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Revista mexicana de ciencias geológicas
On-line version ISSN 2007-2902Print version ISSN 1026-8774
Rev. mex. cienc. geol vol.29 n.1 Ciudad de México Apr. 2012
Geology and emplacement history of the Nuevo Rosarito plutonic suite in the southern Peninsular Ranges batholith, Baja California, México
Geología e historia de emplazamiento de la serie plutónica Nuevo Rosarito en la parte sur del batolito de las Sierras Peninsulares, Baja California, México
Tomás Alejandro PeñaAlonso1*, Luis Alberto DelgadoArgote1, Bodo Weber1, Fernando VelascoTapia2, and Víctor Valencia3,4
1 Departamento de Geología, CICESE, 22800 Ensenada, Baja California, México.
2 Facultad de Ciencias de la Tierra, Universidad Autónoma de Nuevo León, 67700 Linares, Nuevo León, México.
3 Department of Geosciences, University of Arizona, Tucson AZ, 85721, United States of America.
4 Valencia Geoservices, 3389 NRiver Rapids Dr, Tucson AZ, 85712, United States of America. * alepena@cicese.mx, topeax@gmail.com.
Manuscript received: May 16, 2011
Corrected manuscript received: August 23, 2011
Manuscript accepted: September 5, 2011
ABSTRACT
The Cretaceous Nuevo Rosarito plutonic suite is located in the southern part of the Peninsular Ranges batholith (~28.7 °N). It is hosted by a suite of Jurassicgranitoidrocks datedat 151.6Ma (UPb single zircon ages) and by Late Jurassic Early Cretaceous volcanic and volcaniclastic rocks. Host rocks display solidstate fabrics related to a deformational event that occurred before the emplacement of the Nuevo Rosarito plutonic suite. The composition of the suite ranges from gabbro to granite. The suite is subalkaline and it is divided into three mafic and four felsic units. The geochemical composition of the felsic units varies from metaluminous to peraluminous, and shows arcrelated geochemical signatures. Structural and geochemical data suggest that the emplacement of the plutonic suite took place in two episodes. The first one is defined by the intrusion of mafic units in which dioritic bodies were emplaced within a gabbroic body along NNESSW oriented extensionalfractures. The second episode is defined by the intrusion of three felsic units during a NEside up, synemplacement movement that occurred around 108.4 Ma.
Keywords: geochemistry, geochronology, deformation, emplacement, Peninsular Range batholith, Mexico.
RESUMEN
La serie plutónica Nuevo Rosarito del Cretácico se localiza en la parte sur del batolito de las Sierras Peninsulares (~28.7 °N). Está encajonada por granitoides jurásicos fechados en 151.6 Ma (edad UPb en zircones individuales) y por rocas volcánicas y volcanoclásticas del Jurásico Tardío Cretácico Temprano. Las rocas encajonantes presentan fábricas de estado sólido relacionadas a un evento de deformación que ocurrió antes del emplazamiento de la serie plutónica. La composición de la serie varía de gabro a granito. La serie, que es subalcalina, se divide en tres unidades máficas y cuatro félsicas. La composición geoquímica de las unidades félsicas varía de metaluminosa a peraluminosa y muestrafirmas geoquímicas relacionadas a arco. A partir de datos estructurales y geoquímicos se sugieren dos episodios de emplazamiento. El primero está definido por la intrusión de unidades máficas en donde cuerpos dioríticos fueron emplazados dentro de un cuerpo gabróico a través de fracturas de extensión. El segundo episodio está definido por la intrusión de tres unidades félsicas durante un movimiento del bloque NE hacia arriba, simultáneo al emplazamiento, que ocurrió a ca. 108.4 Ma.
Palabras clave: geoquímica, geocronología, deformación, emplazamiento, Batolito de las Sierras Peninsulares, México.
INTRODUCTION
The Peninsular Ranges batholith (PRB) is a continuous belt of Late Cretaceous plutons that crops out from southern California, USA, to the northern half of the Baja California peninsula, Mexico. According to geochemical, mineralogical, geophysical, and age data (e.g., DePaolo, 1981; Todd and Shaw, 1985; Gromet and Silver, 1987; Silver and Chappell, 1988; Gastil et al., 1994; Tulloch and Kimbrough, 2003), it is a general convention to divide axially the batholith into a western and an eastern zone. The western zone is characterized by I type plutons (Walawender et al., 1990) related to an oceanic arc and emplaced at subvolcanic depths (Johnson et al., 2002). Most of the plutons of the western zone intrude AlbianAptian volcanic and volcaniclastic intraarc assemblages associated with the Alisitos Formation (Gastil et al., 1975; Beggs, 1984; Busby et al., 2006). The eastern zone is characterized by younger I and Stype plutons related to a Late Cretaceous, eastwardmigrating arc (Gromet and Silver, 1987) that intruded Ordovician to Permian continental clastic assemblages, as well as Proterozoic to Permian carbonatesiliciclastic assemblages (Gastil and Miller, 1984; Gastil, 1993). Between the western and eastern zones, a transitional zone has been described in several areas as distinct Triassic(?)Cretaceous clastic and volcaniclastic flyschlike assemblage of uncertain tectonic origin (Figure 1a; Schmidt et al., 2002).
Intense ductile deformation found in areas like the Sierra San Pedro Mártir and Calamajué (localities SSPM and 5, respectively, in Figure 1a), in the eastern edge of the western zone and within the transitional zone, suggests that the Alisitos arc was accreted along the southwestern North American continental margin ca. 115108 Ma (Johnson et al., 1999).
