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Andean geology

On-line version ISSN 0718-7106

AndGeo vol.38 no.1 Santiago Jan. 2011


Andean Geology 38 (1): 37-63. January, 2011
formerly Revista Geológica de Chile


Middle-Late Jurassic to Early Cretaceous transtension and transpression during arc building in Central Chile: evidence from mafic dike swarms

Transtensión y transpresión del Jurásico Medio-Superior al Cretácico Inferior durante la construcción del arco magmático en Chile central: evidencia a partir de enjambres de diques máficos


Christian Creixell1*, Miguel Ángel Parada1, Diego Morata1, Paulina Vásquez2*, Carlos Pérez de Arce3, César Arriagada1

1   Departamento de Geología, Universidad de Chile, casilla 13518, Correo 21, Santiago, Chile.;;;
2   Techniche Universität Berlin, Fachgebiet Mineralogie-Petrologie, Sekr. ACk 9, Ackerstrafie 71-79, 13355 Berlin, Germany.
3  Laboratorio de Geocronología, Servicio Nacional de Geología y Minería, Tiltil 1993, Santiago, Chile.
* Present address; Servicio Nacional de Geología de Geología y Minería, Avenida Santa María 0104, Santiago, Chile. Phone; 56-2-4825500, Fax 56-2-7372026.

ABSTRACT. The Middle-Late Jurassie mafic dike swarms of central Chile between 33°and 33°45'S registerthe tectonic activity of the contemporaneous are represented by the Coastal batholith. These dike swarms evidence alternate episodes of transtension and transpression across NW-striking structures, which controlled the construction of the magmatic are. The Middle-Upper Jurassie and Lower Cretaeeous mafic dike swarms in the Coastal range of central Chile has been studied through field observations, geochronology and AMS (anisotropy of magnetic susceptibility) to document the tectonic and magmatic evolution of the Jurassic-Cretaceous are at this latitude. Middle to Upper Jurassie dike swarms (Concón and Cartagena mafic dike swarms) were emplaced between 163 and 157 Ma, along NW-SE to WNW-ESE-striking host fractures, registering a first stage of magma emplaeement under simstral transtension. During this stage, dikes acquired a fabric characterized by magnetic foliation clock wise oblique to dike trend and gently plunging lineations. This stage was followed rapidly by dike emplaeement under sinistral transpression, with associated steeply plunging lineations in the dikes, reverse shear zones in the country rocks and local oceurrence of horizontal mafic dikes. On the other hand, the Lower Cretaeeous El Tabo dike Swarm was emplaced along tensile fractures that do not register shear displacements along their walls. These dikes were emplaced at shallower crustal levels along tensile fractures.Within each dike swarm, differences in the tectonic style of emplaeement correlates with changes in the geochemical composition of the dikes, suggesting a strong coupling between tectonics and nature of magma supplies in the are. Finally, the current results show that the Mesozoic evolution of the Coastal Batholith of central Chile oceurred in several stages of deformation and not under a simple scenario of extensional tectonics. This magmatism and deformation were strongly controlled by NW- to WNW-striking fractures. These structures are spatially correlated with regional-scale Cenozoic lineaments that are oblique to the orientation of the Andean orogen. We suggest that these lineaments are features inherited at least from Jurassie times.

keywords: dike swarm, Magma emplacement, Magnetic fabrics, Transtension, Transpression, Jurassie, NW-SE structures.

