<?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>S1405-33222017000300669</article-id>
<article-id pub-id-type="doi">10.18268/bsgm2017v69n3a9</article-id>
<title-group>
<article-title xml:lang="en"><![CDATA[Paleostress and Geometric Analysis of the Southern Rio Grande Rift in the Northern Chihuahua Trough: Franklin and Potrillos Mountains as examples]]></article-title>
<article-title xml:lang="es"><![CDATA[Análisis geométrico y de paleoesfuerzos de la parte sur del rift del Río Grande al norte del surco de Chihuahua: ejemplo de las montañas Franklin y Potrillos]]></article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Carciumaru]]></surname>
<given-names><![CDATA[Dana]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Ortega]]></surname>
<given-names><![CDATA[Roberto]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
</contrib-group>
<aff id="Af1">
<institution><![CDATA[,Orbis Consultores en Geología y Geofísica SC  ]]></institution>
<addr-line><![CDATA[ ]]></addr-line>
<country>México</country>
</aff>
<aff id="Af2">
<institution><![CDATA[,CICESE  ]]></institution>
<addr-line><![CDATA[ ]]></addr-line>
<country>México</country>
</aff>
<pub-date pub-type="pub">
<day>00</day>
<month>00</month>
<year>2017</year>
</pub-date>
<pub-date pub-type="epub">
<day>00</day>
<month>00</month>
<year>2017</year>
</pub-date>
<volume>69</volume>
<numero>3</numero>
<fpage>669</fpage>
<lpage>689</lpage>
<copyright-statement/>
<copyright-year/>
<self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_arttext&amp;pid=S1405-33222017000300669&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_abstract&amp;pid=S1405-33222017000300669&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_pdf&amp;pid=S1405-33222017000300669&amp;lng=en&amp;nrm=iso"></self-uri><abstract abstract-type="short" xml:lang="en"><p><![CDATA[Abstract We present a deformation history of Potrillo and Franklin Mountains in El Paso, TX, using paleostress and geometric analysis. Application of paleostress and geometric analysis shows that low angle normal faults exposed at Anthony Gap and regions to the north of the Franklin Mountains record differential displacement that increase from North to South along the strike. As displacement on the faults increases, the hanging walls of the faults rotated counterclockwise and transverse faults which accommodate flexure developed as a consequence of that movement. The hanging wall of the faults rotates in a counter-clockwise direction and the transverse faults accommodate the developing flexion. The transverse faults are thought as the result of an isostatic rebound of the footwalls due to the tectonic denudation of the hanging wall. The average elastic thickness of the lithosphere is 23 km. This flexure and isostatic rebound take place in a late stage which was concurrently developed to the mountain range genesis. However, transverse faults do not cut the low angle faults suggesting that the two sets of faults are part of the same system. Increase in displacement along the faults is mirrored by an overall increase in elevation in the Franklin Mountains, which suggests that fault activity is critical to the uplift of the mountain range with respect to the surrounding basins. Estimates of the stresses from small scale faults in the Franklin Mountains indicate that the greatest extension direction was ENE-WSW and the greatest compression direction was subvertical. Low angle normal faults in the Potrillo Mountains belong to two different deformation episodes. The first family of faults occurs along the eastern side of the mountain range. This is cut by younger NNW trending normal faults which bound the range at the East. Fault slip analysis, calcite vein arrays and the geometry of the faults indicate that the first set of low angle normal faults record NNE directed extension and vertical shortening rotated approximately sixty degrees in a counter-clockwise sense as inferred from the trend of the east Potrillo fault. The second generation of faults have strike parallel slickenlines which trend to the ESE. Fault slip inversion indicates that these faults were formed in response to left oblique slip, with a moderately Southeast plunging shortening direction and a shallowly plunging WNW trending extension direction. These observations are most consistent with the first low angle faults in the Potrillo Mountains tracking an early phase of extension distinct from low angle faults in the Franklin Mountains. The second set of faults may have formed in a similar stress field to that recorded in the Franklin Mountains. The combined dataset is most consistent with two phases of extension across low angle normal fault in the southern Rio Grande rift, the first was caused by NNE extension, and the second by ESE directed extension.]]></p></abstract>