Most studies of plutons within the PRB are concentrated between southern California, and the latitude of El Rosario area in Baja California (Figure 1; locality 6). For example, in the El Rosario area, PRB plutons are hosted by the Cretaceous Alisitos Formation (Busby et al., 2006). Few other studies have been conducted south of this region, especially in the El Arco area (Figure 1a, locality 10), which has been recognized as the southernmost exposure of the PRB (Schmidt et al., 2002). In contrast to the geology reported in the El Rosario area, El Arco is a Middle Jurassic porphyry copper deposit (Valencia et al., 2006) emplaced in a primitive oceanic crust environment (Weber and LópezMartínez, 2006) that can be correlated with Jurassic magmatic sequences of the Cedros Island and the Vizcaino península (Kimbrough and Moore, 2003; Hickey, 1984; locality 11).
Another important sequence to consider is the Eugenia Formation. This is represented by Late JurassicCretaceous rocks outcropping in the Vizcaíno peninsula and the Cedros Island as well (Hickey, 1984). It has been proposed that this formation was derived from the San Andrés volcanoplutonic complex (Barnes, 1984), which, in turn, is contemporaneous to the flyschlike assemblages of the PRB transitional zone and to the Alisitos Formation.
The study area consists of a plutonic suite that intrudes prebatholithic undifferentiated metamorphic rocks (Figure 1b). However, northwestward from the study area, the prebatholithic rocks consist of volcanic and volcaniclastic rocks of the Early Cretaceous Alisitos Formation, which have been described by Beggs (1984) around the locality of Punta Prieta (Figure 1b). Similarly, volcaniclastic rocks including fragments of fossiliferous limestone crop out about 10 km north of the study area.
In order to define the relationships between plutonic rocks of the southern PRB and contrasted sequences of prebatholithic rocks, we conducted a comprehensive geological study that includes field work, structural, petrological, geochemical and geochronological analyses in the plutonic suite that has been labeled as the Nuevo Rosarito plutonic suite.
GEOLOGICAL BACKGROUND
The Nuevo Rosarito plutonic suite is located between 28.66 °N and 28.59° N, near the Pacific coast of Baja California (Figure 1). It comprises a northern and a southern part, which share the same lithology and field relationships, but have different geometries and their rocks exhibit drastic textural and mineralogical variations. The northern part consist of a 15 km2 elliptical body elongated in a NNWSSE direction, while the southern part consist of a 7 km2 circular body with a domelike shape that includes host rocks screens as large as 150 m2 (Figure 2a).
Under the premise that plutons are composite bodies usually assembled by several individual magma pulses (e.g., Coleman et al., 2004; Vigneresse, 2004; Matzel et al., 2006; Kemp et al., 2007; Michel et al., 2008), we identified seven different intrusive units that altogether comprise the Nuevo Rosarito plutonic suite. This suite is dominated by mafic rocks. The older and most widely exposed intrusive unit consists of twopyroxene gabbro. The gabbro is cut by smaller intrusions of a twopyroxene diorite (Kd) and a hornblendepyroxene quartz diorite (Kqd). All these lithologies are intruded, in turn, by younger felsic dikes. Moreover, these dikes can be divided according to field relationships, mineralogy, texture, and geochemical composition into four distinct intrusive units: Kt (hornblendebiotite tonalite), Kg1 (biotitehornblende tonalitegranodioritegranite), Kg2 (hornblendeclinopyroxene granitemonzogranitesyenogranite) and Kg3 (biotite granite), in that chronological order.
In the following sections, the lithology and the structural patterns of the northern and southern parts of the Nuevo Rosarito plutonic suite and their host rocks are described. The emplacement conditions are interpreted from petrography and microstructure analyses, whereas igneous processes are elucidated from geochemistry. Furthermore, UPb ages of zircons from host rock units are reported here for the first time, together with an age of a hornblendebiotite tonalite from the central part of the plutonic suite.
HOST ROCKS
The host rocks of the Nuevo Rosarito plutonic suite are grouped into five lithologic units (Figure 2a): granitoid rocks (Jt), metamorphosed quartzfeldespatic volcanic and volcaniclastic rocks (Jv), amphibolitic rocks (Jma), hornfels (Kmh), and clastic rocks (Js).
The granitoid rocks (Jt unit) are widely exposed in the southeastern part of the study area. They are medium to coarsegrained rocks that according to their mineralogy vary from tonalite to granodiorite. They also display protomylonitic to mylonitic fabrics and cmscale aplitic dikes as well as quartz veins. The Jt unit usually contains screens of Jv and Jma rocks that have a nearly vertical attitude and sizes ranging from a few cm up to 600 m long.
In the northern part of the suite, the volcanic and volcaniclastic rocks of the Jv unit are mostly formed by andesitic to dacitic feldsparrich porphyritic lava flows showing a greenschist facies mineralogy. They are composed of abundant euhedral to subhedral, feldspar phenocrysts (0.5 to 1.5 mm) in a very finegrained, quartzfeldspatic, biotite>hornblende matrix. The Jv unit includes horizons of flow breccias formed by matrixsupported, cobblesized fragments of mafic and felsic intrusive rocks, and protomilonitic rocks of andesitic flow breccias and finegrained volcaniclastics. These protomilonitic rocks are located near the NR24 sample site (Figure 2a). Another feature of the Jv unit from the northern part of the suite is that it is in contact with chloritized coarsegrained hornblendebiotite tonalitic rocks that show schistose to protomylonitic fabrics and that locally contain a few mthick screens of felsic protomylonites and amphibolites. Here we hypothesize that such tonalitic rocks are part of the widely exposed Jt unit located on the southern part of the suite; however, this idea remains to be tested.
In the southern part of the suite, the Jv unit is made up by andesitic and rhyolitic lava flows, volcanic breccias, and felsic tuffs. Mafic schists and orthogneisses are also present. Some portions of these Jv volcanic units display dynamic recrystallization and protomylonitic texture. In the eastern side of the study area, near the sample site 17XII07, clastic rocks (Js) are apparently interstratified with protomylonites of volcanic breccias that include granitoid fragments and tuffaceous material.
