La estructura semicircular Rancho Nuevo es una estructura geomorfológica definida por patrones de drenaje en la planicie costera de Sonora, localizada a 160 kilómetros al noroeste de Hermosillo. Su extensión es de 15 por 30 kilómetros y está compuesta por un núcleo de plutones de composición félsica-intermedia (granodiorita, monzogranito, cuarzo pórfido y granito), cubiertos por rocas volcánicas del Mioceno. Este trabajo está enfocado a la deformación de los intrusivos que abarcan casi la totalidad del área de estudio. Los plutones consisten en una serie co-magmática fechada entre 71±1.1 y 67.9±1.0Ma (U-Pb en circones, LA-ICP-MS). La unidad más voluminosa es una granodiorita caracterizada por un fracturamiento conspicuo de forma sigmoidal visible a escala de imágenes de satélite de alta resolución, a lo largo del cual se emplazaron diques de composición riolítica de 13.2Ma (U-Pb en circones, LA-ICP- MS). La fabrica magnética (AMS) y los datos paleomagnéticos fueron colectados en 27 sitios en la unidad granodiorita. La fábrica magnética es débil pero bien definida y se caracteriza por contener planos de foliación en la roca bien desarrollados con rumbos que siguen el patrón de fracturamiento sigmoidal sugiriendo un aplanamiento NE-SW a NW-SE, posterior al emplazamiento. La magnetización característica es de polaridad dual, pero dominantemente inversa y consistente con un emplazamiento durante el cron C31r. La magnetización prevalente es suroeste y moderadamente negativa (10 sitios), mostrando una rotación en sentido horario alrededor de 41°±11 con respecto a la dirección de referencia esperada del Cretácico Tardío. Sin embargo, existe evidencia paleomagnética que sugiere que la estructura Rancho Nuevo no rotó como un cuerpo rígido, sino que en su lugar se deformó internamente. Estos datos indican que la estructura semicircular Rancho Nuevo registra cizallamiento, dextral, frágil-dúctil, a gran escala. La edad de los diques y su relación discordante por rocas asignadas a la Toba San Felipe indican que el movimiento dextral de la península de Baja California (y por lo tanto la placa del Pacífico) afectó la costa de Sonora hace aproximadamente 13Ma.
The Rancho Nuevo semi-circular structure is a geomorphological structure defined by drainage patterns in coastal Sonora, about 160km NW of Hermosillo. The structure is about 15 by 30km, and it is cored by felsic to intermediate plutons (granodiorite, monzogranite, quartz-porphyry) covered by Miocene volcanic rocks. This work is focused on the deformation of the intrusives which cover most of study area.The plutons are a co-magmatic suite dated between 71±1.1 and 67.9±1.0Ma (U-Pb zircon, LA-ICPMS). The most voluminous unit is a granodiorite characterized by conspicuous sigmoidal fractures at the scale of high resolution satellite images, along which rhyolite dikes were emplaced about 13.2Ma. Magnetic fabric (AMS) and paleomagnetic data were collected from 27 sites in the granodiorite. Magnetic fabrics are weak but well developed, and are characterized by steep foliation planes with strikes that follow the sigmoidal fracture pattern and suggest NE-SW to NW-SE flattening after emplacement. The characteristic magnetization is of dual polarity, but it is dominantly reverse consistent with emplacement during chron C31r. The prevalent magnetization is southwest and moderately steep negative (ten sites), a discordant direction rotated clockwise about 41°±11 with respect to the expected Late Cretaceous reference direction, also indicating gentle southward tilt. There is, however, paleomagnetic evidence suggesting that the structure did not rotate as a rigid body, but it deformed internally instead. These data are interpreted to indicate that the Rancho Nuevo semicircular structure is a large-scale, dextral, brittle-ductile shear indicator. The age of the dikes and the fact that they are covered discordantly by rocks assigned to the tuff of San Felipe indicate that northwest, srike-slip, motion of Baja California peninsula (and thus the Pacific plate relative to North America) was accommodated by faults in coastal Sonora about 13Ma ago.
Western North America is perhaps the best studied convergent margin in the world, and possibly the best suited to study oceanic plate-continent interactions. The arrival of the spreading center that existed between the Farallon and Pacific plates to the convergent margin of western North America by the end of Oligocene gave rise to major plate reorganization that subsequently resulted in deformation in the plate boundary region. The margin changed from subduction of the Farallon plate under North America to a dextral oblique transform between the Pacific plate and North America. This resulted, eventually, in rifting between Baja California and North America in the Miocene as this block was transferred to the Pacific plate. There is disagreement among the authors working in the region, however, on the timing and the geodynamics of the changes described above. One of the most contentious issues is whether the initial rifting process between Baja California and North America, between about 13 and 6Ma, was orthogonal or dextral-oblique strike slip. Answering this question requires field studies, to determine the timing and kinematics of the faults along the plate boundary region.
Before the arrival of the Farallon-Pacific ridge to the continental margin, the plate boundary evolved as a compressional Cretaceous to Paleogene continental arc where subduction consumed the Farallon plate forming the Peninsular Ranges and the coastal Sonoran batholith.The semicircular structure Rancho Nuevo (RNSS) is part of the coastal Sonoran batholiths. This paper focus is on the deformation of the granitoids of the RNSS in the central coast of Sonora. New field work, geochronology, and paleomagnetic data show that Late Cretaceous intrusives were rotated about a vertical axis and deformed in a dextral-shear couple. This rotation and deformation of the RNSS are interpreted in terms of plate interactions, and contribute to better understanding the Gulf of California history. Here we interpret the semi-circular Rancho Nuevo structure as a feature produced by dextral shear ca. 13Ma. The RNSS is a dextral, en-echelon system, with brittle-ductile structures associated to right-lateral faults that accommodated motion between Baja California (Pacific plate) and Sonora (North America plate).
Tectonic model for Cenozoic evolution of NW MexicoThe geologic evolution of NW Mexico is closely linked to oceanic plate-continent interactions. Subduction of the Farallon plate produced voluminous arc magmatism, and was also the main driver of the Late Cretaceous-Paleogene Laramide orogeny. The Laramide thickened the crust and created significant topography. This event was followed by the basin and range extensional episode along western North America; extension led to crustal thinning. Although the mechanisms for extension and crustal thinning in the basin and range are under debate, these include gravitational collapse of over thickened crust, lithospheric delamination by a mantle plume, and plate boundary interactions such as a slow-down of the plate convergence rate.