<abstract abstract-type="short" xml:lang="es"><p><![CDATA[Resumen Presentamos un estudio de la deformación de las montañas Potrillo y Franklin, en El Paso Texas, usando un análisis geométrico y de paleoesfuerzos. Utilizando análisis geométrico se muestra que las fallas normales de bajo ángulo expuestas en Anthony Gap y en las Montañas Franklin registraron un desplazamiento diferencial, con aumento de los desplazamientos de norte a sur a lo largo de las fallas. Las partes superiores de las fallas giran en un sentido contrario a las manecillas del reloj y se desarrollan fallas transversales que acomodan la flexión. Se cree que las fallas transversales resultan del rebote isostático del piso de la falla debido a la denudación tectónica del techo de la falla. El espesor promedio de la litosfera es de aproximadamente 23 km. Esta flexión y el rebote isostático ocurren en una etapa tardía de la extensión la cual ocurre paralelamente a la formación de las cordilleras. Sin embargo, las fallas transversales no cortan a las fallas de bajo ángulo, sugiriendo que los dos pares de fallas se forman durante el mismo evento de deformación. El aumento de los desplazamientos en las fallas se refleja en un aumento general de la elevación de las Montañas Franklin, sugiriendo que las fallas son críticas para el levantamiento de la cordillera con respecto a las cuencas adyacentes. El análisis del estado de esfuerzos de las fallas de pequeña escala en las Montañas Franklin nos indica que la máxima dirección de extensión era este-noreste/oeste-suroeste y la máxima dirección de compresión era subvertical. Las fallas normales de bajo ángulo en Las Montañas Potrillo pertenecen a dos episodios de deformación diferentes. La primera familia de fallas se produce a lo largo del lado oriental de la cordillera. Ésta es cortada por fallas normales más jóvenes con dirección norte-noroeste que limitan la cordillera de las Montañas Potrillo. El análisis de las fallas de deslizamiento y la geometría de las fallas indican que el primer conjunto de fallas normales de bajo ángulo registró una extensión norte-noreste y un acortamiento vertical girado aproximadamente sesenta grados en un sentido contrario a las manecillas del reloj, el cual fue inferido a partir del rumbo de las fallas en la parte este de la falla Potrillo (la cordillera que limita una falla de ángulo alto). La inversión de fallas transtensionales indica que estas fallas se forman en respuesta a un deslizamiento oblicuo de falla izquierda, con dirección de acortamiento moderadamente basculado al sureste, también basculando al oeste superficialmente, mientras que al noroeste el rumbo es en la dirección de extensión. Estas observaciones son más consistentes con las primeras fallas de bajo ángulo en las Montañas Potrillo siguiendo una primera fase de extensión distinta a las fallas de bajo ángulo en las Montañas Franklin. El segundo conjunto de fallas puede haberse formado en un campo de extensión similar a las Montañas Franklin. El conjunto de datos combinados es más consistente con las dos fases de extensión a través de fallas normales de bajo ángulo en el sur del Rift Rio Grande.]]></p></abstract>
<kwd-group>
<kwd lng="en"><![CDATA[geometric analysis]]></kwd>
<kwd lng="en"><![CDATA[low angle normal faults]]></kwd>
<kwd lng="en"><![CDATA[paleostress]]></kwd>
<kwd lng="en"><![CDATA[Rio Grande rift]]></kwd>
<kwd lng="es"><![CDATA[Análisis geométrico]]></kwd>
<kwd lng="es"><![CDATA[fallas normales de bajo ángulo]]></kwd>
<kwd lng="es"><![CDATA[paleoesfuerzos]]></kwd>
<kwd lng="es"><![CDATA[Rio Grande Rift]]></kwd>
</kwd-group>
</article-meta>
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