RESUMEN. Los enjambres de diques máficos del Jurásico Medio-Superior de Chile central entre los 33° y 33°45'S registran la actividad tectónica del arco contemporáneo representado por el batolito costero. Estos enjambres de diques evidencian episodios alternados de transtension y transpresion a lo largo de estructuras de rumbo NW, las cuales controlaron la construcción del arco magmático. Los enjambres de diques máficos del Jurásico Medio-Superior y del Cretácico Inferior de la Cordillera de la Costa de Chile central han sido estudiados a través de observaciones de terreno, geocronología y Anisotropía de Susceptibilidad Magnética (ASM) para documentar la evolución tectónica y magmática del arco Jurásico-Cretácico en esta latitud. Los enjambres de diques del Jurásico Medio a Superior (enjambres de diques máficos de Concón y Cartagena) se emplazaron entre los 163 y 157 Ma, a lo largo de fracturas hospedantes de rumbo NW-SE a WNW-ESE, registrando una primera etapa de emplazamiento magmático bajo transtension sinistral. Durante esta etapa, los diques adquirieron una fábrica caracterizada por foliación magnética oblicua en forma antihoraria respecto al rumbo de los diques y lineación de bajo ángulo. Esta etapa fue seguida rápidamente por emplazamiento de diques bajo transpresion sinistral, a la que se asocia lineaciones de alto ángulo en estos diques, zonas de cizalle inverso en las rocas de caja y ocurrencia local de diques máficos horizontales. Por otra parte, el enjambre de diques máficos de El Tabo fue emplazado a lo largo de fracturas de tension que no registran desplazamientos a lo largo de sus paredes. Estos diques fueron emplazados en niveles corticales más superficiales gracias a fracturamiento extensional. Dentro de cada enjambre de diques, diferencias en el estilo tectónico de emplazamiento se correlaciona con cambios en la composición geoquímica de los diques, sugiriendo un fuerte acoplamiento entre la tectónica y la naturaleza de los magmas adicionados en el arco. Finalmente, estos resultados muestran que la evolución tectónica del batolito costero de Chile central ocurrió en varias etapas de deformación y no solo bajo un escenario simple de tectónica extensional. Este magmatismo y deformación fueron fuertemente controlados por fracturas de rumbo NW a WNW. Estas estructuras están espacialmente correlacionadas con lineamientos cenozoicos de escala regional, fuertemente oblicuos respecto a la orientación del orógeno andino. Nosotros sugerimos que estos lineamientos son características heredadas al menos desde el Jurásico.

Palabras clave: Enjambre de diques, Emplazamiento de magma, Fábricas magnéticas, Transtension , Transpresion , Jurásico, Estructuras NW-SE.

1.       Introduction

Subduction zones concentrate crustal deformation caused by convergence of subducting and overriding plates. In these settings, deformation is more concentrated in the magmatic arc zone, where fluid circulation, the highest heat flow and consequently thermal weakening of the crust occur. Therefore, the analysis of magma emplacement mechanisms in ancient magmatic arc zones is a key tool to understand the tectonic behavior of the overriding plate during plate convergence. The Mesozoic arc of the central Andes exposed along the Coastal Ranges of north and central Chile has proved to be an exceptional site to describe and understand upper-plate deformation that occurred during Mesozoic subduction along the western margin of Gondwana. This exceptional situation reflects excellent bedrock exposures and the eastward migration of the magmatic arc from Triassic to Cretaceous time which has left older arc rocks comparatively intact.

Magmatic dikes, have been extensively used as paleostress indicators, based on the assumption that these structures are oriented normal to the least principal stress (σ3) during emplacement (e.g. Anderson, 1951). This simple model does not apply, however, if there are pre-existing fractures that can open following the a3 directionbut are not oriented perpendicular to σ3. In these cases, dike orientation cannot be considered directly as paleostress indicators and a more careful analysis of emplacement mechanisms, mainly studying emplacement fabrics, is needed to understand how dikes are related to the stress state of the crust during magma intrusion (e.g., Delaney et al., 1986; Blumenfeld and Bouchez, 1988; Féménias et al., 2004; Clemente et al., 2007). The study of emplacement mechanisms of dike swarms has been proved as can be an efficient tectonic tool to understand the evolution of ancient magmatic areas (e.g. Glazner et al., 1999).