Amphibolitic rocks (Jma; Figure 2a) parallel the foliation of the granitoid unit Jt and crop out as large lenslike screens in the eastern margin of the study area or as isolated rock screens within the gabbroic rocks (Kgb). Their typical mineral assemblage is plagioclase+hornblende+actinolite± biotite±epidote.
Along the western contact with the gabbroic rocks of the northern part of the suite, the host rocks developed a 10 to 100 mwide contact aureole that is characterized by hornblendehornfels and pyroxenehornfels facies (Kmh; Figure 2a). The mineralogy of the hornblendehornfels is plagioclase+hornblende+clinopyroxene+opaques±quartz in a finegrained texture. The pyroxenehornfels, in turn, is formed by an assemblage of plagioclase+orthopyroxene +clinopyroxene+opaques±biotite±hornblende, having a medium to coarsegrained granoblastic texture. A subvertical penetrative schistosity developed on the Jv volcanic rocks and the Kmh hornfels of the northern part of the suite, parallel to the contact aureole, is sometimes destroyed by younger Kg1 and Kg2 felsic bodies.
The intensity of the fabrics and the structural patterns of the host rocks of the northern part of the suite are strongly different from those of the southern one. On the one hand, in the northern part of the suite, the host rocks have solidstate fabrics ranging from schistose to protomylonitic. Moreover, average foliation and bedding dips towards the SW (mean 150°/60°W; Figure 3a). In addition to that, the protomylonitic rocks exhibit a welldeveloped SWdipping stretching lineation that is oriented towards 228°/58° in average (Figure 3a). On the other hand, in the southern part of the suite, host rock bedding and deformational fabrics are subvertical and NNW oriented (mean 342°/83°E; Figure 3b). The Jv volcanic host rocks display intense deformational fabrics, defined by penetrative schistosity and/or asymmetric porphyroclast tails in the lavalike rocks, and by elongated fragments in the volcanic breccias. Furthermore, welldeveloped stretching lineations in biotite from granitoids, and lineation of quartz exhibited by some volcanics are nearly vertical or dip toward SE (Figure 3b). All those patterns are also present in the host rock screens contained within the gabbroic rocks (which indicates that their deformational fabrics were developed prior to the gabbro emplacement). Another difference between the northern and southern part of the suite is that the circular geometry of the southern part of the suite locally controls the schistose fabrics of the surrounding host rocks.
THE NUEVO ROSARITO PLUTONIC SUITE
Melanocratic twopyroxene gabbro (Kgb) show coarse to mediumgrained textures, and commonly exhibits 6 cm to 2 m thick layers defined by granulometric variations of the plagioclase. In the southern part of the suite, the gabbro locally displays cm to mscale cumulitic layers composed of mm to 2 cmeuhedral plagioclase phenocrysts (Figure 4a). Along the contacts with the host rock screens, the Kgb unit shows magmatic fabrics defined by cmwide compositional banding. Also, they usually preserve vertical primary fractures oriented towards NWSE and NESW (Figure 3c).
In the northern part of the suite, twopyroxene diorite (Kd) crop out as bodies of less than 100 meters long and as cmscale dikes as well. Diorite is cut by abundant amphibole veins of probable hydrothermal origin (dioritic enclave in Figures 4b and 4c). However, in the southern part of the suite, diorite crops out as 2 to 20 mwide bodies of interfingered geometry and with jaggedlike contacts (Figure 4d), as well as 3 to 50 cmthick dikes displaying smoothly curviplanar contacts. The interfingered Kd bodies and dikes are persistently oriented towards NNE throughout the suite (mean 21°/85°SE, Figure 3d).
The geometry of a hornblendepyroxene quartz diorite (Kqd) that crops out in the central portion of the study area is obscured by the intrusion of younger felsic bodies (Kt, Kg1, Kg2, and Kg3 in Figure 2a). This unit includes subangular enclaves of the twopyroxene diorite (Kd) suggesting that it postdates Kd. Occasionally, quartz diorites have NWSE oriented solidstate fabrics indicated by the elongation of amphiboles and cmscale shear bands.
The gabbro (Kgb), diorite (Kd) and quartz diorite (Kqd) units are intruded by a medium to coarsegrained, hornblendebiotite tonaliticgranodioritic unit (Kt). This unit crops out in the southwestern portion of the study area as a massive body of approximately 800 m2 or like NWSE oriented dikes in the northern part of the suite. The Kt massive body shows numerous angular to subrounded, cm to dmscale dioritic autoliths and enclaves (Figures 4b and 4c), and displays wellpreserved vertical magmatic fabrics defined by the alignment of minerals, by local schlierentype banding, and by the alignment and/or elongation of dioritic enclaves and autoliths (mean 172°/87°W; Figure 3e). In contrast, the Kt dikes exhibit magmatic fabrics delineated by mineral alignment, and overprinted by schistose textures.
Following the sequence of emplacement, the Kt unit is intruded, in turn, by a series of dikes showing single and sheeted geometries. Their modal composition varies from tonalite to granite (Kg1 unit) or from granite to syenogranite (Kg2 unit). Both Kg1 and Kg2 units show imbricate contact relationships suggesting a penecontemporaneous emplacement.
The Kg1 unit represents white to light gray, biotiterich bodies showing sheetedlike geometries or cropping out as single cm to mthick dikes following a NW orientation. The sheetedlike Kg1 bodies have porphyritic to granular texture, and display local schistosity paralleling dmscale Kg2 dikes (Figures 4e and 4f). However, Kg1 dikes exhibit intense solidstate fabrics (Figure 4g) dominated by mylonitic textures (Figures 4h and 4i). They can also contain ductile deformed mafic xenoliths or host rock enclaves oriented subparallel to the foliation.
