000100065</article-id>
<article-id pub-id-type="doi">10.18268/bsgm2005v57n1a4</article-id>
<title-group>
<article-title xml:lang="es"><![CDATA[El sistema de fallas Taxco-San Miguel de Allende y la Faja Volcánica Transmexicana, dos fronteras tectónicas del centro de México activas durante el Cenozoico]]></article-title>
<article-title xml:lang="en"><![CDATA[The Taxco-San Miguel de Allende fault system and the Transmexican Volcanic belt: two tectonic boundaries in central Mexico active during the Cenozoic]]></article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Alaniz-Álvarez]]></surname>
<given-names><![CDATA[Susana A.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Nieto-Samaniego]]></surname>
<given-names><![CDATA[Ángel Francisco]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
</contrib-group>
<aff id="Af1">
<institution><![CDATA[,Universidad Nacional Autónoma de México Centro de Geociencias ]]></institution>
<addr-line><![CDATA[Querétaro Qro.]]></addr-line>
<country>Mexico</country>
</aff>
<pub-date pub-type="pub">
<day>00</day>
<month>00</month>
<year>2005</year>
</pub-date>
<pub-date pub-type="epub">
<day>00</day>
<month>00</month>
<year>2005</year>
</pub-date>
<volume>57</volume>
<numero>1</numero>
<fpage>65</fpage>
<lpage>82</lpage>
<copyright-statement/>
<copyright-year/>
<self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_arttext&amp;pid=S1405-33222005000100065&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_abstract&amp;pid=S1405-33222005000100065&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_pdf&amp;pid=S1405-33222005000100065&amp;lng=en&amp;nrm=iso"></self-uri><abstract abstract-type="short" xml:lang="es"><p><![CDATA[Resumen La Faja Volcánica Transmexicana se ha reconocido como un arco volcánico que atraviesa México de la costa pacífica al Golfo de México, con actividad volcánica y fallamiento normal desde el Mioceno al Reciente. Se ha planteado que la oblicuidad del arco volcánico con la trinchera es debida a la geometría de la subducción, cuyo ángulo de inclinación varía haciéndose menor hacia el oriente. Por otra parte, se ha propuesto que la Faja Volcánica Transmexicana se ubica sobre una zona de debilidad preexistente. En este trabajo se discuten los eventos de deformación cenozoicos ocurridos al norte y sur de la Faja Volcánica Transmexicana para identificar el tiempo en el que ésta actuó como zona de discontinuidad y también para determinar la presencia del campo de deformación precursor del emplazamiento del arco volcánico. Utilizamos como una de las referencias el sistema de fallas Taxco-San Miguel de Allende, ya que es la única estructura reconocida que atraviesa el arco volcánico y de la cual se ha estudiado con detalle su evolución estructural. En la Mesa Central, al norte de la Faja Volcánica Transmexicana, la deformación extensional postlaramídica ha ocurrido en tres eventos relativamente discretos durante el Eoceno, Oligoceno y Mioceno-Reciente. Los tres eventos liberaron extensión en dos direcciones principales horizontales y acortamiento vertical. Del evento eocénico las direcciones principales de deformación son poco conocidas. El evento del Oligoceno fue el más importante y la mayor extensión fue de 20% hacia el ENE-WSW; en el tercer evento, activo desde el Mioceno, la deformación ha estado concentrada principalmente en la Faja Volcánica Transmexicana y en su límite norte con la Mesa Central. La deformación extensional oligocénica de la Mesa Central migró hacia el poniente hasta culminar con la apertura del Golfo de California y hacia el sur-oriente hacia la Faja Volcánica Transmexicana. En la Sierra Madre Oriental, al oriente de la Mesa Central y norte de la Faja Volcánica Transmexicana, la deformación cenozoica ha sido mínima. Al sur de la Faja Volcánica Transmexicana, en la región de Taxco, Gro., se han documentado dos eventos de deformación postlaramídicos acomodados principalmente por fallas laterales NW-SE y N-S. El primero ocurrió durante el Eoceno tardío con una dirección de extensión NNW-SSE y acortamiento hacia el ENE-WSW. El segundo evento ocurrió durante el Oligoceno temprano, la extensión máxima ocurrió hacia el NE-SW y el acortamiento hacia el NW-SE, ambos eventos migraron hacia el oriente. La mayor parte de las rocas volcánicas a lo largo de la Faja Volcánica Transmexicana son rocas volcánicas miocénicas, sin embargo se ha reportado la presencia de rocas volcánicas oligocénicas en la mitad inferior del relleno de la cuenca de México; por otro lado este arco volcánico se encuentra alojado en cuencas tectónicas limitadas por fallas mayores. Para la cuenca de México se infiere que la actividad de las fallas