This contribution seeK3s to describe and interpret Jurassic and Cretaceous dike swarms and associated Jurassic mafic plutonic rocks , exposed on the coast-line of central Chile (33° and 33°45'S). To reach these goals, we combine field-based süuctural data, microstructural observations and AMS (anisotropy of magnetic susceptibility method) to get a detailed image of the internal fabric architecture of the dikes. This combination of methods is especially useful in the case that dike fabric is not always evident or measurable in the field, as in the studied dike swarms. These results are discussed in terms of identification of the emplacement mechanisms of dike swarms and recognition of the regional deformation history (e.g., transtension and transpression) during constraction of the Jurassic to Cretaceous Coastal Batholith of central Chile.

2.       Geological setting

Between the Late Permian and the Early Cretaceous, the Andean crust in north and central Chile was deformed as a retreating subductionboundary. characterized by mostly extensional and transtensional deformation (e.g., Gxocoiiet al, 1994; Scheuber and González, 1999; Grocott and Taylor, 2002; Cembrano et al., 2005). This deformation, mostly along the magmatic are and the Atacama Fault Zone, was contemporaneous withthe subsidence of Early Cretaceous basins in north and central Chile, in which large volumes of mantle-derived lavas accumulated (Vergara et al., 1995; Aguirre et al., 1999). Parada et al. (1999) proposed that progressive depletion in the Sr and Nd isotopic signature of magmas towards MORB from the Jurassic to the Cretaceous was caused by an increased amount of lithosphere removal and crustal thinning related to extension .

The Coastal Ranges between 33° and 33°45'S are mainly composed of Upper Paleozoic to Lower Cretaceous intrusive and volcanicrocks (Fig. 1a). In this segment, a well developed pattern of eastward-decreasing age is observed, from Lower Jurassic to Lower Cretaceous granitoid complexes and Mesozoic volcanic-sedimentary sequences (e.g., Levi, 1973; Vergara et al., 1995; Parada et al., 1999). One striking feature of this area is the presence of NW-SE to WNW-ESE regional lineaments that crosseut the Coastal Ranges oblique to the current continental margin. These lineaments are in some cases related to large magnetic anomalies (e.g., Yáñez et al., 1998) and to Upper Paleozoic and Upper Jurassic belts of intrusive rocks (Fig. 1b).

2.1.       Late Paleozoic-Triassic basement country rocks

The oldest units recognized in the area corres-pond to Upper Carboniferous granitoids (Hervé et al., 1988; Gana et al., 1996; Gana and Tosdal, 1996; Wall et al., 1996). These rocks range in composition from tonalite to granite (Siña, 1987; Arce, 2002). Granitoids crop out along the coastal line north of Valparaiso (33°S), between Quintay and El Tabo and at Santo Domingo (Fig. 1b). Seismic reflection data suggests that Upper Paleozoic granitoids continué to the west of the coastline of Valparaíso, forming an uplifted crustal competent block (Topocalma Knoll ; Yáñez et al., 2001). The age of the intrusions is constrained by U-Pb concordia ages and whole-rock Rb-Sr isochrons between 309 and 292 Ma (Godoy and Loske , 1988; Hervé et al., 1988; Gana and Tosdal, 1996). The granitoids show foliation and lineation in most outerops, defined by crystal and mafic enclave alignment. At a regional scale, the foliation in the granitoids vanes in orientation between NW-SE to E-W with variable dips to the south, whereas mineral lineation plunges to the south. In addition to granitoids, tonalitic to granitic gneisses are distributed between Las Cruces and Cartagena, and at Quintay (Fig. 1b). These rocks display variable attitude of foliation and mineral and stretching lineations mostly plunging to the south, with local oceurrence of high-strain ductile structures (shear zones and pencil lineations). The age of metamorphism is not totally clear. A dioritic gneiss from Cartagena yielded a zircon U-Pb age of 214±1 Ma (Gana and Tosdal, 1996), whereas at Quintay, the gneiss has ages of 290 Ma (zircon U-Pb concordia, Godoy and Loske , 1988). K-Ar age determinations inbiotite, amphibole and plagioclase from the gneiss in Cartagena mostly gave Middle-Late Jurassic ages between 167 and 145 Ma (Cordani et al., 1976; Hervé et al., 1988; Gana et al., 1996).

