Cenozoic volcanism and extension in northwestern Mesa Central, Durango, México

Volcanismo cenozoico y extensión al noroeste de la Mesa Central, Durango, México

Isidro Loza-Aguirre^{1, 2,*}, Ángel F. Nieto-Samaniego¹, Susana A. Alaniz-Álvarez¹, Carlos Ortega-Obregón¹

¹ Centro de Geociencias, Universidad Nacional Autónoma de México, Campus Juriquilla, Boulevard Juriquilla No. 3001, Juriquilla, Querétaro, México, CP 76230. ^*isla@geociencias.unam.mx

Manuscript received: April 4, 2012.
Corrected manuscript received: June 7, 2012.
Manuscript accepted: June 6, 2012.

Abstract

The Santiago Papasquiaro region is located in the northwest portion of the Mesa Central and is characterized by Tertiary Sierra Madre Occidental lithology. Geologic mapping and dating of key units using U-Pb laser ablation method on zircons has identified three different lithostratigraphic groups. These include: (1) early Eocene felsic volcanic rocks, consisting of the Antigua ignimbrite [51.75 +0.35/-0.45 Ma]; (2) late Eocene - early Oligocene felsic to intermediate volcanic rocks, consisting of the Altamira ignimbrite [38.8 ± 1.0 Ma], El Cazadero andesite [ages of 37.2 +0.30/-0.40 Ma and 35.95 +0.45/-0.5 Ma], a dioritic intrusion, the Venadita rhyolite, Puente Negro ignimbrite [34.0 +0.50/-0.70 Ma], Los Fresnos ignimbrite and Balín ignimbrite [33.2 +0.50/-0.20 Ma]; and (3) late Oligocene to Quaternary sedimentary and volcanic mafic rocks comprising the Santiago sedimentary formation, basalts equivalent to Metates Formation and Neogene to Quaternary continental non-consolidated deposits. Within the studied area, the main volcanic pulse of the Sierra Madre Occidental volcanic province corresponds to the second group, which lasted ca. 5 Ma. Older rocks are represented by a single outcrop of the Antigua ignimbrite, and the younger units are mainly continental clastic sediments intercalated with sporadic mafic alkaline volcanic rocks that record a major change in the tectonic regime. Extension that began in late Eocene - Oligocene gradually tilted the late Eocene – early Oligocene volcanic sequence and formed the NNW-trending Santiago Papasquiaro half-graben, which is the northernmost and earliest structure of the Río Chico-Otinapa graben. NW-striking faults of the San Luis-Tepehuanes fault system were synchronous with the development of the Santiago Papasquiaro half-graben. The deformation propagated gradually to the south, forming the NNW Río Chico-Otinapa graben by the early-middle Miocene, and to the east-southeast in the Santiaguillo graben. A recent minor extensional deformation accommodated by NE-striking faults was probably related to seismic deformation of the Nuevo Ideal zone, approximately 40 km southeast of the study area.

Keywords: Cenozoic, stratigraphy, extension, Mesa Central, Sierra Madre Occidental, graben system.