The basin and range event is also associated with emplacement of large volumes of felsic and mafic volcanic products (bimodal volcanism). Damon et al. (1981) showed that the position of the magmatic front migrated eastward during the Laramide orogeny, from Sonora to central Coahuila, migrating back to the west during the basin and range extensional event to reach the longitude of the Gulf of California by mid- Miocene time. This evolution can be explained by subduction dynamics: flattening of the slab during the Laramide orogeny and later slab roll-back.
A Late Oligocene to Middle Miocene volcanic arc (27–16Ma) was established between the Peninsular Ranges and coastal Sonoran batholiths, the region that today is occupied by the Gulf of California Umhoefer et al., (2001). Arc magmatism culminated by the end of middle Miocene, marking the end of the subduction process between Farallon and North American plates at the latitude of the Gulf of California. At this latitude subduction was oblique, and relative plate motion in the plate boundary region was partly accommodated by a dextral transtensional system. The time of the tectonic transition from orthogonal basin and range style extension to dextral transtension in the Gulf extensional province (GEP, Figure 1) is, however, controversial.
Geologic map of central-coastal Sonora, showing the location of the Rancho Nuevo semi-circular structure. The inset shows the distribution of plutonic rocks assigned to the Peninsular Ranges and the Sonoran Laramide batholithsas well as the Gulf of California extensional province. Modified from Servicio Geológico Mexicano (SGM), 2008. KsGd-Tn = Upper Cretaceous granodiorite and tonalite; KsTpaGr-Gd = Upper Cretaceous-Paleocene granite and granodiorite; JiAr-Cz-Lm-Cgp=Lower Jurassic sedimentary rocks; pTsDo-Ar=Neoproterozoic metasedimentary sedimentary rocks.
In general terms, the distinction between the Gulf extensional province from the basin and range proper has not been defined. The GEP is the area between the SMO and coastal Sonora and Baja California (Stock & Hodges, 1989). This region experienced crustal extension in wide-rift mode and core complex formation between 25 and 16Ma (Wong and Gans, 2008; Nourse et al., 1994; Vega-Granillo and Calmus, 2003). Subsequent minor extension continued until 12Ma and after (McDowell et al., 1997). This extensional episode is coeval with subduction of the Farallon its fragmentation into other microplates, and arc volcanism in Baja California and Sonora. In Baja California, stratigraphic relationships at Sierra San Felipe indicate that transtentional faulting initiated synchronously as a kinematically linked fault system before ~ 7Ma. This is based on the timing of footwall exhumation, during a phase of rifting that has been called “proto-Gulf” (Seiler et al., 2010). The coastal Sonora region hosts the onshore portion of the transform boundary between the Upper Tiburón and Adair-Tepoca marine basins, two early-formed oblique rift segments. Extension commenced here between 11.5 and 7Ma (Bennett et al., 2013). Based on structural, 40Ar/39Ar geochronology, and a palinspastic reconstruction Gans (1997) proposed the onset of transtension and relative motion of Baja California together with the Pacific plate shortly after the ~11Ma termination of subduction.
Correlation of geologic features on both sides of the Gulf of California (Oskin and Stock, 2003a) indicates about 280km of slip along faults in the gulf, from 6Ma to present (Atwater and Stock, 1998; Oskin et al., 2001). Nonetheless, there are 300km of dextral motion between the Pacific plate and North America that must be accommodated during the proto-Gulf episode between ~12 and 6Ma (Stock, 1989; Stock and Hodges, 1989; Stock and Molnar, 1988). Relative plate motion during the protoGulf event may have been accommodated west of Baja California by the San Benito and Tosco- Abreojos faults (Stock and Hodges, 1989), east of Baja California along coastal Sonora, or in both (Gans, 1997; Fletcher et al., 2007; Bennett et al., 2013).
MethodologyThis work is based on 1:10,000 field mapping of the RNSS, and detailed petrographic analysis of 50 samples, 16 of which were point-counted for modal analysis (with a minimum of 600 points) for later classification in a Streickeinsen diagram (Streickeinsen, 1976). Structural data were collected at 148 stations, including foliation, lineation, dike orientation, bedding attitude, brittle fault plane, and pitch of striations. Five rock samples were dated using U-Pb geochronological analysis by LA-ICP-MS (Laser Ablation-Inductively Coupled Plasma-Mass Spectrometry). Three samples (T-83, T-91, T-92) were prepared, processed, and analyzed at the University of Arizona, Tucson, using standard techniques that include crushing, sieving, magnetic separation and high-density liquids for final extraction of heavy minerals. Zircon separates were mounted manually in epoxy and polished. Zircons were analyzed in a VGI isoprobe multi-collector ICP-MS, equipped with nine Faraday collectors, an axial Daly detector, and four ion counting channels (Gehrels et al., 2006). Two samples (T-205 y TR- 46) were processed for zircon separation at the Centro de Geociencias, UNAM Juriquilla Campus, where they were first crushed and sieved, and then subjected to magnetic separation and heavy liquids extraction (MEI). Zircon separates were then manually mounted in epoxy resin and polished. These two samples were analyzed with an ICP-MS Thermo X series “quadrupole” at Centro de Geociencias in Juriquilla Mexico. (Solariet et al., 2010).
We collected samples in 27 paleomagnetic sites, all in granodiorite, for a total of 162 samples; the samples have a cylinder shape with 1 inch of diameter and 1 inch high. The same samples were used for anisotropy of magnetic susceptibility measurements (AMS) with the objective of observing if there are changes in the magnetic fabric related to post-emplacement deformation. The sampling was performed with a portable drill using diamond tip drillbits; samples were oriented with magnetic and sun compasses. As with all other field stations, sites were located using a portable GPS device. For magnetic susceptibility measurements we used a KLY-3 Kappabridge susceptibilimeter, using 15 positions. For remanence measurements we used a JR-5 Spinner magnetometer. All samples were subjected to progressive demagnetization, either alternating field demagnetization using an ASC LDA-3 up to inductions of 100mT or thermal demagnetization using an ASC-TD48 furnace up to temperatures of 590°C. The main objective of the paleomagnetic part of this study was to determine a possible rotation or tilt within the RNSS by comparing observed directions with the expected direction from the North America craton reference pole for the Late Cretaceous. All magnetic measurements were performed at the Paleomagnetic Laboratory of the Centro de Geociencias, UNAM Juriquilla Campus. Orthogonal demagnetization diagrams were used to interpret the vectorial composition of the natural remanent magnetization (NRM), and characteristic directions were computed using principal component analysis (Kirschvink, 1980). Site mean directions were calculated using Fisher statistics.