que limitan a la Faja Volcánica Transmexicana inició en el Eoceno tardío. Se concluye que desde el Eoceno el estilo de la deformación de la Mesa Central y de la Sierra Madre del Sur ha sido distinto, esto implica la existencia de una zona de despegue entre estas provincias. A partir del Oligoceno la actividad de las fallas laterales en la Sierra Madre del Sur produjeron acortamiento en la dirección principal NW-SE, generando en la zona de despegue una deformación con extensión oblicua a la dirección del arco volcánico y una componente de cizalla izquierda. Los eventos de deformación anteriores al Mioceno formaron una zona de despegue en la cual se desarrolló la cuenca de México y además en esa misma zona se canalizaron hacia la superficie los magmas que formaron la parte central de la Faja Volcánica Transmexicana.]]></p></abstract>
<abstract abstract-type="short" xml:lang="en"><p><![CDATA[Abstract The Transmexican Volcanic Belt has been recognized as a major volcanic arc which crosses Mexico from the Pacific coast to the Gulf of Mexico. This volcanic arc had normal faulting and volcanism since Miocene. It has suggested that the volcanic arc is not parallel to the Mesoamerican trench because the subduction angle varies being gentler to the east. Also it has been proposed a preexisting zone of weakness below the Transmexican Volcanic Belt. In this work we present the deformation events that have been recorded north and south of the Transmexican Volcanic Belt in order to identify the time in which this zone began to be a crustal discontinuity and also to determine the deformation field precursor of the emplacement of the volcanic arc. We use as a reference the studies along the Taxco-San Miguel de Allende because it is the only recognized structure that crosses the Transmexican Volcanic Belt. In the Mesa Central, north of the Transmexican Volcanic Belt, the postlaramidic deformation occurred in three extensional events during the Eocene, Oligocene and Miocene to Recent. The three events liberated extension in two horizontal directions and shortening in the vertical direction. The Eocene event was extensional but the directions of the principal extensions are not very well known. The Oligocene event was the most important; it extended 20% in the ~ENE-WSW direction. This event migrated toward west, finishing in the opening of the California Gulf, and also migrated toward south-southeast to the Transmexican Volcanic Belt. The most recent event, active since middle Miocene, has been developed in the Transmexican Volcanic Belt and its northern boundary. In the Sierra Madre Oriental, east of the Mesa Central and north of the Transmexican Volcanic Belt, the Cenozoic deformation has been minimum. South of the Transmexican Volcanic Belt, in the Taxco region, there were two postlaramidic deformation events, mainly liberated by NW-SE and N-S lateral faults. The first one occurred in late Eocene with a NNW-SSE horizontal extension direction and shortening to the ENE-WSW. The second event was early Oligocene with a maximum extension to the NE-SW and shortening to the NW-SE, both migrated toward east. Most of the volcanic rocks along the Transmexican Volcanic Belt are Miocene, however it has reported Oligocene mafic volcanic rocks in the middle of the Mexico basin. Besides, this volcanic arc is located into tectonic basins bounded by major faults. In the case of the Mexico basin, faulting initiated in late Eocene time. It is concluded that since the Eocene, the deformation style was different in the Mesa Central and in the Sierra Madre del Sur, this implies the presence of a detachment zone between these provinces. From the Oligocene the lateral faults activity in the Sierra Madre del Sur produced shortening in the NW-SE principal direction, generating an oblique-extension with a left-lateral component within the zone now occupied by the central part of the Transmexican Volcanic Belt. The pre-Miocene deformation events formed a detachment zone in which the Mexico basin was developed, also through this zone was canalized the magmas surface forming the central part of the Transmexican Volcanic Belt.]]></p></abstract>
<kwd-group>
<kwd lng="es"><![CDATA[Faja Volcánica Transmexicana]]></kwd>
<kwd lng="es"><![CDATA[fallas mayores]]></kwd>
<kwd lng="es"><![CDATA[cenozoico]]></kwd>
<kwd lng="es"><![CDATA[reactivación]]></kwd>
<kwd lng="en"><![CDATA[Transmexican Volcanic Belt]]></kwd>
<kwd lng="en"><![CDATA[major fault]]></kwd>
<kwd lng="en"><![CDATA[Cenozoic]]></kwd>
<kwd lng="en"><![CDATA[reactivation]]></kwd>
</kwd-group>
</article-meta>
</front><back>
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