La región de Santiago Papasquiaro está localizada en el noroeste de la Mesa Central y está caracterizada por litología terciaria de la Sierra Madre Occidental. Mediante la cartografía geológica del área y la realización de fechamientos isotópicos por el método U-Pb de ablación láser en circones se reconocieron tres grupos litoestratigráficos. Estos incluyen: (1) rocas volcánicas félsicas del Eoceno temprano, que consiste de la ignimbrita Antigua [51.75 +0.35/-0.45 Ma]; (2) rocas volcánicas félsicas a intermedias del Eoceno tardío-Oligoceno temprano, que incluye a la ignimbrita Altamira [38.7 ± 1.0 Ma], la andesita El Cazadero [edades de 37.2 +0.30/-0.40 Ma y 35.95 +0.45/-0.5 Ma], una intrusión diorítica, la riolita Venadita, la ignimbrita Puente Negro [34.0 +0.50/-0.70 Ma], la ignimbrita Los Fresnos y la ignimbrita Balín [33.2 +0.50/-0.20 Ma]; y (3) rocas sedimentarias continentales y volcánicas máficas del Oligoceno tardío-Cuaternario que comprenden a la formación Santiago, basaltos equivalentes a la Formación Metates y sedimentos continentales no consolidados del Neógeno-Cuaternario. En la zona de estudio el pulso volcánico más importante de la provincia volcánica de la Sierra Madre Occidental corresponde al segundo grupo, que duró ca. 5 Ma. Las rocas más antiguas están representadas por un afloramiento de la ignimbrita Antigua, y las unidades más jóvenes son principalmente sedimentos clásticos continentales intercalados con esporádicas rocas volcánicas máficas alcalinas, que registran un cambio importante en el régimen tectónico. La extensión que comenzó en el Eoceno tardío-Oligoceno basculó gradualmente a la secuencia volcánica del Eoceno tardío-Oligoceno temprano y formó al semigraben de Santiago Papasquiaro de rumbo NNW, que es la estructura más septentrional, y primera en desarrollarse del graben de Río Chico-Otinapa. La actividad en las fallas de rumbo NW del Sistema de fallas San Luis-Tepehuanes fue sincrónica con el desarrollo del semigraben de Santiago Papasquiaro. La deformación se propagó gradualmente hacia el Sur, desarrollándose el graben de Río Chico-Otinapa de rumbo NNW durante el Mioceno temprano-medio, y hacia el Este-Sureste en el graben de Santiaguillo. La deformación menor extensional reciente acomodada por fallas de rumbo NE, estuvo relacionada probablemente con la actividad sísmica en la zona de Nuevo Ideal, 40 km al sureste del área de estudio.

Palabras clave: Cenozoico, Estratigrafía, Extensión, Mesa Central, Sierra Madre Occidental, sistema de graben.

1. Introduction

Santiago Papasquiaro is located in central Mexico in the northwestern portion of the Mesa Central physiographic province (MC) (Nieto-Samaniego et al., 2005), almost 130 km northwest from Durango City (Figure 1 A, B). The most recent geological studies in the zone are the Santiago Papasquiaro geological maps published by the Servicio Geológico Mexicano at scales of 1:250000 (Mungía-Rojas et al., 2000) and 1:50000 (Luévano-Pinedo et al., 2003), as well as the study of Nieto-Samaniego et al. (2012) about the stratigraphy, deformation and seismicity in the Santiaguillo graben, located 40 km southeast of Santiago Papasquiaro (Figure 1 C). This region is characterized by outcrops of Tertiary volcanic rocks of the Sierra Madre Occidental volcanic province (SMOc) (Ferrari et al., 2005) (Figure 1C and 2).

Regional structures in the study area strike from NE to NW (Mungía-Rojas et al., 2000; Luévano-Pinedo et al., 2003; Nieto-Samaniego et al., 2005). NE faults are poorly known, although in some regions of the SMOc they act as transfer zones between domains of different tilts (Henry and Aranda-Gómez, 2000). NNE to NNW-striking grabens are located within the Sierra Madre Occidental (SMOc) and the Mesa Central (MC), one of the most noticeable of these structures is the ~150 km long Río Chico-Otinapa graben (RCOG) (Figures 1 and 3) (Aranda-Gómez et al., 1997; Henry and Aranda-Gómez, 2000). In previous studies the NW faults have been considered part of the San Luis-Tepehuanes Fault System (SLTFS) (Nieto-Samaniego et al., 2005, 2012). The SLTFS is a major structure that crosses central Mexico from San Luis de La Paz, Gto., to Tepehuanes, Dgo., consisting of normal faults that had been active from Eocene to Quaternary time (Figure 1 C). In the NW segment, southeast of Santiago Papasquiaro, the SLTFS had associated Quaternary magmatism and seismic activity (Figures 1 C and 2) (Nieto-Samaniego et al., 2005, 2012). Part of the northwestern segment of the SLTFS intersects the northernmost portion of the RCOG within the study area (Figures 1 and 3).

Representative volcanic units of the study area were dated with U-Pb on zircons using a spot of 23 microns of laser ablation attached to an inductively coupled plasma mass spectrometer (LA-ICP-MS). All of these ages were obtained at the Laboratorio de Estudio Isotópicos (LEI), Centro de Geociencias, UNAM. Detailed methodology of this technique and data reduction procedures used in this laboratory are described by Solari et al. (2010) and Solari and Tanner (2011). Due to the lack of common lead (²⁰⁴Pb) values (e.g., from feldspars) of these rocks, we use the algebraic method of correction of Andersen (2002) with a careful analysis on Tera-Wasserburg concordia diagrams. Analyses that show evidence of inclusions or lead loss were discarded during data reduction procedure and only the most concordant ages were used to determine the mean age using the Zircon Age Extractor script from Ludwig (2008).