Regional geologyThe stratigraphy of western Sonora includes a basement unit composed of various Paleozoic metasedimentary units, with protoliths that range in age from the Cambrian to the Devonian (Gastil and Krummenacher, 1977; Stewart, 1988; Ávila-Ángulo, 1987; Poole, 1993). This assemblage was thrusted over an Upper Paleozoic basin, late in the Ouachita orogeny (Poole et al., 2005). Late Cretaceous plutonic rocks of the Sonoran Laramide batholith intruded the entire basement assemblage (Anderson and Silver, 1969; Gastil and Krummenacher, 1977; Valencia Moreno et al., 2003; Ramos-Velázquez et al., 2008).
The supracrustal units in the GEP in Sonora include four groups after (Oskin and Stock; 2003b, Bennet, 2009; 2013). The oldest, Group I, consists of continental sedimentary rocks of Oligocene-Miocene age. It includes coarse to fine sandstone and conglomerate with basement clasts and clasts of intermediate volcanic rocks. These rocks were deposited by immature fluvial systems and rest unconformably on basement. Group I represents an erosional episode perhaps linked to Basin and Range tectonics within the Gulf of California extensional province.
Group II rocks are likely related to arc volcanic activity associated with the Early-to Middle-Miocene Comondú arc, and subduction of progressively younger Farallon oceanic lithosphere (Umhoefer et al., 2001; Gastil et al., 1979; Hausback, 1984; Oskin and Stock, 2003b; Bennett, 2009). It consists of volcanic flows and pyroclastic deposits of intermediate composition. Although the tuff of San Felipe is included in Group II, and represents the onset of extension in the northern GEP, and it clearly postdates the end of subduction and arc volcanism (Stock et al., 1999; Vidal Solano et al., 2007; 2008). The tuff of San Felipe (Ttsf) is a regional stratigraphic marker that covered an approximate surface of >4000km2 on both margins of the Gulf of California. Distribution of the Ttsf has been used as a piercing point for reconstruction of the peninsula to its pre-opening position because the age of Ttsf is 12.5Ma (Oskin, 2002; Oskin and Stock 2003a). The Ttsf crops out in the RNSS with a thickness of 60m (Figure 2).
Group III consists of basaltic and rhyolitic rocks interstratified with non-marine strata. It is Middle Miocene to Late Miocene (11.47–6.39Ma), (Oskin et al., 2003b; Bennett et al., 2007). The upper age of Group III is considered late Miocene, based on the age of the Mesa Cuadrada tuff of 6.39±0.02Ma, 40Ar39Ar, in plagioclase, published by Bennett et al. (2007). Group III includes ignimbrites regionally distributed over an area >2100km2 on both margins of the Gulf, in Isla Tiburón, (Oskin and Stock, 2003a, b), and in coastal Sonora (Oskin et al., 2001). Mesa Cuadrada tuff deposits are thin, about 30m. Characteristics of this unit that makes it easily recognizable are that it changes laterally from non-welded to poorly welded, and it presents a conspicuous salmon color. The series of rocks deposited between the San Felipe and Mesa Cuadrada tuffs, between 12.5–6.4Ma (Stock et al., 1999), may contain the geologic record of transtension in the Gulf of California. Finally, Group IV consists of sedimentary rocks, characterized by non-marine strata with local intercalations of pyroclastic deposits such as air-fall tuffs. These strata were deposited during the latest proto-Gulf stages (Pliocene-Holocene). Coastal eolian and beach deposits, as well as alluvial and fluvial strata also included in Group IV.
Geology of Rancho Nuevo Semicircular StructureThe RNSS is located in the Sonoran coastal plain, about 160km NW of the city of Hermosillo and about 40km from the coast. RNSS is composed of granitic rocks that intrude an andesite unit mapped as part of the Sonoran Laramide batholith. The RNSS is a domo shaped geomorphic feature defined by conspicuous drainage patterns. The dome may have been produced by a magmatic chamber, or with later erosion. The structure is an elongated dome, with a 30km long axis, oriented nearly N-S, and it is about 15km wide. The arroyos (ephemeral streams) draining small and apparently disorganized sierras outside the structure run into a loop that surrounds the structure, whilst drainage runs radially away from the core of the structure into the same loop. Drainages eventually collect south of the RNSS and flow into playa San Bartolo. The RNSS is cored by suite of Late Cretaceous intrusive rocks (Figure 2). For the description of the geology of the RNSS, we grouped rocks chronologically associated with the Late Cretaceous intrusive suite, and rocks associated with the Miocene volcanic and volcaniclastic sequence.
Late Cretaceous intrusive and volcanic rocks at Rancho NuevoThe Cretaceous suite at the RNSS is composed of plutonic rocks and their host rock. The host rocks are Late Cretaceous, greenish gray andesite flows. These lava flows crop out primarily in the south-central sector of the structure, forming low-standing hills (Figure 2). The andesite unit is intruded by plutonic rocks which include four units: (1) granodiorite-monzogranite, (2) monzogranite, (3) quartz-feldspathic porphyry, and (4) quartzrich granitoid, aplitic and pegmatite dikes. Near the contact with the intrusions the andesite unit it develops neoformations zones, or andesite breccias at greater distance from the contact. The mineralogy of andesite flows consists of plagioclase > pyroxene + chlorite and Fe-oxides.
The granodiorite-monzogranite unit is the largest of the intrusive suite because of its volume and areal extend. It is also important because this unit has a sigmoidal fracture pattern, which is described in the next section. This pattern is further emphasized by the intrusion of a series of Miocene rhyolitic dikes (Figure 2). Outcrops of the granodiorite-monzogranite unit form valleys between minor and discontinuous north-south ranges where plutons of more felsic composition crop out. The granodiorite-mozogranite unit is light to dark gray depending on mafic mineral content. Microscopically, the quartz presents undulatory extinction, and the plagioclases are often fractured or broken forming a matrix of small crystals with quartz and feldspar recrystallization. The biotite abundance increases in zones of hydrothermal alteration. Amphiboles are often corroded, and also altered to chlorite and epidote. Potassium feldspar content gradually increases to the east of the RNSS, where the composition changes transitionally from granodiorite to monzogranite. (Figure 3 and Appendix I).
Intrusive rocks classification diagram, Streickeisen (1976), shows the representative samples distribution of RNSS units. The original data are summarized in Appendix I.