The Kg2 unit represents pinkcolored, hornblenderich dikes ranging from few decimeters to 1 m in thickness exhibiting internal compositional banding and mmscale miarolitic cavities. In the northern part of the suite they have sheeted geometries containing cmscale Kg1 dikes and lenses of mafic rocks, whereas in the southern part they crop out as single dikes.
The mafic rocks in the immediate vicinity of Kg1 and Kg2 units usually display ductile features (Figures 4h and 4i). The internal fabrics of the Kt dikes and the Kg1 bodies are oriented towards NWSE (Figure 3f), exhibiting stretching lineation dipping SW and NE in average (Figure 3g). In contrast, the Kg2 bodies are mainly oriented SE (Figure 3h), developing a SW directed lineation (Figure 3i). Nine kinematic indicators were obtained from the Kt dikes, and the Kg1 and Kg2 bodies: two from outcrops (as the SC structures from Figure 4g), and seven from thin sections oriented parallel to the XZ plane. Those kinematic indicators invariably indicate a northeast side up sense of shear.
The last unit in the emplacement sequence is composed of cm to mthick aplitic dikes of biotite granite (Kg3 unit) that include pegmatite facies concentrated at their margins or along their axial planes. These dikes are mainly NESW oriented (Figure 3j).
PETROGRAPHY AND MICROSTRUCTURES OF THE NUEVO ROSARITO INTRUSIVE UNITS
Twopyroxene gabbro (Kgb)
As shown in the modal classification of Figure 5a, seven of the eleven samples of the gabbroic rocks plot in the gabbronorite field. They display hypidiomorphic textures, showing seriated, euhedral to anhedral labradoriteandesine (4062 %) typically exhibiting a normal zonation. Orthopyroxene (429 %) is coarsegrained, granular to subophitic. Subophitic augite (427 %) is medium to coarsegrained. Opaque minerals can reach 12 % of total mineral content. The cumulitic textures of the southern part of the suite are made up by 9098 % coarsegrained labradorite that can exhibit reaction rims. Additionally, augite commonly exhibits ropetype pigeonite exsolution lamellae and minor inverted pigeonite. Also, plagioclase crystals occasionally have trachytoid textures. At the contacts with the Kd interfingered bodies (Figure 4d), up to 34 % of the Kgb pyroxene content is partially replaced by greenbrown hornblende.
At two locations, where deformed gabbro occurs in the immediate vicinity of the felsic dikes, the gabbro is metamorphosed under greenschist (albite+quartz+actinolite±biotite±epidote±oligoclase) to amphibolite (sodic plagioclase+hornblende±epidote±clinopyroxene) facies conditions.
Twopyroxene diorite (Kd)
Diorite is commonly alliotromorphic granular. Its modal composition is defined by andesine (5155 %), fine to mediumgrained subophitic enstatite (725 %), augite (1013 %), minor brownpoikilitic or greeninterstitial hornblende (417 %), and opaque minerals (612 %).
In the southern part of the suite, dioritic rocks in contact with gabbro commonly contain calcic plagioclase xenocrysts, which composition is highly similar to the gabbroic plagioclase. In addition, the contact between interfingered diorite and gabbro (Figure 4d) is microscopically delineated by the crystalline margins of plagioclase grains from the gabbro (Figure 6a). Both observations define an interlocking texture as described by Hibbard and Waters (1985), suggesting late magmatic fracturing.
Hornblendepyroxene quartz diorite (Kqd)
Most of the quartz dioritic rocks show seriated medium to coarsegrained, hypidiomorphic and allotriomorphic textures composed of andesine (5279 %), intergranular quartz showing undulatory extinction (<4 %), subophitic green hornblende with occasional inclusions of augite (1341 %), reddish brown biotite (34 %), and opaque minerals (13 %). Few analyzed samples include minor hypersthene grains (<3 %). Numerous plagioclase grains are discontinuously normal zoned and show highly fractured, boxylike calcic cores with convoluted rims that are indicative of core resorption.
Hornblendebiotite tonalite (Kt)
The massive body of this unit is formed by coarse to mediumgrained, hypidiomorphic rocks, whereas dikes are usually allotriomorphic. This unit is composed of oligoclase (3762 %) commonly displaying discontinuous normal and oscillatory zonation; potassic feldspar (<12 %) with subophitic texture usually displaying tartan twinning; finegrained quartz (2325 %) with incipient chessboard undulatory extinction (Figure 6b); green hornblende (215 %) with intergranular fractures; intergranular to intragranular redbrown biotite (up to 14 %) exhibiting misoriented segments or kinking; and opaque minerals (up to 2%). Zircon and apatite occur as accessory minerals. Kt dikes can exhibit incipient SC structures and myrmekite intergrowth in the potassic feldspar grains.
Biotiterich tonalitegranodioritegranite (Kg1)
This unit has compositions ranging from biotite tonalite to potassic feldsparrich granite (Figure 5b), containing oligoclase (1049 %), potassic feldspar (1066 %), quartz (2440 %), biotite (<16 %), and opaque minerals (<1 %). Zircon, apatite, and tourmaline can also be present as accessory minerales. In the southern part of the suite, this unit also contains hornblende (28 %).
The internal fabrics of the Kg1 dikes are mainly mylonitic, defined in the microscale by feldspar, quartz and/or hornblende porphyroclasts wrapped by finegrained, quartz and biotiterich folia. The feldspar porphyroclasts display sigmoid shape, and moderate to intensively recrystallized grain margins (Figure 6c). Potassic feldspar porphyroclasts frequently exhibit tartan twinning and/or flame perthites. The quartz porphyroclasts are rounded, displaying undulatory or chessboard extinction. The hornblende porphyroclasts exhibit misoriented segments and boudinage (Figure 6d). Hornblende can also occur as recrystallized aggregates outlining the folia. The texture of the quartz of the folia (anastomose around the deformed porphyroclasts) suggests recrystallization by bulging or subgrain rotation mechanism.