2. Geological setting

In this portion of the MC the lithological record includes Paleozoic to Quaternary rocks (Figure 2). Gneiss and schist, with a metamorphic age of ~252 Ma (Ar-Ar on moscovite, Iriondo et al., 2003), crop out ~100 km to the east-southeast of Santiago Papasquiaro, and schist with a metamorphic age of 326 ± 26 Ma (K-Ar, Araujo-Mendieta and Arenas-Partida, 1986) crops out ~100 km to the north. Unconformably overlying the Paleozoic units are clastic and carbonate Jurassic and Cretaceous marine rocks (Zaldívar and Garduño, 1984; Aranda-García et al., 1987; Contreras-Montero et al., 1988; Córdoba, 1988) that were folded and thrusted during the Laramide Orogeny (Nieto-Samaniego et al., 2005). These Mesozoic rocks are covered by continental conglomerates, Eocene to Miocene mainly acid to intermediate volcanic rocks of the SMOc, and Oligocene-Miocene to Pleistocene basic volcanic rocks (McDowell and Keizer, 1977; Swanson et al., 1978; McDowell and Clabaugh, 1981; Córdoba, 1988; Aguirre-Díaz and McDowell, 1991; Mungía-Rojas et al., 2000; Luhr et al., 2001; Ferrari et al., 2005; Nieto-Samaniego et al., 2005; Solé et al., 2007; Nieto-Samaniego et al., 2012). Miocene to Quaternary alluvial and lacustrine deposits fill continental basins, and Quaternary alkaline basalts top the lithologic column (Figure 2) (Nieto-Samaniego et al., 2005).

The Mesa Central has undergone extension since the late Eocene (Nieto-Samaniego et al., 2005). Previous studies have defined two main events in this region: the first one occurred in early-late Oligocene and the second one in late Miocene. These events are characterized by the development of high angle normal faults that formed graben-type tectonic depressions (Figures 1 and 3) (Aguirre-Díaz and McDowell, 1993; Aranda-Gómez et al., 1997; Henry and Aranda-Gómez, 2000; Luhr et al., 2001; Ferrari et al., 2005; Nieto-Samaniego et al., 2005, 2012). Although the timing of the regional extension is generally known, information about the age, geometry and kinematics of individual grabens and half grabens in the region is scarce, with the exception of the Santiaguillo graben (Nieto-Samaniego et al., 2012), the Rodeo half-graben (Luhr et al., 2001) and the southernmost part of the Río Chico-Otinapa graben (Aranda-Gómez et al., 1997; Henry and Aranda-Gómez, 2000).

3. Local stratigraphy

3.1. Early Eocene volcanism

3.1.1. Antigua ignimbrite

The pyroclastic deposits located at the bottom of the stratigraphic sequence are named in the present work as Antigua ignimbrite. This unit crops out in the northern part of the Santiago Papasquiaro-Los Altares highway and its base is not exposed (Figure 4, Tables 1 and 2). The Antigua ignimbrite unconformably underlies the El Cazadero andesite. A U-Pb age of 51.75 +0.35/-0.45 Ma (Figure 5, Tables 3 and 4) was obtained by LA-ICP-MS on zircons of a representative sample of this unit (Fres-b). We interpret this age as the crystallization time of magmatic zircons that should be very close to the time of rock emplacement (cooling), because the date was obtained from the younger coherent group of concordant ages obtained from the border of zircons. The Antigua ignimbrite has similar lithological characteristics and equivalent stratigraphic position as rocks reported by Aguirre-Díaz and McDowell (1991) in the Nazas region, east of the study area (Figure 2). The volcanic sequence near Nazas consists of silicic pyroclastic rocks, intermediate lava flows and domes, with ages between 48.8 ± 3 and 40.3 ± 1 Ma (K-Ar, on plagioclase, biotite, sanidine and hornblende).