Table of Percentages of quartz, feldspar and plagioclase, and classification of the major intrusive units in RNSS. Nomenclature: Unidad Gd-Mzgr = granodiorite-monzogranite, UnidadGrG = monzogranite GrC = granite rich in quartz, aplitic dikes and pegmatites. And location in UTM WGS84, Zone 12.
| Sample name | Unit | Coord E | Coord N | Quartz% | K-Feld- spar% | Plagioclase % | Classification |
| T 23 Oeste | Gd-Mzgr | 419178 | 3249104 | 17.34 | 25.16 | 57.50 | Gd |
| Oeste | Gd-Mzgr | 417124 | 3250151 | 17.64 | 25.40 | 56.94 | Gd |
| PdA | Gd-Mzgr | 421360 | 3252144 | 16.55 | 27.35 | 56.10 | Gd |
| T 35 | Gd-Mzgr | 422750 | 3255818 | 14.69 | 39.30 | 46.01 | Gd |
| T 30 | Gd-Mzgr | 416533 | 3253342 | 29.78 | 23.27 | 46.93 | Gd |
| T 33a | Gd-Mzgr | 421297 | 3253474 | 16.28 | 41.20 | 42.50 | Gd |
| T 212 | Gd-Mzgr | 418797 | 3253613 | 27.52 | 27.52 | 49.94 | Gd-Mzgr |
| T 30 A | Gd-Mzgr | 417126 | 3252972 | 13.78 | 35.42 | 41.88 | Mzgr |
| NWGA | Gd-Mzgr | 427007 | 3259018 | 31.11 | 28.90 | 39.95 | Mzgr |
| T 209 | Gd-Mzgr | 418206 | 3253914 | 31.64 | 33.67 | 34.68 | Mzgr |
| T 21 2 GB | Gd-Mzgr | 418853 | 3253558 | 34.70 | 40.78 | 24.51 | Mzgr |
| T 214 | Gd-Mzgr | 418511 | 3253372 | 25.28 | 49.66 | 27.04 | Mzgr |
| TR 12 36 | Gd-Mzgr | 424988 | 3248395 | 26.86 | 47.71 | 25.42 | Mzgr |
| T 4 | GrG | 419832 | 3243410 | 28.23 | 39.30 | 32.47 | Mzgr |
| T 1 | GrG | 420614 | 3243460 | 38.69 | 39.43 | 21.88 | Mzgr |
| T 29 | Grc | 416289 | 3252218 | 13.78 | 61.87 | 24.40 | Grcz |
The granodiorite-monzogranite unit is intruded by coarse-grained monzogranite unit. Characterized by a distinctive texture of large feldspars phenocrytals and marked mineral lineation and in outcrop it presents a pinkish coloration due to K-feldspar content and biotite oxidation. The monzogranite crops out on the southern and western sides of the structure (Figure 2). The monzogranite presents various families of fractures with different orientations, which are often filled by aplitic dikes and pegmatites. Locally, the monzogranite includes granodiorite xenoliths, which lack reaction rims and do not present preferential orientation. Xenoliths may be as much as 20cm in diameter but are generally between 5 and 10cm. In thin section, this rock is composed of quartz with undulatory extinction, both microclines and orthoclases are 1 to 2cm in length, plagioclase crystals are not zoned but a number of them are broken up or deformed as kink-bands. Plagioclase rims are often corroded and show quartz-feldspar recrystallization. This is often a feature produced by crystal-plastic deformation (Vernon, 1975). Many biotite and amphibole crystals are altered to chlorite, epidote and Fe-oxides.
The quartz-feldespatic porphyry unit crops out in the south-central part of the RNSS, forming small hills. To the northeast of the structure, the porphyry intrudes the granodiorite-monzogranite unit in the form of dikes with a preferred orientation 10° to 20° NW (Figure 2). Quartz and K-feldspar crystals are embedded in an aphanitic matrix. Potassium-feldspar (orthoclase) is commonly broken up and shows sericitic alteration. Many plagioclase crystals are zoned. Biotite grains are euhedral; most of them are fractured, corroded, oxidized and sericitized. There are small amounts of hornblende altered to epidote, chlorite and Fe-oxides.
The granite rich in quartz, aplite and pegmatite dikes unit is the kind of facies typically associated with late crystallization phases in the magma chamber. The granite bodies are scarce within the RNSS, cropping out as scattered apophyses not larger than ~100m in diameter. They are light gray and of fine-grained texture. The aplitic and pegmatites dikes are generally less than 1m thick, and show no preferred orientation. More common mineralogical association in these dikes is quartz, potassium-feldspar, plagioclase, mica, and accessory tourmaline.
The Miocene volcanic and sedimentary rocksMiocene volcanic and intrusive rocks in the RNSS either unconformably overlie the Cretaceous plutons or intrude in to them. They were mapped as three compositional units: rhyolite lava, rhyolitic tuffs, and basalts flows. The rhyolite unit includes dikes filling sigmoidal fractures within the granodiorite-monzogranite main pluton, as well as associated domes which are coeval. The rhyolite dikes occur mostly in the western side of the RNSS, but dikes cut the entire structure from north to south; they also occur in the central-eastern side and cut quartz feldspatic porphyry (Figure 2). The dikes form as discontinuous prominent ridges, rising tens of meters above their surroundings. As mentioned earlier, rhyolites dikes follow sigmoidal trends striking N-S in the north, NE-SW in the center, and NNW in the south. The sigmoidal fracture pattern that they intrude was developed earlier or during the emplacement of the rhyolitic dikes within the granodiorite-monzogranite. The rhyolite dikes are ~ 2km long, but they are narrow (2–4m). The rhyolite unit also includes domes up to 400m in diameter. Generally they are pink to reddish-gray because of the presence of Fe-oxides. They have an aphanitic texture, containing <5% of quartz, feldspar or plagioclase phenocrysts.The rhyolite also contain small crystals of fayalite, aegirine (<1%), and arfvedsonite (<1%), which are indicators of high alkaline composition (Vidal-Solano, personal communication 2012).
Dispersed across the RNSS, there are outcrops of volcanic and volcaniclastic rocks mapped as the rhyolitic tuff unit. These rocks generally occur as small remnants, filling paleo-valleys between minor ranges composed of granitoid. The largest outcrops are about 3km2 in the east-central side of the RNSS. The base of the volcaniclastic sequence is formed by tuffaceous breccias, which include clasts of the volcanic and granitic older units, overlain by a well-stratified volcanic sequence. This sequence is composed of ~18m thick a black vitrophyre, lapilli tuffsof rhyolithic composition, ~20m of pinkish lithic tuff of rhyolitic composition, about 3m of clear fine-grained tuff (pumicite), and a second vitrophyre 4m thick. The sequence overlies ~18m of pinkish and yellowish tuff for a total thickness of about 60m. This unit is gently tilted, 5°–18° to the west, probably produced by the paleo-geography. The petrological characteristics of this unit suggest that it may correlate with the tuff of San Felipe. The basalt unit in the map (Figure 2) is restricted, to isolated outcrops scattered along the RNSS; however, the contact with the underlying intrusions is not well exposed. In the central part of the structure basalts flows dip gently ~10° to the northeast.