Some samples include feldspar grains with intragranular fractures filled by late phases of albite or quartz (submagmatic fractures after Bouchez et al., 1992). We also report zoned plagioclase grains whose chemical zonation is truncated in high angles with respect to the foliation and healed by latephases, which are in optical continuity with the outer rims (Figure 6e; fusion contact from Park and Means, 1996).
Hornblenderich granitemonzogranitesyenogranite (Kg2)
The bodies from this unit are finegrained, allotriomorphic granular, composed of subhedral to anhedral oligoclase displaying mechanical twinning and misoriented segments (2147 %); anhedral potassic feldspar with tartan twinning and/or replaced by myrmekites (1263 %); indented to lobular quartz (Figure 6f) with subgrains and undulatory to incipient chessboard extinction (643 %); and elongated green hornblende (sometimes boudinaged) paralleling the foliation (114 %). They also contain minor anhedral augite or pigeonite (trace4 %), opaque minerals (trace8 %), and a relatively high population of accessories (25 %), including apatite, tourmaline, zircon, sphene, rutile, and hematite.
Biotite granite (Kg3)
Dikes from this unit have hypidiomorphic to allotriomorphic granular textures. Oligoclase (2145 %) shows normal zoning and mechanical twining; potassic feldspar (2653 %) is present in perthites and mesophertites with a typical tartan twinning; and anhedral quartz grains (1926 %) showing consertal textures and undulatory to incipient chessboard extinction. Other minerals present in this unit are intergranular biotite incipiently chloritized (2 %), minor white mica (<1 %), opaque minerals (<1 %), and apatite and zircon as accessory minerals (<1 %). Euhedral to subhedral almandine can reach up to 6 % volume content in the northern part of the suite.
WHOLEROCK GEOCHEMISTRY
Analytical and initial data handling procedures
Representative samples of all plutonic units, excepting Kqd, were selected to establish their major and trace element composition. Sample locations are shown in Figure 2a, whereas details of field description and petrographic features are summarized in Table 1.
Samples were initially processed at the Geology Department at CICESE using a Braun® ironjaw crusher and a Bico® disk plate pulverizer to obtain grain sizes less than 1.0 mm. Following, representative aliquots of ~100 gr of rock powder were processed using a Bico® tungsten carbide ring pulverizer and stored in Nalgene® HDPE (high density polyethylene) bottles. Wholerock major and trace element compositions were determined in ActLabs laboratories, Canada, by 4B or 4Litho analytical codes. Major and trace element compositions under 4Litho code, and major element compositions under 4B code, were determined by a lithium metaborate/tetraborate fusion procedure followed by an ICPMS method. Trace element compositions under 4B code were determined by: (a) a total digestion procedure followed by ICPMS analysis (Cu, Mo, Ni, S, Zn), (b) a lithium metaborate/tetraborate fusion procedure followed by ICPMS analysis (Sr, V, Y, Zr), and (c) an instrumental neutron activation technique (As, Co, Cr, Hf, Rb, Sc, Th, U, La, Ce, Nd, Sm, Eu, Yb, Lu). CIPW norms were calculated considering an anhydrous 100% adjusted basis, with Fe2O3/ FeO ratios adjusted according to SiO2 content (Middlemost, 1989). All computations (anhydrous and ironoxidation ratio adjustments, and CIPW norm compositions) were automatically done using the SINCLAS software (Verma et al., 2003). Geochemical data were compiled and used to construct several variation and REE chondritenormalized diagrams. Normalization REE data of chondrite were taken from Haskin et al. (1968) and Nakamura (1974).
Geochemistry
As expected, with the exception of alkalis, TiO2 and P2O5, major element compositions decrease with increasing SiO2 (for example MgO; Figure 7a). In contrast, (Na2O + K2O) content increases with SiO2, showing a nearly linear pattern (Figure 7b). Sr also shows a marked decrease with increasing SiO2 (Figure 7c), whereas Ba, Zr, and LREE display an opposite behavior (for example, Figure 7d). The rest of the trace elements are characterized by a lack of coherent trends in the variation diagrams.
Mafic units
Gabbroic rocks (Kgb; 42.947.5 wt % SiO2) have high alumina (17.223.7 wt %) and moderate to high magnesium content (5.611.7 wt %). Most of the samples contain normative olivine (1.529.6 %) and hypersthene (0.813.5 %) with the exception of one sample that yielded normative nepheline (0.8 °%). Gabbroic rocks are characterized by low concentrations of TiO2 and P2O5 compared to the other units (Table 2). Chondritenormalized REE abundances of the gabbroic rocks (Figure 8a) have 2 to 5 times the chondrite level, display relatively flat patterns (La/YbCN 0.51.5), and positiveEu anomaly (Eu/Eu* 0.52). One sample has a negative Ce anomaly (gabbro 40XI08; Table 2), probably related to oxidation and secondary mobility of Ce. As pyroxene of this sample is moderately altered to uralite, particle scavenging hydrothermal activity (e.g., Hongo et al. , 2007) may explain this anomaly.
Dioritic rocks (Kd; 49.350.2 wt % SiO2) also have high alumina (18.218.4 wt %), and moderate magnesium content (5.25.8 wt %). Their CIPW norm is characterized by low olivine (0.21.9 %) and high hypersthene content (21.923.9 %). Chondritenormalized REE abundances of diorite (Figure 8a) have 7 to 17 times the chondrite level. Our available REE data indicate a minor LREE fractionation (La/SmCN 1.31.7), and suggest a positive Eu anomaly (Figure 8a).
According to the Ti/V ratios of gabbro (Kgb; 7.613.3) and diorite (Kd; 16.4 20.1), these units plot in the lower limit or within the arc field on the Shervais (1982) TiV discrimination diagram (Figure 9).