FIG. 1 a. Regional map showing the distribution of Late Paleozoic, Middle-Late Jurassic and Early Cretaceous batholithic belts. The segmented black line shows the approximate trend of the Jurassic batholith along the Coastal range. The solid square indicates the location of map of figure la; b. Geological map of the Coastal range of central Chile, between 33° and 33°45'S, modified from Gana et al. (1996), Wall et al. (1996) and SERNAGEOMIN (2002); c. Detail map of the Cartagena-San Antonio area, modified from Siña (1987), showing the location of AMS sampling sites.

2.2.       Jurassic-Early Cretaceous magmatic units

The volumetrically most important unit of the area corresponds to a NW-SE belt of Middle-Upper Jurassic granitoids that vary in composition between gabbro and granite (Gana et al., 1996; Wall et al., 1996). Some of these intrusive rocks show an intense ductile foliation, as observed in diorites from Laguna Verde area (Godoy and Loske , 1988). Precise titanite and zircon U-Pb radiometric dating define a pattern of decreasing ages to the east, from 163-160 Ma at Laguna Verde (Godoy andLoske , 1988) and 158+1 to 154+4 Ma eastern Limache and Sauce units, res-pectively, the two last located at 21 and 12 Km east of Laguna Verde (Gana and Tosdal, 1996). These ages are broadly similar to those obtained along the N-W belt exposed in the Coastal Ranges north of 33°S(Irwin et al., 1987; Parada et al., 1988).Lower-Upper Cretaceous granitoids occupy the eastern slope of the Coastal Ranges and vary in age between 118 and 91 Ma (Corvalán and Munizaga, 1972; Gana et al., 1996; Parada et al., 2005).

In addition to plutonic rocks , several mafic dike swarms have been recognized along the coastline between 33° and 33°45'S, mainly intruding the Upper Paleozoic basement. These are the Concón Mafic dike Swarm (CMDS), Cartagena Mafic dike Swarm (CrMDS) and El Tabo dike Swarm (ETDS), which are described in detail below (section 4).

Between 33° and 33°45'S, Lower to Middle Jurassic volcanic and marine sequences (Ajial and Cerro Calera formations) are poorly exposed (Thomas, 1958; Piracés, 1976). Late Jurassic to Early Cretaceous successions are dominant in this segment of the Coastal ranges. They are characterized by large volume of mafic volcanic rocks . Upper Jurassic sedimentary rocks intercalated with volcanic sequences mark a change to subaerial deposition in the Late Jurassic (Vergara et al., 1995).

3.       Analytical methods

Microprobe analysis of mafic silicates (amphibole, pyroxene and biotite) and plagioclase of selected dike samples were carried out at the Geology Department of the Universidad de Chile, using a CAMECA SU-30 SEM-probe, with WDS, using a beam current of 10.15 nA, 15.11 K3V of acceleration voltage and 5 to 20 µm beam size. Additional analyses were performed at ZELMI Laboratory, TU-Berlin, using a CAMEBAX microbeam electron microprobe. with PAP correction. Running conditions for these analyses were 13.1 nA beam current and 15.18 K3V acceleration voltage. Accuracy is estimated as approximately 1 % relative for major and 10% relative for minor elements.