GeochronologyFive samples within the RNSS were selected for U-Pb zircon dating. Analytical results are summarized in Appendix 2, and results are summarized in Figure 4 and Table 1. An isotopic age of 79.5±1.0Ma (Campanian) was obtained for sample T205 of the andesite unit, host rock to the Rancho Nuevo intrusive suite. The age is based on the average of 11 concordant grains. The zircon analysis of the intrusive rocks yielded ages of 71±1.1Ma (sample T92, from granodiorite-monzogranite, average of 27 concordant grains), 68±1.0Ma (sample T91, monzogranite, average of 24 concordant grains), and 67.9±1.0Ma (sample T83, quartz-feldspar porphyry, average of 24 concordant grains). The ages obtained are consistent with field relations, as the granodiorite-monzogranite is intruded by the younger granitic and subvolcanic units. A rhyolitic feeder dike yielded a crystallization age of 13.2±0.4Ma (Figure 4, and Table 1) based on the average of 10 concordant grains.
The Rancho Nuevo granodiorite-monzogranite unit contains sigmoidal fractures hundreds to tens of meters long, where most of the fractures were filled by viscous rhyolite. These fractures were clearly formed after pluton emplacement. The sigmoidal pattern of fractures and rhyolite dikes is clearly visible on satellite images of high resolution. Figure 5. The fractures and dikes are nearly vertical (79°–90°). In the north, fractures and dikes strikes are predominantly 20°–30° to NE (Figure 6a), and change orientation to 0°–10° NNE in the central portion of the range (Figure 6b), whilst in the south fractures and dikes strike 0°–10°NNW (Figure 6c). Figure 6d shows the strike of the complete data set, with a resultant strike. The geometry of the fractures and dikes in the RNSS resembles an en-echelon, dextral-shear indicator, formed in a brittle-ductile environment. Apparently, the continuation of the Rancho Nuevo sigmoidal struture is buried by alluvial deposits south and north of the RNSS (Figure 2).
The granodiorite-monzogranite body does not display a macroscopic foliation or mineral lineation, nor ductile shear zones. Other kinematic indicators are striations in the internal faces of the factures where rhyolite dikes were emplaced. These observations combined with observations of microscopic brittle deformation and plagioclase recrystallization, suggest that deformation occurred at relatively shallow crustal levels. The coarse-grained granite unit in the southern extreme of the RNSS is characterized by variable but nearly N-S magmatic foliation defined by feldspatic phenocrystals that deep steeply >70° to the east.
Anisotropy of magnetic susceptibilityBecause of the scarcity of kinematic indicators and the homogeneity of the Cretaceous granitoids, we employed anisotropy of magnetic susceptibility (AMS) as an estimate of strain recorded by intrusive rocks of the RNSS. AMS fabric often parallels the orientation of the strain ellipsoid, but interpretation may not be straightforward. AMS fabrics are represented by an ellipsoid defined by the axis of maximum, intermediate and minimum susceptibility (kmax, kint, and kmin). The maximum and intermediate axes define the magnetic foliation plane, while the shape of the ellipsoid is described using relations between the axes in terms of the parameter T (T<0 for prolate ellipses, and T>0 for oblate ellipses). The intensity of the fabric is evaluated with the percentage of anisotropy (Pj) parameter (Table 2).
Summary AMS data of RNSS.
| Site | N | Kmean | K1 | K2 | K3 | Dec K1 | Dec k2 | Dec k3 | Inc k1 | Inck2 | Inck3 | L | F | P | Pj | T | U |
| RN1 | 12 | 1.18 e-2 | 1.004 | 1.001 | 0.995 | 339.7 | 79.1 | 242.3 | 8.4 | 47.7 | 41.1 | 1.003 | 1.007 | 1.01 | 1.01 | 0.385 | 0.383 |
| RN2 | 9 | 2.91 e-2 | 1.066 | 1.056 | 0.878 | 46.9 | 315.2 | 139.8 | 2.2 | 37.4 | 52.5 | 1.009 | 1.204 | 1.215 | 1.246 | 0.907 | 0.898 |
| RN3 | 6 | 2.66 e-2 | 1.023 | 1.015 | 0.962 | 50.9 | 161.3 | 315.6 | 10.7 | 61.4 | 26.1 | 1.008 | 1.0055 | 1.063 | 1.069 | 0.741 | 0.734 |
| RN4 | 9 | 1.09 e-2 | 1.014 | 1.004 | 0.982 | 222.4 | 45.7 | 313.5 | 35.6 | 54.3 | 1.6 | 1.01 | 1.022 | 1.032 | 1.033 | 0.389 | 0.383 |
| RN5 | 12 | 6.58 e-3 | 1.016 | 0.998 | 0.986 | 53.7 | 173.9 | 320.1 | 11 | 68.9 | 17.8 | 1.018 | 1.012 | 1.03 | 1.03 | -0.213 | -0.220 |
| RN6 | 13 | 2.03 e-2 | 1.017 | 1.008 | 0.975 | 6.4 | 248.4 | 99.6 | 9.9 | 69.5 | 17.8 | 1.01 | 1.033 | 1.043 | 1.045 | 0.547 | 0.54 |
| RN7 | 9 | 1.81 e-4 | 1.006 | 1.002 | 0.992 | 100.1 | 241.7 | 8.2 | 11.7 | 75.2 | 8.9 | 1.003 | 1.01 | 1.013 | 1.014 | 0.488 | 0.485 |
| RN8 | 10 | 1.82 e-2 | 1.028 | 1 | 0.972 | 167.3 | 76.3 | 333.9 | 15.3 | 3.4 | 74.3 | 1.028 | 1.028 | 1.058 | 1.058 | -0.002 | -0.016 |
| RN9 | 7 | 2.94 e-2 | 1.019 | 1.003 | 0.978 | 262.8 | 170.8 | 75.6 | 31.9 | 3.2 | 57.9 | 1.016 | 1.025 | 1.042 | 1.042 | 0.222 | 0.212 |
| RN10 | 9 | 3.06 e-2 | 1.04 | 0.993 | 0.967 | 207.9 | 69.2 | 327.9 | 54.4 | 28.6 | 19.9 | 1.047 | 1.027 | 1.075 | 1.076 | -0.226 | -0.283 |
| RN11 | 7 | 5.57 e-2 | 1.027 | 0.989 | 0.984 | 190.8 | 100.5 | 283 | 0.08 | 20.2 | 69.8 | 1.038 | 1.006 | 1.044 | 1.047 | -0.74 | -0.745 |
| RN12 | 7 | 1.53 e-2 | 1.017 | 0.997 | 0.986 | 40 | 298.4 | 180.4 | 29.8 | 19.3 | 53.4 | 1.019 | 1.011 | 1.031 | 1.031 | -0.252 | -0.259 |