Felsic units
According to the classification scheme for granitic rocks based in the Fe* vs weight per cent SiO2 diagram (Fe*=FeOt/(FeOt + MgO); Frost et al., 2001), tonalites of the Kt unit (samples NR16 and 12III06) and the Kg1 dike represented by the sample 19VII06 are magnesian. The rest of the felsic samples plot in the ferroan field. Even though, all the felsic units are inside the Cordilleran granites field (Figure 10a). From the MALI diagram (modified alkalilime index; Frost et al., 2001), Kt and Kg1 units plot in the calcic field, which typify the granitoids of the Cordilleran Mesozoic batholiths. The only exception is sample 41XI08 from Kg2 unit, which is alkaline granite (Figure 10b). In relation to the Shand aluminum saturation index (Al / [Na+K] vs Al / [Ca+Na+K]; Terra Softa, Inc., 2009), both the Kt unit and the Kg1 dike 19VII06 plot within the metaluminous field. The other three samples are peraluminous, whereas granite 41XI08 is located in the border of the metaluminous and the peralkaline fields (Figure 10c).
Chondritenormalized REE abundances of the Kt unit samples (NR16 and 12III06 in Figure 8b) have about 27 times the chondritic levels (except for La of sample 12III06). The REE pattern of sample NR16 from the massive outcrop displays only slight LREE fractionation (La/SmCN 1.3), a moderate negative Eu anomaly (Eu/Eu* 0.74), and a flat HREE pattern (Figure 8b). The 12III06 Kt dike shows a similar chondritenormalized REE pattern and higher LREE fractionaiton (La/SmCN 2.6) relative to NR16. Available data also suggest a moderate negative Eu anomaly.
Chondritenormalized REE abundances of the two samples representing the Kg1 unit (12III06 and 19VII06; Figure 8b) are 30 to 45 times the chondritic levels, with a moderate fractionation of LREE (La/SmCN 2.44.8). In turn, the sample 41XI08 (Figure 8b) has about 30 times the chondritic content, slight fractionation of LREE (La/ SmCN 1.6), slight negative Eu anomaly (Eu/Eu* 0.75), and a relative flat HREE pattern (Figure 8b). Finally, the Kg3 unit (samples 64VII07 and 53XI08; Figure 8b) have 10 to 45 times the chondritic content, the highest silica (76.7 wt %) and the lowest magnesium content (0.20.3 wt %). In turn, sample 53XI08 shows a highly fractionated LREE (La/SmCN 3.94.8). It is characterized by the absence of a Eu anomaly, a concavedown shape of their HREE with the lowest value at Dy, and a positive slope in their LREE (Figure 8b).
UPb GEOCHRONOLOGY
Analytical procedures
Zircons were separated by standard procedures at the Geology Department, CICESE. Crushed, milled, and sieved samples were processed using a Wilfley® table, a Frantz® isodynamic separator, and heavy liquid techniques using methylene iodide. Finally, inclusionsfree crystals were selected by handpicking.
Individual zircon crystals were analyzed at the Geosciences Department of the University of Arizona, Tucson, with a Micromass Isoprobe multicollector ICPMS, equipped with nine Faraday collectors, an axial Daly detector, and four ioncounting channels. An ArF Excimer laser system with an emission wavelength of 193 nm is coupled to the isoprobe. The collector configuration allows measurement of 204Pb with an ioncounting channel whereas 206Pb, 207Pb, 208Pb, 232Th and 238U are measured simultaneously with Faraday detectors. The analyses were conducted following the method described by Gehrels et al. (2006) in static mode with a laser beam diameter of 35 um with output energy of ~32 mJ and a repetition rate of 8 Hz. Each analysis consisted of one 20 secondsintegration on peaks with no laser firing for background measurement and 12 onesecond integrations on peaks with laser firing. The background values are used to remove any Hg contribution to the 204Pb mass. Uranium and Thorium concentrations were monitored by analyzing a standard (NIST 610 Glass) with ~500 ppm Th and U, for every sample. Interelement fractionation was monitored by analyzing zircon standard fragments from Sri Lanka (SL1) with a known concordant IDTIMS age of 564 ± 4 Ma (2o) (Gehrels et al., 2008), once for every four unknown sample zircon grains.
All reported ages are based on the 206Pb/238U ratios because errors of the 207Pb/235U and 206Pb/207Pb ratios are greater due to the low 207Pb signal of young samples. The 206Pb/238U ratios were corrected for common lead by using the measured 204Pb assuming an initial Pb composition from Stacey and Kramers (1975) and an uncertainty of 1.0 for 206Pb/204Pb.
Weighted average ages were calculated using Isoplot v. 3 (Ludwig, 2003). Systematic errors were propagated separately, and include the age of the standard, calibration correction from standard analyses, composition of common Pb, and U decay constant uncertainties. All age uncertainties are reported at the 2sigma level (2o). UPb geochronological data are presented in Table 3.
Zircon UPb results
We analyzed zircons from a hosting granitoid rock of the unit Jt (sample 17XII07; Figure 2), a hosting volcanic breccia of the Jv unit (sample NR24), and a tonalite from the Kt massive body (sample NR16). Measurements were made at the center and tips of the zircon crystals. Zircons from all three samples are colorless, and have a welldeveloped prism {110} and pyramid {101} forms. They also have U/ Th <3 indicating a magmatic origin (Rubatto, 2002).
Zircons from the plutonic rocks (17XII07 and NR16) are dominantly prismatic (lengthtowidth ratio between 2 and 4). Separated grain sizes vary from 100 to 450 um. Thirty one zircon grains from sample 17XII07 were measured, yielding a weighted 206Pb/238U age of 151.6 ± 2.6 Ma (2o, including systematic error; Figure 11a). Thirty two laser spots were measured on zircons from sample NR16. They yield a weighted 206Pb/238U age of 108.4 ± 2.2 Ma (2o, including systematic error; Figure 11b). Zircon crystals from sample NR24 are long prismatic (l/w of 6 to12), ranging from 550 to 120 um in size. Twenty six laser spots on zircons from sample NR24 yield a weighted 206Pb/238U age of 139.5 ± 2.0 Ma (2o, including systematic error; Figure 11c). In one grain of the last sample an inherited zircon core with a 206Pb/238U age of 152.7 ± 1.5 Ma (1o analytical uncertainty) was detected.