3.2. Late Eocene-early Oligocene volcanism

3.2.1. Altamira ignimbrite

The Altamira ignimbrite is a pyroclastic deposit that crops out in the eastern and southeastern parts of the study area (Figure 4, Tables 1 and 2). This unit is the A1 member of the Altamira ignimbrite reported by Nieto-Samaniego et al. (2012) in the Nuevo Ideal-Canatlán region, 40 km southeast of the study area. Nieto-Samaniego et al. (2012) inferred that the olivine crystals (Table 2) observed in thin section must be fayalite because they appear as phenocrysts in association with quartz and K-feldspar. The Altamira ignimbrite unconformably underlies the Venadita rhyolite, Puente Negro ignimbrite and Santiago formation (Figure 4). In the Nuevo Ideal region, Nieto-Samaniego et al. (2012) obtained an age of 38.8 ± 1.0 Ma (K-Ar age, sanidine). This unit has lithological similarities and equivalent stratigraphic position as late Eocene-early Oligocene volcanic pulse rocks reported by Aguirre-Díaz and McDowell (1991) in the Nazas region, composed by rhyolitic domes and tuffs with ages from 34.0 ± 0.8 Ma to 29.5 ± 1.0 Ma (K-Ar ages, K-feldspar, plagioclase).

3.2.2. El Cazadero andesite

El Cazadero andesite consists of an intercalation of andesitic lava, breccia and tuff, as well as continental clastic deposits composed of andesite fragments, which crops out west of El Cazadero town, in the west-southwestern part of the study area (Figure 4). In previous studies this unit was named "andesite-andesitic breccia" (Mungía-Rojas et al., 2000; Luévano-Pinedo et al., 2003). General macroscopic and microscopic characteristics of lavas are shown in Tables 1 and 2. In some outcrops along the Santiago Papasquiaro-Los Altares highway, the rock has isolated reabsorbed andesite fragments in red and pale brown flow bands. The andesitic breccia shows several tones of green with matrix-supported, subangular to subrounded volcanic rock fragments in a fine to medium grained matrix. A dark reddish brown deposit composed of coarse sandstone and shale unconformably underlies the volcanic breccia. The sandstone contains andesite fragments supported by silicic matrix. A light colored pyroclastic deposit that contains pumice and holes left by eroded pumice fragments is intercalated between clastic deposits and lavas of El Cazadero andesite. This deposit contains lithic fragments between 5 mm and 10 cm across, and isolated biotite crystals up to 5 mm in diameter. El Cazadero andesite overlies unconformably the Antigua ignimbrite. U-Pb ages of two lavas of El Cazadero andesite were obtained by laser ablation inductively coupled plasma mass spectrometer (LA-ICP-MS) on zircons. Dating results were 37.2 +0.30/-0.40 Ma (Figure 6, Tables 3 and 5) for sample And-cl, and 35.95 +0.45/-0.5 Ma (Figure 6, Tables 3 and 6) for sample Caz-1. El Cazadero andesite has similar ages and lithology as Coneto andesite of the Nuevo Ideal region, which has reported ages of 35.0 ± 0.6 Ma (Ar-Ar on plagioclase, Nieto-Samaniego et al., 2012) and 40.15 +0.35/0.95 Ma (U-Pb on zircons, Nieto-Samaniego et al., 2012).

In the present study the name of Venadita rhyolite was given to a group of lava domes that overlies the Altamira ignimbrite and the El Cazadero andesite (Figure 4). Outcrops of this unit can be observed in some streams like La Venadita and El Almagre in the northeast of the study area, Santa Lucia and El Cardo in the southwest, and Puente Negro and Tía Lina in the north (Figure 4). General macroscopic and microscopic characteristics are shown in Tables 1 and 2. Commonly, the rhyolite has basal vitrophyres and autobreccias as well as flow foliation. Spherulitic texture is developed in some outcrops. The matrix is devitrified and presents perlitic fractures in thin section. The Venadita rhyolite unconformably underlies the Puente Negro ignimbrite. Due to lithological features and stratigraphic position this unit has similarities with the rhyolitic dome of 34 ± 0.8 Ma reported in Nazas region (Aguirre-Díaz and McDowell, 1991). For that reason, we consider the Venadita rhyolite of late Eocene-early Oligocene age.

3.2.4. Puente Negro ignimbrite

Puente Negro ignimbrite is a massive pyroclastic deposit that crops out in the northern and northeastern parts of the study area (Figure 4, Tables 1 and 2). This unit forms large tilted plateaus in the central-northern part of the area (Figures 3 and 4). The Puente Negro ignimbrite overlies unconformably the Altamira ignimbrite and Venadita rhyolite, and underlies unconformably the Santiago formation and the Neogene-Quaternary continental sediments. A U-Pb age of 34.0 +0.50/-0.70 Ma (Figure 7, Tables 3 and 7) was obtained from a representative sample (Pas-nc). This unit is considered part of the late Eocene-early Oligocene volcanic pulse.