| RN13 | 7 | 1.75 e-2 | 1.011 | 1.004 | 0.984 | 169 | 289.4 | 76.7 | 8.7 | 73.2 | 14.3 | 1.007 | 1.021 | 1.028 | 1.029 | 0.497 | 0.492 |
| RN14 | 6 | 1.19 E-2 | 1.017 | 1.003 | 0.98 | 9 | 244.9 | 129.8 | 39.5 | 34.3 | 31.9 | 1.014 | 1.023 | 1.038 | 1.038 | 0.224 | 0.215 |
| RN15 | 10 | 1.68 e-2 | 1.032 | 1.001 | 0.966 | 74.5 | 225.1 | 323.4 | 56 | 30.5 | 13.7 | 1.031 | 1.037 | 1.069 | 1.069 | 0.081 | 0.064 |
| RN16 | 7 | 1.72 e-2 | 1.026 | 0.998 | 0.976 | 41.3 | 282 | 133.1 | 7.2 | 74.6 | 13.6 | 1.028 | 1.022 | 1.051 | 1.051 | -0.11 | -0.122 |
| RN17 | 9 | 1.67 e-2 | 1.026 | 0.999 | 0.975 | 196.6 | 303.6 | 94.5 | 14.9 | 47.8 | 38.4 | 1.027 | 1.024 | 1.053 | 1.053 | -0.057 | -0.07 |
| RN18 | 8 | 2.1 e-2 | 1.028 | 0.999 | 0.973 | 111.3 | 4.7 | 263.4 | 48.6 | 14.1 | 37.9 | 1.028 | 1.027 | 1.056 | 1.056 | -0.031 | -0.044 |
| RN19 | 8 | 9.12 e-4 | 1.01 | 0.998 | 0.992 | 168.8 | 69.5 | 265 | 7.7 | 50.3 | 38.6 | 1.012 | 1.006 | 1.018 | 1.018 | -0.342 | -0.346 |
| RN20 | 8 | 1.99 e-2 | 1.032 | 1.017 | 0.95 | 113.9 | 258.2 | 354 | 63.4 | 22.1 | 14 | 1.014 | 1.071 | 1.086 | 1.092 | 0.653 | 0.641 |
| RN21 | 6 | 1.24 e-2 | 1.013 | 0.994 | 0.993 | 92.2 | 329.2 | 213.1 | 38.6 | 34.3 | 32.8 | 1.019 | 1.001 | 1.02 | 1.023 | -0.864 | -0.865 |
| RN22 | 6 | 2.2 e-2 | 1.015 | 0.998 | 0.987 | 195.7 | 311.5 | 80.3 | 28.6 | 38.6 | 38.2 | 1.017 | 1.011 | 1.029 | 1.029 | -0.229 | -0.236 |
| RN23 | 7 | 4.74 e-3 | 1.011 | 1.005 | 0.983 | 150.5 | 35.2 | 301.5 | 67.5 | 10 | 20 | 1.006 | 1.023 | 1.029 | 1.03 | 0.578 | 0.573 |
| RN24 | 7 | 6.97 e-3 | 1.011 | 1.003 | 0.987 | 199.1 | 353.1 | 94 | 48 | 39 | 13.1 | 1.008 | 1.016 | 1.024 | 1.025 | 0.337 | 0.331 |
| RN25 | 7 | 5.45 e-3 | 1.011 | 1.007 | 0.982 | 178.9 | 357.8 | 88 | 69.7 | 20.3 | 0.3 | 1.003 | 1.026 | 1.03 | 1.032 | 0.772 | 0.769 |
| RN26 | 6 | 1.24 e-2 | 1.02 | 0.999 | 0.981 | 354 | 120.6 | 211.2 | 82.2 | 4.7 | 6.2 | 1.021 | 1.018 | 1.039 | 1.039 | -0.06 | -0.069 |
| RN27 | 6 | 1.006 | 1.002 | 0.991 | 291.5 | 142.4 | 36.2 | 41.4 | 44.3 | 16.1 | 1.004 | 1.011 | 1.015 | 1.016 | 0.452 | 0.449 |
AMS studies have been applied to the systematic study of plutonic rocks, which generally have relatively simple magnetic mineralogy (Borradaile, 1988; Borradaile and Henry, 1997). The interpretation of these data, however, can be difficult because the magnetic susceptibility ellipsoid often reflects the combination of emplacement related strain (due to magma flow or interaction with the host rock), regional strain during emplacement, as well as solid-state deformation after emplacement.
AMS data were obtained in all 27 drilled sites. The samples were measured prior to beging demagnetized, Magnetic susceptibility for samples of the granodiorite-monzogranite are high, with the mean of the samples ranging between about 5×10−3 and 6×10−2 SI units, except for sites 7 and 19 that have significantly lower values (between 1 and 9×10−4). The high susceptibility values suggest that the magnetic fabric is dominated by the ferromagnetic mineral phases (Ellwood and Wenner, 1981). Despite the fact that the granodiorite-monzogranite unit does not display a visible fabric, there is a weak but well-defined magnetic fabric. Percentage anisotropy is relatively low, with an average value of 1.048 (typical of undeformed to weakly deformed granitoids), but with a wide range between 1.010 and 1.246; the high values suggest that high strain is recorded at some sites. The highest values of percent anisotropy (Pj>1.06) were observed in the northern and eastern sides of the mountain range. The shape parameter T varies within the Rancho Nuevo sigmoidal structure. Four sites in the central part of the RNSS have a range of T between −0.002 and −0.11, indicating nearly tridimensional to weakly prolate ellipsoids (Figure 7, Table 2). In the northern and southern sectors of the structure, ellipsoids are dominantly prolate (at six sites T ranges between −0.252 and −0.864). Nonetheless, at rest of the sites T typically has positive values indicating ellipsoids of oblate shape. Oblate ellipsoids suggest generally SE- NW to NE-SW compression.
Drilling sites for paleomagnetism and magnetic fabric, the stereograms represent the graphics (AMS) in lower hemisphere. Squares correspond to maximum, triangles to intermediate, and circle to minimum susceptibility axes. The black line symbolize average magnetic folitation plane for each particular site in granodiorite-monzogranite unit.
The orientation of kmax, kint and kmin is displayed in Figure 7. The orientation of the AMS foliation in the granodiorite-monzogranite unit is generally parallel to the dike orientations, such as in sites 13 through 17 in the NE side of the sigmoid, sites 6 and 11 in the northern side, and sites 21 to 25 in the southern sector of the sigmoid (Figure 7). There are, however, significant deviations with foliation planes oblique to the structure, such as sites 20 and 21, as well as 7. These sites generally show the lowest percentage anisotropy values (<1.015), suggesting they were not affected significantly by deformation after emplacement. Magnetic lineation, interpreted from kmax, suggests roughly a NNE-SSW direction and small elongation in the northern part of the RNSS, and N-S and moderately steep in the southern part.