DISCUSSION
Host rocks
The host rocks of the Nuevo Rosarito plutonic suite are dominated by volcanic units and granitoid rocks. The granitoids have minor screens of volcanics, amphibolite and clastic sedimentary rocks. Accordingly, we assume that the Nuevo Rosarito plutonic suite was emplaced into a volcanoplutonic assemblage.
In the southern part of the suite, the 151.6 ± 2.6 Ma UPb age obtained from the granitoid Jt unit makes this plutonic sequence contemporaneous to the San Andrés volcanoplutonic complex (locality 11; Figure 1a), whose UPb zircon ages vary between 134.5 and 155.6 Ma (Kimbrough and Moore, 2003). In the northern part of the suite, the dated sample NR24 from a volcanic breccia deposit yield an UPb zircon age of 139.5 ± 2.0 Ma, which is also contemporaneous to the San Andrés volcanoplutonic complex and to the volcanogenic deposits from the Eugenia formation. The orientations of the fabrics of all host rock units (including the screens within the gabbroic rocks) are persistent at the regional scale, except for the outcrops close to the margins of the southern part of the suite, where fabrics have a tendency to outline its circular geometry. Such tendency indicates that ductile deformation and overturning of the structures occurred before the emplacement of the gabbro.
Mafic units (Kgb, Kd, Kqd)
The absence of olivine and the presence of orthopyroxene in the gabbroic (Kgb) and dioritic (Kd) rocks allow us to compare the mafic units with the amphiboleorthopyroxene subseries of the gabbroic rocks of the Peninsular Ranges batholith in southern California (Walawender and Smith, 1980). The Kgb rocks have alumina concentrations in the range of 17.2 to 23.7% (Table 2), exceeding the normal content for subalkaline gabbroic rocks (Cox et al., 1979). Such high alumina content is a typical composition of highalumina arc basalts (1722 wt %; e.g., Fournelle and Marsh, 1991), which is the dominant rock type in most island arc settings (e.g., Wilson, 1989). As observed elsewhere (Fournelle and Marsh, 1991; Tate et al., 1999), positive Eu anomaly (Figure 8a) is associated with the presence of the plagioclase cumulates from the southern part of the suite (Figure 4a).
The Kd interfingered bodies (Figure 4d) exhibit at the microscopic and hand specimen scales a clear interlocking texture (Figure 6a). According to Hibbard and Waters (1985), such texture suggests magmatic fracturing with presence of intergranular melt that, in this case, is dioritic. Nonfractured fragments of gabbro included within diorite dikes support a late stage magmatic fracturing with a minor presence of intergranular dioritic melt compared with the interfingered bodies. Both the Kd interfingered bodies and Kd dikes do not have chilled margins, suggesting a small temperature contrast between the dioritic melt and the hosting gabbro. As a result, the textural variation in the Kd dikes and the fact that diorite is enclosed by the gabbro also suggest that dioritic melt was segregated from a gabbroic mush. This interpretation is supported by the following geochemical data: (a) the MgO and alkalis contents of the two diorite samples (18VII06 and 14III06) are similar to the lowest compositional values of the same oxides of the gabbroic rocks (Figures 7a and 7b); (b) dioritic and gabbroic rocks have comparable REE patterns with positive Eu anomalies (Figure 8a); (c) diorite has higher REE abundances and higher incompatible element concentrations (e.g. Ba, Y, Zr, Hf, La, Ce; Table 2) than gabbro.
Decades of observations of intrusive geometries have shown that the alignment of magmatic bodies is the product of (a) melt channelizing through preexisting fabric anisotropies (e.g., Sawyer, 2001) or (b) melt migration along extensional fractures or dilatant structures generated by active stress regimes (e.g., Anderson, 1938, 1951; D'Lemos et al., 1992; Brown and Solar, 1998; Barros et al., 2001; Geshi, 2001). In accordance with previous studies, we favor the generation of extensional structures oriented NNESSW in a progressively crystallizing gabbroic mass as the mechanism responsible for the dioritic emplacement because (a) it is unexpected for a progressively crystallizing magmatic body to hold any preexisting anisotropy; (b) the Kd interfingered bodies and Kd dikes have a persistent orientation within the gabbro (Figure 3d); (c) the vertical geometry of the dioritic bodies suggest a vertical direction of the maximum main stress; and (d) the lack of field evidence for any transpressional or transtensional deformation to produce dilatant structures (e.g., enechelon structures, structures with systematic orientation variation, etc.) during the diorite emplacement.
This proposal may be regionally reconciled with the numerous mafic dikes oriented NNESSW reported by Busby et al. (2006) near El Rosario (Figure 1a; locality 6), which were interpreted by these authors from field observations and UPb in zircon data as synvolcanic faults generated under an extensional regime at ca. 111 Ma.
Felsic units (Kt, Kg1, Kg2 and Kg3)
The geochemistry of the felsic units of the Nuevo Rosarito plutonic suite (Figures 10a and 10b) is consistent with the composition of the Cordilleran batholiths reported by Frost et al. (2001), except for the Kg2 dike, which shows anomalously high alkalis (sample 41XI08; Figure 10b). Nevertheless, chondritenormalized REE patterns of this sample, as well as those of the rest of the felsic units, are consistent with those reported by Gromet and Silver (1987) for the western zone of the Peninsular Ranges batholith. Also, the Sr content, and the Sm/Dy and Sr/Y ratios of all the felsic units can be compared with those reported by Gromet and Silver (1987) and Tulloch and Kimbrough (2003) for the western zone batholith.