3.2.5. Los Fresnos ignimbrite

Los Fresnos ignimbrite is a set of pyroclastic deposits that crop out west and northwest of Santiago Papasquiaro, and can be observed along the Santiago Papasquiaro-Los Altares highway (Figure 4, Tables 1 and 2). They have been grouped previously with other volcanic deposits and named as "rhyolitic tuff-ignimbrite" by Luévano-Pinedo et al. (2003). In the bottom of the Los Fresnos ignimbrite there are a series of pyroclastic-flow and fall deposits, with a total thickness of 2 m. Individual layers are red and yellow and have thicknesses of less than 5 cm. Los Fresnos ignimbrite overlies unconformably the Antigua ignimbrite, the El Cazadero andesite and the Venadita rhyolite, and underlies conformably the Balín ignimbrite. Los Fresnos ignimbrite has not been dated. However, its stratigraphic position indicates an early Oligocene age, including this unit as part of the late Eocene-early Oligocene ignimbritic pulse (Figure 4).

3.2.6. Balín ignimbrite

3.2.7. Santiago formation

The Santiago formation is the name proposed for epiclastic light brown-yellowish deposits of medium to coarse sand, gravel and conglomerate that crop out in the eastern, northern and western borders of the Santiago Papasquiaro valley (Figure 4, Tables 1 and 2). These deposits were named in previous works as "rhyolitic breccia-rhyolitic tuff" (Luévano-Pinedo et al., 2003). The most accessible outcrops are along the Santiago Papasquiaro-Nuevo Ideal highway as well as along the Santiago Papasquiaro-Garame de Abajo road (Figure 4). The Santiago formation includes intercalations of continental deposits of sand and conglomerates that are moderately lithified. In the southernmost outcrops these strata are composed of fragments that range in size from medium to coarse sand. Interbedded with the fine grained deposits are some lenticular deposits where fragment size increases. In the northernmost deposits of this unit the fragments are almost 60 cm. The source of these deposits probably was north of the study area because the clasts size increases toward the north. The Santiago formation overlies unconformably the Puente Negro ignimbrite and underlies unconformably basalt flows equivalent to the Metates Formation. This unit has similar lithological features and stratigraphic position as the Santa Inés Formation previously reported in Nazas by Aguirre-Díaz and McDowell (1991); these authors also described in the Nazas area 24 Ma mafic lavas overlying the Santa Inés Formation; mafic lavas of similar age had not been found in the Santiago Papasquiaro region. Taking into account its stratigraphic position, we propose a late Oligocene age for the Santiago Formation (Figure 4).

3.3. Miocene

3.3.1. Basalt equivalent to the Metates Formation

The Metates Formation was defined by Córdoba (1963) west of Durango City, around 130 km to the south-southeast of Santiago Papasquiaro. Equivalent basalts mapped in the study area consist of basaltic flows and dikes, which overlie and/or intrude the late Eocene-early Oligocene ignimbritic sequence. Small basalt flows crop out east of Santiago Papasquiaro (Figure 4). Also, some dikes and small flows crop out along the Santiago Papasquiaro-Nuevo Ideal highway and the Santiago Papasquiaro-Francisco Javier Leyva road. These lava flows usually present basal and upper breccias, and some glomerophenocrysts of ca. 15 mm (Tables 1 and 2). The basalts equivalent to the Metates Formation overlie unconformably the Santiago formation and are intercalated with Neogene-Quaternary unconsolidated deposits (Figure 4). Iriondo et al. (2004) obtained Ar-Ar isochron and plateau-like ages of 10.63±0.05 Ma and 10.95±0.02 Ma from one sample of these lavas, locating this unit at the base of the late Miocene.

3.3.2. Neogene-Quaternary sediments

3.4. Dioritic intrusion

A dioritic intrusive neck crops out west-southwest of Los Herrera (Figure 4, Tables 1 and 2). This intrusion was reported previously by Mungía-Rojas et al. (2000) and Luévano-Pinedo et al. (2003). This body intrudes rocks of the El Cazadero andesite of late Eocene age.