40Ar/39Ar dating was carried out on hornblende separates from mafic dikes at the Geochronology Laboratory of Servicio Nacional de Geología y Minería (SERNAGEOMIN). Approximately one kilogram of sample was crushed and sieved to obtain grain sizes of 100 to 250 µm. Amphibole and biotite were separated using an isodynamic magnetic separator and heavy liquids, followed by hand picking under a binocular microscope. The samples were irradiated in the nuclear reactor of the Comision Chilena de Energía Nuclear (La Reina, Santiago de Chile). The irradiation factor for each sample was J=0.0010241±7.9x10-6 (sample CC-03-66) and J=0.0010502±8.1x10-6 (sample CC-03-27). Gas extraction was performed using a step heating procedure with a CO2 laser beam on hornblende grain populations (<15 grains). Detailed analytical procedures are given in Arancibia et al. (2006). The criteria used to define a plateau age are that it should contain more than 50% released 39Ar, that there should be at least three successive steps in the plateau, and that the integrated age of the plateau should agree with each apparent age of the plateau within 2σ.

Sampling for AMS was carried out using an oil-powered drill at 4 sites (34 samples) of the CrMDS and 2 sites (24 samples) of Laguna Verde diorites. Sampling in dikes was carried out especially along dike margins but also in central part of dikes, for a better characterization of internal fabric. Samples were oriented using solar and magnetic compasses. The anisotropy of magnetic susceptibility (AMS) of the samples was measured and thermomagnetic experiments were conducted at the Laboratorio de Paleomagnetismo, Departamento de Geología, Universidad de Chile, using KLY-3S Kappabridge equipment (AGICO Ltd.), working under a weak alternative magnetic field, with a resolution as high as 10-8 SI. IRM (isothermal remanent magnetization) experiments at the same laboratory were performed using an ASCIM-10-30 Impulse Magnetometer.

4.       Mesozoic dike swarms and Laguna Verde diorites

Mafic dike swarms, recognized along the coastline of central Chile (Muñoz-Cristi, 1964; Irwin et al., 1987; Creixell et al., 2006), will be described in terms of petrography and structures. In addition, the main structural and petrographic features of plutonic rocks located at Laguna Verde will be also described, because these intrusions are coeval and spatially associated with Jurassic dike swarms.

4.1.       Concón Mafic dike Swarm (CMDS)

This dike swarm is recognized along the coastal road between Concón and Viña del Mar and intruded into foliated Late Paleozoic granitoids. This dike swarm, described in detail by Creixell et al. (2006). consists of two generation of basaltic-andesitic dikes. an early group of thick dikes (mostly between 5 and 12 m thickness), intruded by thin dikes (0.5-3 m thickness). All of these dikes strike NW-SE (Figs. 2a and 2b). The thick dikes are characterized by the presence of pervasive ductile deformation at thin section scale (Fig. 3a and 3b), whereas thin dikes show amagmatic foliation. Two amphibole 40Ar/9Ar ages of 157 and 163 Ma on deformed (thick) and undeformed (thin) dikes, respectively, broadly indicate that emplacement of the dike swarm occurred in the Middle-late Jurassic (Creixell et al., 2006).

FIG. 2. Stereonet diagrams for orientation of mafic dikes of the a. CMDS (thick dikes). b. CMDS (thin dikes), c. CMDS country rocks (foliated granitoids), d. CrMDS e. CrMDS country rocks (gneiss and amphibolites), f. Laguna Verde diorites, g. ETDS, NW-striking dikes, h. ETDS, NE-striking dikes, and i. ETDS country rocks (foliated granitoids).

FIG. 3. a. Microphotograph of a CMDS dike , showing plagio-clase (pl) porphyroclasts surrounded by a deformed fine grained matrix composed by plagioclase, hornblende. biotite, quartz and magnetite armored by titanite; b. Detail of an elongated magnetite (mt) crystal armored by a titanite rim; c. Plagioclase (pl) and quartz (qz) por-phyroclasts in a mylonitic sinistral C/S fabric of a diorite from Laguna Verde.