PaleomagnetismSamples of the granodiorite-monzogranite collected at Rancho Nuevo generally have moderately strong magnetizations, and relatively straightforward demagnetization behavior. The NRM is typically the sum of two magnetizations. A low coercivity magnetization is removed with inductions of about 12mT (Figure 8). The directions of the low coercivity component show no prevalent within-site orientation. A moderate-coercivity (20–80mT) magnetization is defined by linear trajectories to the origin, and it is considered the characteristic magnetization (ChRM). The direction of the ChRM is typically to the SW and moderately steep negative, or antipodal to this direction, but it is to the southwest and shallow at three sites in the north and the west sides of the structure and to the NW (SE) and moderately steep positive (negative) at sites 9 and 19 (Figure 8, Table 3). A ChRM was identified at 16 sites, but in one of them the statistic is poor. Within-site dispersion of the ChRM is low, with precision parameter generally higher than 50. At eleven sites no stable magnetization was observed. In some of these sites the NRM is of very low coercivity, and directions within a site have high dispersion; in others demagnetization behavior is erratic. The ChRMin 15 sites are predominantly of reverse polarity, consistent with emplacement during C31r. based on the average age of ~70Ma, for granitoids.
Paleomagnetic data. (a-c) Orthogonal demagnetization diagrams of selected samples. Open (closed) symbols are projections on the vertical (horizontal) plane. (d) Stereographic projection of the characteristic magnetization (in situ), here open (closed) symbols are projections on the upper (lower) hemisphere.
Paleomagnetic data and statistical parameters.
| Site | n | Dec (°) | Inc (°) | k | a95 | Dec (°) | Inc (°) |
| rnl | 1 | 204.9 | −13.7 | 202.6 | −12.6 | ||
| rn5 | 3 | 233 | 2.4 | 76.9 | 14.2 | 233.1 | −1.5 |
| rn6 | 4 | 211.6 | 16.7 | 162.6 | 7.2 | 214.6 | 16.2 |
| rn9 | 3 | 146.8 | −37.4 | 44 | 18.8 | 144 | −28 |
| rn15 | 3 | 247.3 | −41.1 | 76.3 | 23.4 | 240.1 | −46.4 |
| rn16 | 5 | 236.4 | −35.1 | 20.0 | 17.5 | 229.4 | −39 |
| rn17 | 6 | 233.9 | −49.5 | 288.7 | 3.9 | 222.1 | −52.6 |
| rn18 | 6 | 231.5 | −48.4 | 46.0 | 10.0 | 220.1 | −51.1 |
| rn19 | 2 | 341 | 55.1 | 333.5 | 47.1 | ||
| rn20* | 6 | 185.4 | −68.3 | 10.9 | 21.3 | 167.1 | −62.7 |
| rn21 | 6 | 233.7 | −59.6 | 393.2 | 3.4 | 216.2 | −62.2 |
| rn22 | 4 | 199.5 | −62.4 | 54.7 | 12.4 | 182.5 | −59.1 |
| rn24 | 6 | 197.5 | −49.3 | 152.9 | 5.4 | 187 | −46.2 |
| rn25 | 6 | 196.8 | −47.1 | 505.6 | 3.0 | 187.1 | −44 |
| rn26 | 6 | 21.3 | 44.6 | 498.7 | 3.0 | 12.1 | 42.3 |
| rn27 | 3 | 211.4 | −43.3 | 203.8 | 8.7 | 202.1 | −42.7 |
| Mean | 10 | 219.7 | −49.5 | 28.4 | 9.2 | 207.9 | −50.2 |
Here n is the number of samples used in the calculation of the site mean.
Dec and Inc are the declination and inclination, with statistical parameters k and alpha 95. Dec+ and Inc+ correspond to tilt corrected directions.
Between-site dispersion appears high, but a group of ten sites yields a well defined mean direction of D=219.7° and I=−49.5° (k=28.4 and a95=9.2°); this calculation includes most of the sites in the southern and eastern sides of the structure. Corrected for the gentle westward tilt of the Miocene tuffs near El Volteadero ranch in the center of the structure, the direction is D=207.9° and I=−50.2°. The ChRM is discordant with respect to the direction calculated for the sampling locality from the North America reference pole, which is D=166.1° and I=−56.9° (based on Besse and Courtillot, 2002). The mean direction indicates clockwise rotation of 41.8°+/−11.6°, with small flattening (F=6.7°+/−3.4°). For individual sites, calculations of R(rotation) range between about 16° and 74°. It appears, however, unlikely that the RNSS rotated as a rigid body, as sites in the north and west with southwesterly and shallow ChRM indicate a combination of rotation and tilt (southward), and two sites (9 and 19) do not record significant rotation.
DiscussionTo our knowledge, this is the first study where the deformation of intrusive rocks in the extensional province of the gulf is analyzed. The most evident indication of deformation in the RNSS is the presence of a sigmoidal structure, which later on was filled by viscous rhyolite as dikes.The sigmoidal structure appears to have been produced by the gash extensional fractures (σ3) which are perpendicular to the maximum stress (σ1, Figure 9). The fractures may be rotated by ductile deformation either during or after formation. As gash fractures develop at different times of ductile shearing they show different amounts of rotation. This deformation coincides with the results of the paleomagnetic study.
Schematic model of a right-lateral, brittle-ductile, en-echelon pattern of fractures developed in the Rancho Nuevo granitoids and filled by Miocene hyperalkaline dikes. Also indicate the gash fractures formed as extensional fractures that are perpendicular to the minimum compressive stress, Where, σl is a maximun stress and σ3 is minimun stress.
The AMS is a technique that defines the orientation and intensity of the magnetic fabric in the rocks. The AMS in the granodiorita-mozogranite unit of the RNSS shows that considerable changes in the orientation of the magnetic fabric exist in the rock, indicating that they record significant strain. Also, the characteristic magnetization of the granodiorite-monzogranite is discordant with respect to the expected direction; the discordance is best explained by rotation about a local nearly vertical axis of about 40°. As mentioned above, not all sites record the same amount of rotation. For instance, sites 5 and 6 in the western side of the structure require a combination of rotation and tilt. This suggests that the structure did not behave as a rigid body during deformation. Based on the crystallization age (U-Pb) for the dikes of rhyolite, which are considered coeval or little younger than the dextral transtentional deformation, we conclude strike-slip deformation occurred by about 13Ma.
