<?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>1026-8774</journal-id>
<journal-title><![CDATA[Revista mexicana de ciencias geológicas]]></journal-title>
<abbrev-journal-title><![CDATA[Rev. mex. cienc. geol]]></abbrev-journal-title>
<issn>1026-8774</issn>
<publisher>
<publisher-name><![CDATA[Universidad Nacional Autónoma de México, Instituto de Geología]]></publisher-name>
</publisher>
</journal-meta>
<article-meta>
<article-id>S1026-87742022000100082</article-id>
<article-id pub-id-type="doi">10.22201/cgeo.20072902e.2022.1.1688</article-id>
<title-group>
<article-title xml:lang="es"><![CDATA[Definición del campo de esfuerzos-deformación y sismotectónica del sistema de fallas Morelia-Acambay, México]]></article-title>
<article-title xml:lang="en"><![CDATA[Definition of the stress-deformation field and seismotectonics of the Morelia-Acambay fault system, Mexico]]></article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Mennella]]></surname>
<given-names><![CDATA[Luca]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Garduño-Monroy]]></surname>
<given-names><![CDATA[Víctor Hugo]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Giner Robles]]></surname>
<given-names><![CDATA[Jorge Luis]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Liotta]]></surname>
<given-names><![CDATA[Domenico]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
<xref ref-type="aff" rid="Aaf"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Brogi]]></surname>
<given-names><![CDATA[Andrea]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
<xref ref-type="aff" rid="Aaf"/>
</contrib>
</contrib-group>
<aff id="Af1">
<institution><![CDATA[,Universidad Michoacana de San Nicolás de Hidalgo Instituto de Investigaciones en Ciencias de la Tierra ]]></institution>
<addr-line><![CDATA[Morelia Michoacán]]></addr-line>
<country>México</country>
</aff>
<aff id="Af2">
<institution><![CDATA[,Universidad Autónoma de Madrid Departamento de Geología y Geoquímica ]]></institution>
<addr-line><![CDATA[Madrid ]]></addr-line>
<country>Spain</country>
</aff>
<aff id="Af3">
<institution><![CDATA[,Universidad de Bari &#8220;Aldo Moro&#8221; Dipartimento di Scienze della Terra e Geoambientali ]]></institution>
<addr-line><![CDATA[Bari ]]></addr-line>
<country>Italy</country>
</aff>
<aff id="Af4">
<institution><![CDATA[,Consiglio Nazionale delle Ricerche Instituto di Geoscienze e Georisorce ]]></institution>
<addr-line><![CDATA[Pisa ]]></addr-line>
<country>Italia</country>
</aff>
<pub-date pub-type="pub">
<day>00</day>
<month>00</month>
<year>2022</year>
</pub-date>
<pub-date pub-type="epub">
<day>00</day>
<month>00</month>
<year>2022</year>
</pub-date>
<volume>39</volume>
<numero>1</numero>
<fpage>82</fpage>
<lpage>99</lpage>
<copyright-statement/>
<copyright-year/>
<self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_arttext&amp;pid=S1026-87742022000100082&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_abstract&amp;pid=S1026-87742022000100082&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_pdf&amp;pid=S1026-87742022000100082&amp;lng=en&amp;nrm=iso"></self-uri><abstract abstract-type="short" xml:lang="es"><p><![CDATA[RESUMEN El sistema de fallas Morelia-Acambay (SFMA), situado en la región centro-occidental de la Faja Volcánica Transmexicana (FVTM), se desarrolla como una franja transtensiva de ~30 km de ancho, constituido por fallas E-O y ENE-OSO. La sismotectónica del SFMA controla desde el Mioceno medio (7-9 Ma) la evolución de las cuencas lacustres y depresiones alargadas E-O (Zacapu, Cuitzeo, Morelia y Acambay). Este trabajo estudia el SFMA en su sector centro-occidental enfocándose en la variación espacial del estado de deformación reciente a través del análisis estructural de poblaciones de fallas medidas en el campo y la definición del régimen de esfuerzos regional a partir del análisis de los mecanismos focales de sismos intraplaca someros. Los datos cinemáticos indican que el SFMA se formó a partir de un régimen de deformación con una dirección NE-SO de máxima compresión horizontal (Ey). Hoy en día las fallas NE-SO están asociadas al sistema transtensivo lateral izquierdo, donde las principales morfoestructuras de