4.2.       Cartagena Mafic dike Swarm (CrMDS)

This swarm consists of basaltic dikes that are 1.5 m thick and crop out between Santo Domingo and Cartagena (Fig. 1e). Some of the dikes locally reach 2 to 2.5 m thickness. The strike of the dikes varies between NW-SE and E-W with a mean orientation of 287°/80°N (Fig. 2d). NE-striking dikes were locally observed at Panul, but their crosseutting relations with the other dikes were not observed. The density of dikes is largely variable, reaching maximum densities of approximately 20 to 30% of the outcrop in local sections (profiles 300 to 500 m in length) in Cartagena beach. The country rocks include Upper Triassic dioritic gneiss, mylonitic gneiss and Upper Paleozoic granitoids with variable fabric orientation (Fig. 2e).

These dikes are composed of an equigranular to porphyritic arrangement of intergranular amphibole (Mg-hornblende to tschermakite), plagioclase (An30-62), biotite, low-Ti magnetite and accessory pyrrhotite, pyrite and apatite, with amphibole (mostly Mg-hornblende) and plagioclase (An59-82) phenocrysts. Pyrrhotite oceurs as inclusions in amphibole, in the same way as in late thin dikes of CMDS (Creixell et al., 2006). Phenocrysts mostly correspond to Mg-hornblende. Some strongly altered dikes of this swarm are characterized by a planar fabric, but extreme replacement of hornblende by chlorite prohibits to recognize the magmatic texture.

The age of the dike swarm is only constrained by a new hornblende 40Ar/39Ar plateau age of 157±3 Ma (Fig. 4a, 4b. Details of the analysis are given in table 1 of supplementary data). Late Jurassic K-Ar ages obtained by Gana et al. (1996) in Upper Triassic gneissic host rocks from Cartagena are interpreted to reflect extensive thermal resetting by the intrusion of the CrMDS.

FIG. 4. a. 40Ar/39Ar age spectra for sample CC-03-66 (CrMDS); b. Inverse isochron; c. 40Ar/39Ar age spectra for a mafic dike of the ETDS; d. Inverse isochron.

4.3.       Laguna Verde diorites

This unit consists of gabbroic to dioritic intru-sive rocks and some gneissic diorites, with minor felsic components (Hervé, 1976; Godoy andLoske , 1988). Deformation on this unit is largely variable in space, but diorites with intense ductile deformation (gneissic diorites) tend to coincide with location of most prominent NW-SE lineaments in the area. The age of relatively undeformed diorites (two-pyroxene diorite) is constrained by zircon U-Pb concordant agesbetween 163-160 Ma (Godoy and Loske , 1988). Zircons from gneissic diorites in this unit show similar concordant ages of 163 Ma (Godoy and Loske , 1988). According to these authors, slight dispersion in the ages is probably related to variable amount of Pb loss in the zircons. An 40Ar/39Ar age of 165±2.6 Ma in hornblende from diorites (Irwin et al., 1987) partially overlaps with these U-Pb ages. A younger Rb-Sr mineral errorchron age of 156.3±1.2 Ma (Godoy and Loske , 1988) show variable degree of isotopic disequilibrium and could be affected by post-crystallization alteration processes.

Laguna Verde diorites show coarse-grained texture. Deformed diorites are formed by sigmoidal plagioclase (An48-52) and amphibole (mostly Fe-Mg hornblende and minor Fe-edenite) porphyroclasts, in a matrix of stätically recrystallized hornblende, plagioclase (An25-36), quartz, titanite, magnetite and accessory allanite (armored by epidote). In some samples, S/C microstructures are well developed between matrix and porphyroclasts (Fig. 3c).

4.4.             Structures in Jurassic dikes and Laguna Verde diorites

The different types of planar structures (dike margins, foliations and shear zones) recognized in Jurassic dikes and diorites strike dominantly to the NW-SE. In the CMDS, thick and thin dikes show internal foliations that are clock wise oblique to dike margins. Passive markers with sinistral offsets at each side of the dikes are locally observed. In vertical sections, thin dikes show a trace of steep lineations and sigmoidal xenoliths indicating reverse shearing along dike walls. Some thin dikes are near horizontal. Variations from solid-state to magmatic microfabrics in thick dikes and magmatic fabrics in thin dikes suggest that the whole swarm can be consideredas syntectonic (Creixell et al., 2006). In CrMDS at Cartagena, a set of the near-vertical dikes resemble the thin dikes of CMDS and are ductilely deformed where are cut by nearly coeval E-W reverse faults (Figs. 5a, b). Horizontal dikes of the CrMDS are observed in the Santo Domingo area (Figs. 5c, d). In most cases, we can note that the orientations of the mafic dikes differ from the orientation of the host rock fabric (Figs. 2a to 2e).