4. Structure of the Santiago Papasquiaro valley

The Santiago Papasquiaro valley is formed by NNW and NW striking blocks tilted to the southwest (Figures 3, 4 and 9). The tilted blocks of the Santiago Papasquiaro valley were formed in the intersection of two major fault systems: the San Luis-Tepehuanes NW-striking fault system (SLTFS) and the Río Chico-Otinapa NNW graben (RCOG) (Figures 1 and 3) (Nieto-Samaniego et al., 2005). The Tepehuanes and Santiaguillo grabens are part of the SLTFS (Figure 3) (Nieto-Samaniego et al., 2012). Between the Santiaguillo and Tepehuanes grabens there is a zone with NW faults that produce elongated blocks tilted to the southwest (Figures 3, 4 and 9). The second system is formed of several NNW grabens and half grabens that form a tectonic depression that is ~150 km long and averages 10 km wide (Figure 3). The northernmost structure of the RCOG is the Santiago Papasquiaro half-graben, which is oriented N15°W and is ~40 km long and ~10 km wide. Within the study area the master faults of both the SLTFS and RCOG are located in the western border of the Santiago Papasquiaro valley (Figures 3, 4 and 9). Those faults separate the Neogene-Quaternary sediments from the late Eocene-early Oligocene volcanic units. The estimated throw of the Santiago Papasquiaro half-graben (RCOG) is around 200 m, but considering throws of the adjacent major faults, the total throw is around 600 m (Figures 4 and 9). The throw of the SLTFS master fault is 500 m, adding the throws of the adjacent major faults, the total estimated throw reaches 800 m (Figures 4 and 9).

The average strike of the measured planes is NNW, and there is no significant difference between northern and southern portions of the measured fault planes (Figure 10). As seen in Figure 3, the average strike of SLTFS and RCOG is very similar at Santiago Papasquiaro latitude. Although the slickenlines show large dispersion, the movement is mainly normal to left oblique (Figure 10). Calculated strain tensors, using the dynamic analysis of Spang (1972), show minimum principal stress oriented 230/01 for the northern part of the study area and 244/05 for the southern part (Figure 10). We can see that inversion results are similar for both analyses, considering separately northern and southern data; this means that very similar strain tensors were obtained for both SLTFS and the Santiago Papasquiaro half-graben (Figure 10).

5. Geologic Evolution

The late Eocene-early Oligocene volcanic episode began ca. 38 Ma and is composed of acid to intermediate rocks (Figure 11). In Santiago Papasquiaro the volcanism continued into the early Oligocene. In the Nuevo Ideal region the age of the Coneto Rhyolite, the youngest unit of this volcanic sequence, is unknown. Volcanic activity is reported from 31 Ma to ca. 28 Ma in Durango and from 34 to 29 Ma near Nazas (Figure 11).

Volcanic activity ceased in late Oligocene time, and continental epiclastics were deposited in topographic depressions. During Neogene and Quaternary time, non-consolidated clay, sand and conglomerate were deposited. In the Miocene, basalt flows with ages ~24 Ma were emplaced in the Nazas region (Luhr et al., 2001), whereas in Santiago Papasquiaro and Durango basalts are younger, with ages from 10 to 12 Ma (Figure 11). The Durango Volcanic Field in Nuevo Ideal and Durango is composed of several volcanoes and basalt flows of Quaternary age (Albritton, 1958) (Figures 1, 2 and 11).

Extensional deformation (D1) initiated during the emplacement of the late Eocene-early Oligocene volcanic rocks. The coeval faulting and volcanism is inferred because the lower stratigraphic units show slightly greater tilts. D1 generated NW striking faults of the SLTFS in the north of the study area and NNW striking faults of the Santiago Papasquiaro half-graben in the south of the study area, creating an elongated depression where the Santiago formation was deposited. Some of the faults active during D1 were buried during deposition of the Santiago formation. We propose that RCOG began during D1 with the Santiago Papasquiaro half-graben and propagated southwards. This inference is based on the following observations: (a) vertical displacements of the RCOG diminish towards the south, from ~600 m near Santiago Papasquiaro to ~300 m near Otinapa, and the graben terminates 25 km south of Otinapa (Aranda-Gómez et al., 1997; Henry and Aranda-Gómez, 2000); (b) the basin fill erosion is more advanced in the Santiago Papasquiaro half-graben than in the southernmost regions, near Otinapa and Rio Chico, where the erosion is incipient; (c) sedimentary deposits that fill the northern depressions are more than 300 m thick and thin southward to tens of meters (Aranda-Gómez et al., 1997; Henry and Aranda-Gómez, 2000); (d) the basin system slopes northward, going gradually from average heights of 2100 masl in the south to 1700 masl in the north. We interpret that D1 initiated synchronously with the final stage of late Eocene-early Oligocene volcanism because, even though the collected data are scarce, the average tilting of El Cazadero andesite and Puente Negro ignimbrite is ~17° SW, whereas the Balín ignimbrite average tilting is ~12° SW, forming a slight angular unconformity that could be observed in the transect across Santiago Papasquiaro-Los Altares highway.