Prior to ~16Ma, the southwestern edge of the North American plate along northwestern Mexico was a subduction boundary (Fig. 2A; Atwater, 1970). By ~12.5Ma, the Rivera- Pacific-North America triple junction jumped southeastward, setting the stage for transfer of the Baja peninsula to the Pacific plate. Karig and Jensky (1972) proposed that prior to the gulf existed in the area in the earliest stages of rifting from ca. 14 to 6Ma a simple orthogonal extensional regime. Gastil and Krummenacher (1977), as well as Gastil et al. (1999), by means of reconnaissance mapping with geochronologic data determined that the timing of extensional faulting along coastal Sonora, between Puerto Lobos and Bahia Kino, occurred between 10–7Ma but more likely before 9Ma.
Stock and Hodges (1989) first proposed the ‘strain partitioning’ model for the Pacific-North America plate boundary. The model was supported by estimations of the timing and direction of extensional structures during proto-Gulf time, along with estimations of the direction and amount of Pacific-North America plate motion throughout Miocene time. Neuhaus (1989) studied volcanic rocks in Isla Tiburón with ages between 19 and 15 Ma that were tilted between about 13 and 11Ma. Based on refined geochronology, additional structural observations, and paleomagnetic data, Oskin et al. (2001), as well as Oskin and Stock (2003a), proposed that dextral motion of Baja California was accommodated by faults within the gulf between about 6–7Ma and the present. Bennett (2013), used paleomagnetic, geochronological and structural data to conclude that the extension in coastal Sonora commenced between 11.5Ma and 7Ma.
Dextral slip oriented parallel to the Gulf of California (roughly NNW) in the coast of Sonora is inferred from the geometry of the Rancho Nuevo semicircular structure. The geometry is consistent with a very large-scale,en-echelon, brittle-ductile shear zone, and this geometry is supported by deformation recorded by AMS fabric and paleomagnetically determined clockwise rotation of about 40°; the model is illustrated in Figure 9. Rhyolite dikes and domes emplaced along sigmoidal fractures in the RNSS are hyperalcaline (Vidal Solano et al., 2007).They are related to extension, and their crystallization age is ~13Ma, and they are discordantly covered by the tuff of San Felipe dated at 12.5Ma by Vidal Solano et al. (2007) and Stocket al. (1999).
Our findings suggest that deformation of Cretaceous plutonic rocks at Rancho Nuevo is driven by transtensional shearing along dextral strike-slip faults north and south of the structure, such as the Sacrificio, Infiernillo, and Kino bay faults (Bennett and Oskin, 2007); these faults are most likely related to transtensional motion of Baja California peninsula, and thus the Pacific plate. Some authors (e.g., Oskin and Stock, 2003a,b; Bennett, 2009; and Darin et al., 2012) have proposed that right-lateral slip of the peninsula is limited to 7-0Ma, based on studies of the Miocene volcanic sequence of coastal Sonora. Nonetheless, in this study we recognized the emplacement of hyperalkaline dikes with crystallization ages of ~13Ma, in plutonic rocks defining anen-echelon dextral geometry. The structural observations, such as the presence of striations, crushed plagioclase at microscopic scale, and the magnetic fabric are consistent with a brittle-ductile setting. The deformation is dated at about 13Ma based on the overlap relationship between tuff San Felipe and rhyolite dikes. Magnetic anisotropy is also consistent with ENE flattening linked to NNE right-lateral shear. We notice that the prolate AMS fabrics at the extremes of the RNSS are also consistent with elongation caused by right-lateral shear. The most convincing evidence of dextral slip and transtensional shearing in late Middle Miocene time is provided, however, by the clockwise rotation observed in the central and southern part of the Rancho Nuevo sigmoid structure. This transtensional deformation is thus related to North America-Pacific plate motion early during the capture of the Baja California Peninsula by the Pacific Plate. may record similar deformation. They include a rhomboidal structure at playa San Bartolo, 27km to the southwest of Sierra Rancho Nuevo, and a series of dikes located 30km to the north of the of it, these dikes have a length of the 17km oriented NNW, suggesting strong structural control by Miocene faults.
ConclusionsThe semi-circular Rancho Nuevo structure is a structural dome exposing a Late Cretaceous Plutonic suite partially covered by the ~12.5Ma tuff of San Felipe. The core of the structure includes granodiorite-monzogranite, monzogranite, quartz-feldespathic porphyry, and granite rich in aplitic dikes and pegmatites. This suite has crystallization age between about 71 and 68Ma. The plutonic suite is intruded by ~13Ma (U-Pb zircon) Miocene dikes and disconformably covered by Miocene volcanic rocks.
A sigmoidal fracture pattern affected the plutonic rocks of the RNSS, and it is best developed in the granodiorite-monzogranite body. The fractures were filled by Miocene hyperalkaline dikes, defining an en-echelon, brittle-ductile, dextral shear indicator of kilometric scale. Magnetic anisotropy in the plutonic rocks shows a foliation that commonly follows the strike of the dikes, and thus records post-emplacement crystal plastic deformation. In thin section, this deformation is observed as crushed plagioclase grains, undulatory extinction in quartz, and kink-bands. Magnetic fabric suggests elongation to the NNW-ESE, and NW-SE to NE-SW flattening.
The characteristic magnetization in granodiorite of the RNSS is to the southwest and moderately steep negative, indicating (when compared to the expected reference direction) ~40° horizontal rotation about a vertical axis. Rotation is unlikely to have occurred as a simple rigid block. Instead, paleomagnetic data suggest internal deformation of the structure within a zone of dominant right-lateral strain. Therefore, we propose that NNW trending right-lateral faults bound the Rancho Nuevo crystalline block and were active during emplacement of ca. 13Ma hyperalkaline dikes in the RNSS. This suggests that strain was localized. We also propose that these faults accommodated part of the NW motion of Baja California peninsula during the proto-Gulf event.
We thank CONACYT who supported the research of D.García and R. Molina with CB grant 12982. We also thank Thierry Calmus, José Luis Rodriguez C, and Sergio Salgado S. for their comments and support. Alexander Iriondo provided direction and support in U-Pb determinations at Centro de Geociencias, Juriquilla. We also thank Aimée Orci Romero for thin section preparation, Pablo Peñaflor Escárcega for help in sample preparation, and Jesús Vidal Solano for valuable comments to previous version of this manuscript and discussion of hyperalcaline magmas. We thank Mr. Pilo Galáz y Mr. Miguel Robles for access to their properties, as well as Gonzalo Ibarra for his assistance in the field. We thank Dr. Garcia y Barragán, for his detailed review of the paper. The comments of K. Busby and treewo anonymous reviewers served to improve this article and are greatly appreciated.