fallas E-O son paralelas y tienen movimiento normal-direccional izquierdo, mientras que las fallas normales NE-SO responden a la cinemática con una geometría en échelon. La dirección de máxima compresión horizontal (Ey) del SFMA resulta variable pero constantemente en el cuadrante NE-SO, evidenciando una rotación en el sentido horario del campo de esfuerzos que hace que Ey pase de direcciones NNE-SSO en el sector occidental (Pázcuaro-Zacapu-Morelia-Cuitzeo-Acámbaro) hasta direcciones E-O en su sector oriental (Maravatio-Acambay). La integración de los resultados muestra que las trayectorias del campo de deformación reciente y las trayectorias del campo de esfuerzos actual son claramente paralelas, indicando que el régimen neotectónico del Plioceno se ha mantenido constante durante el Cuaternario hasta el presente. Algunas fallas del SFMA son actualmente activas y han sido epicentro de sismos históricos (1858, 1912, 1979 y 2007). Esta definición del campo de deformación y esfuerzos se convierte en una información de primer orden para estudios futuros de paleosismología y el análisis del peligro sísmico. Esta visión espacial permite considerar la orientación de las fallas con respecto a las trayectorias del campo de esfuerzos como uno de los criterios para que dichas fallas se deban considerar o no potencialmente activas. La propuesta más pausible para explicar la deformación transtensiva en el sector central de la FVTM es el modelo de la convergencia oblicua de las placas y la partición del ángulo de subducción de la parte norte de la Trinchera Mesoamericana.]]></p></abstract>
<abstract abstract-type="short" xml:lang="en"><p><![CDATA[ABSTRACT The Morelia-Acambay Fault System (MAFS) is located in the central-western part of the Trans-Mexican Volcanic Belt (TMVB). The MAFS is a 30 km wide-transtensional shear zone made up of E-W and ENE-WSW oriented faults. Since middle Miocene (7-9 Ma), the seismotectonics of this fault system has controlled the evolution of E-W tectonic depressions (Zacapu, Cuitzeo, Morelia, and Acambay), and the lacustrine environments. This paper describes the spatial variation of the state of recent deformation through the structural analysis of fault populations measured in the field and the definition of the regional stress regime from the analysis of the focal mechanisms of shallow intraplate earthquakes. Kinematic data indicate that the MAFS formed under a maximum NE-SW oriented horizontal compression (Ey). Today, the NE-SW faults act as left-lateral oblique slip faults, the main W-E faults as left lateral normal faults; and the NE-SW faults are displayed in en échelon setting. A variation in the direction of Ey is deduced from our data: Ey in fact remains NE-SW oriented in the north-western part of the MAFS, whereas it rotates toward the NNE-SSW and E-W directions in the western (Pázcuaro-Zacapu-Morelia-Cuitzeo-Acámbaro) and eastern (Maravatio-Acambay) MAFS sectors, respectively. Data integration indicates that the main stress axes trajectories remained constant since the Pliocene. Some of the faults of MAFS are presently active, as demonstrated by the distribution of historical epicenters (1858, 1912, 1979 and 2007). These results are of primary relevance for future seismic risk studies in the region. The most reasonable explanation to account for the transtensional regime occurring in the central part of the TMVB is the oblique convergence between the lithospheric plates and, in particular, the partition of the subduction angle in the northern part of the Mesoamerican subduxiton zone.]]></p></abstract>
<kwd-group>
<kwd lng="es"><![CDATA[sistema de fallas Morelia-Acambay]]></kwd>
<kwd lng="es"><![CDATA[México]]></kwd>
<kwd lng="es"><![CDATA[sismos]]></kwd>
<kwd lng="es"><![CDATA[modelo de deslizamiento]]></kwd>
<kwd lng="es"><![CDATA[campo de deformación y esfuerzos]]></kwd>
<kwd lng="en"><![CDATA[Morelia-Acambay geological fault]]></kwd>
<kwd lng="en"><![CDATA[Mexico]]></kwd>
<kwd lng="en"><![CDATA[earthquakes]]></kwd>
<kwd lng="en"><![CDATA[slip model]]></kwd>
<kwd lng="en"><![CDATA[strain and stress field]]></kwd>
</kwd-group>
</article-meta>
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