In the early-middle Miocene time, after the deposition of Santiago formation, a second extensional deformation phase (D2) took place that reactivated NNW striking faults of the Santiago Papasquiaro half-graben. D2 was inferred from faults that cut and tilt the Santiago formation. Some of these faults can be observed on the Santiago Papasquiaro-Garame de Abajo road and Santiago Papasquiaro-Nuevo Ideal highway. Some D2 faults were used later by feeder dikes of the equivalent Metates Formation; these dikes can be observed along the Santiago Papasquiaro-Nuevo Ideal highway and Santiago Papasquiaro-Francisco Javier Leyva road. Observed displacements on D2 NW faults of San Luis-Tepehuanes are less than 10 m; displacement in this system might have migrated to the east-southeast to the Santiaguillo graben where the peak of deformation ended in early Miocene (Nieto-Samaniego et al., 2012).

Minor extensional deformation (D3) in the Pliocene-Quaternary is evidenced from NE faults that affected the Neogene-Quaternary non-consolidated sediments. North of Santiago Papasquiaro two faults were measured in the recent basin fill deposits, with displacements of ~2 meters (Figure 13). Nieto-Samaniego et al. (2012) documented seismic activity in the Santiaguillo graben region. The reported seismicity supports that there is active deformation in the region, which could be responsible for the younger faults mapped in the study area.

6. Conclusions

• Six new U-Pb isotopic dates contribute to constraining the time of two volcanic pulses during the Cenozoic and the hiatus between them: The first volcanic pulse, referred to in the text as the Paleocene-middle Eocene volcanic pulse, is represented in the study area by 51.7 Ma rocks. The second volcanic pulse occurred in the late Eocene-early Oligocene and spanned from: 38.7 to 33.2 Ma.

• Three units with late Oligocene to Quaternary ages were distinguished in the study area: Santiago formation, basalts equivalent to the Metates Formation and non-consolidated sediments of the Neogene-Quaternary.

• Reported 56.4 and 51.7 Ma volcanic rocks confirm the existence of a pre-Oligocene volcanism pulse in the northwestern portion of the Mesa Central.

• Oligocene volcanism has been reported extensively in the Mesa Central. In the study area this volcanic pulse initiated at ca. 37-38 Ma, shortly earlier than in other areas, and lasted ca. 5 Ma. There is a hiatus between those two volcanic pulses, as has been previously reported in other areas of the Mesa Central (Nieto-Samaniego et al., 2005; Loza-Aguirre et al., 2008). The data presented here allows arguing that this hiatus lasted ca. 10 Ma in Santiago Papasquiaro.

• Three deformational phases where identified in the study area: D1 during the late Eocene-early Oligocene formed NW striking faults of the San Luis-Tepehuanes fault system and NNW striking faults of the Santiago Papasquiaro half-graben. The deformation migrated southward from Santiago Papasquiaro to the Rio Chico-Otinapa region. D2 during the early-middle Miocene reactivated NNW and faults NW. D3 during Pliocene-Quaternary formed minor displacement NE striking faults that cut unconsolidated deposits.

• Late Oligocene to Quaternary units record a new stage in the tectono-magmatic evolution of this region of the MC: the end of explosive acid volcanism of the SMOc, changing to an erosional phase with deposition of continental sediments in graben structures with small amounts of basaltic magmatism.

In the study area, crustal extension and volcanism occurred synchronously from late Eocene to present. The peak of extension and volcanism extended from late Eocene to early Oligocene.

The present work was financed by CONACYT projects 80142 and 049049. All the lab work was done at the Centro de Geociencias, Universidad Nacional Autónoma de México. We thank Juan Tomas Vázquez Ramírez for thin section preparation. Reviews by Fred McDowell and Christopher Henry substantially improved this manuscript.

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