The REE pattern of the Kg3 unit is distinct from the rest of the felsic units, specifically the concave shape pattern of their HREE which is indicative of hornblende fractionation (Gromet and Silver, 1987; Bea, 1996).
Synemplacement deformation
The conspicuous intense solidstate fabrics exhibited by the Kt dikes and the Kg1 and Kg2 bodies at the mesoscale (Figures 4e), and the ductile deformation that the gabbro usually shows in the vicinity of the felsic dikes (Figures 4h and 4i), strongly suggest that the ductile deformation in these units was simultaneous to their emplacement. Evidence of synemplacement deformation is also found at the microscale through the submagmatic fractures (Bouchez et al., 1992; Park and Means, 1996) observed within the feldspar grains of many Kt and Kg1 unit samples, as well as the fusion contact microstructure observed in feldspars. Other evidences are the common hightemperature and solidstate microstructures (Vernon, 2000) observed as chessboard extinction in quartz (Mainprice et al., 1986), flame perthites in potassic feldspar (Vernon, 1999), and boudinage in hornblende (Hacker and Christie, 1990).
These mesoscale and microscale observations imply that the Kt dikes and the Kg1 and Kg2 units experienced a transition from magmatic, meltsupported flow to solidstate, grainsupported flow prior to their complete crystallization (submagmatic flow; Paterson et al., 1998; Vernon, 2004). Such submagmatic flow, in addition to their persistent NWSE orientation and NESWdirected lineation (Figures 3g and 3i), further suggests that those felsic units were more or less coeval, and linked together under a single deformational event.
Field observations indicate that the generation of the felsic units started with the emplacement of the Kt unit. In contrast to the Kt dikes which display intense internal fabrics, the Kt massive body exhibits clear magmatic fabrics in the mesoscale (Figures 4b and 4c) and different structural patterns (compare Figure 3e with Figures 3f and 3h). Thus, because deformation is particularly well recorded in the Kt dikes, and in the Kg1 and Kg2 bodies as well, we propose that the emplacement of the 108.4 ± 2.2 Ma old Kt massive body marks the beginning of increasing strain rates, and therefore the initiation of the NEside up deformational event.
The time interval and shear sense of the deformational event reported here is comparable to the intense ductile deformation that, according to Johnson et al. (1999) and Alsleben et al. (2008), mainly occurred between ca. 115 and 108 Ma in Sierra San Pedro Mártir (Figure 1a; locality SSPM), and between ca. 115 and 95 Ma in Calamajué (Figure 1a; locality 5), respectively.
The emplacement of the Kg3 dikes was the last intrusive event. These dikes have distinct orientations relative to the Kt dikes and the Kg1 and Kg2 bodies (compare Figure 3j with Figures 3f and 3h), distinct REE patterns (Figure 8b), and less intense solidstate microstructures relative to the Kg1 unit. These observations suggest that the emplacement of the Kg3 unit may coincide with the decrease of the strain rates and/or the presence of a different stress regime.
SUMMARY AND CONCLUSIONS
The 139.5 ± 2.0 Ma UPb zircon age of the hosting volcanic breccia from the northern part of the suite is contemporaneous with the lower member of the Eugenia Formation located in the Vizcaíno península and the flyshlike assemblages of the PRB transitional zone. In turn, the 151.6 ± 2.6 Ma old granitoid (Jt unit) located in the southern part of the suite is coeval with the San AndrésCedros volcanoplutonic. However, north of Punta Prieta (Figure 1b), plutonic rocks of the PRB intrude the Cretaceous Alisitos Formation, which indicates that the Nuevo Rosarito plutonic suite is located near a boundary between the Cretaceous arc, represented by the Alisitos Formation, and a Jurassic arc, represented by a volcanoplutonic sequence that is contemporaneous to the San Andrés complex in the Vizcaíno peninsula.
Field relationships and structural analyses suggest that the deformational event responsible for the overturning of the host rocks and their intense internal fabrics occurred prior to the Cretaceous emplacement of the Nuevo Rosarito plutonic suite.
Nuevo Rosarito has geochemical characteristics similar to the western zone of the Peninsular Ranges batholith. Their intrusive units have a wide compositional range and a emplacement history that is separated into two phases. The first phase is defined by the emplacement of the mafic units, particularly, to the late crystallization of the gabbro and its fracturation under an extensional stress regime.
We propose that this promoted a local pressure contrast that drew the gabbroic residual melt to produce the NNEoriented diorite bodies. The second phase is defined by the emplacement of the felsic units, particularly when a NEside up deformational event occurred just after the emplacement of the 108.4 Ma old Kt massive body. This event was mainly recorded by the Kt dikes and the Kg1 and Kg2 bodies. The emplacement of the Kg3 dikes would indicate the end of the deformational event.
ACKNOWLEDGEMENTS
This paper was benefited from several discussions with colleagues at CICESE, including J. Fletcher, F. Suárez, A. MartínBarajas, and O. Terán. We thank P. Montecinos, J. Estrada, G. Villalobos, and J. Contreras for comments on an early draft of the paper, Gabriel Rendón, Víctor Pérez, Susana Rosas, and Luis Gradilla for their technical support, and Emmanuelle Frery, Doris Piñeiro, Román Manjarrez, Porfirio Avilez and Patricia Juárez for joining us during fieldwork. Also thanks to Joaquin Ruiz and George Gehrels for allowing us the use of the LAICPMS facilities at the Department of Geosciences, University of Arizona at Tucson, and to Felipe Escalona for his help during the LAICPMS measurements. Financial support was mostly provided by the project CONACyT 45817 granted to Luis Delgado, and by PAICYTUANL CT13109 granted to Fernando Velasco.
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