FIG. 5. Field features of CrMDS and Laguna Verde diorites, with schematic representation of the outcrops at the right side of the photograph (b, d); a. Mafic dikes of the CrMDS displaced and ductilely sheared by reverse faults. Away from the dike , the faults evidence frague deformation. View to the east, c. Near-horizontal CrMDS dike intruding Late Paleozoic granitoids at Santo Domingo beach, view to the south.

Structures of Laguna Verde diorites were mainly studied at two localities, especially where the NW-SE shear zones terminate westwards at the surface. In the northern locality studied, near-vertical sinistral shear foliation is spatially associated with meter-scale sub-vertical folds and ductile reverse shear zones. Shear foliation is oriented 110°-160765o-90° SW and stretching lineations plunge to the south (46o-77°, Fig. 2f). The microfabrics in these deformed diorites show sinistral C/S fabrics, with evidence of high-temperature ductile deformation on 8-type porphyroclasts (sigmoidal shape in plagioclase and amphibole) and foliated and recrystallized matrix.

4.5.             El Tabo Mafic dike Swarm (ETDS)

This swarm consists of two systems of dikes of basaltic composition that mainly occur between Algarrobo and El Tabo. Such dikes are sparse at Cartagena and Las Cruces. The dikes intrude foliated Late Paleozoic granitoids. One system of intrusions comprises porphyritic to aphanitic NW-striking dikes, with a mean thickness of 0.6 m and mean orientation of 137789°W (Fig. 2g), usually occurring as a group of múltiple parallel intrusions. Its texture comprises subparallel plagioclase phenocrysts (An53-74) and amphibole prisms (mostly tschermakite and minor proportion of Mg-hastingsite) and clinopyroxene (Wo28En48-50Fs20-23) phenocrysts, withabundantbrown hornblende prisms in the groundmass, accompanied by accessory titanite, magnetite and locally chromite. The other system comprises NE-striking dikes (main orientation: 65779°N, Fig. 2h) of variable thickness between 0.5 and 4 m (mean thickness of 2.6 m). The rocks are porphyritic and contain plagioclase phenocrysts in a medium-grained groundmass of clinopyroxene ( Wo40-42En29-31Fs26-29) and plagioclase (An52-53) accompanied by ilmenite, apatite and minor biotite. A relevant field observation is that both dike systems show mutual crosscutting relations between them.

The age of the dike swarm is poorly K3nown. An imprecise new hornblende 40Ar/39Ar age from a NW-SE dike yields a plateau age of 175+4 Ma involving 54.2% of 39Ar released (Fig. 4c, details of the analyses are given in table 1 of supplementary data), but incremental release pattern show a typical 'U-shaped' shape, with relatively high apparent ages in the first two incremental heating steps, a relatively fíat pattern in the C, D and E steps and finally again higher apparent ages in steps F to G. This kind of degasification pattern is indicative of Ar excess in the sample. According to this, the lower apparent ages contained in steps D and E (140.1 and 141.0 Ma) could represent the maximum ages for the sample. These two steps are characterized by lower Ca/K ratios with respect to high temperature steps, pointing to important heterogeneities in the sample and possible degasification of calcic phases at high temperature (plagioclase inclusions). The influence of Ar excess in the analyses is favored by the very low K20 of the analyzed amphiboles (between 0.098 and 0.223 wt%). This possible Early Cretaceous age is similar to K-Ar and 40Ar/39Ar ages between 144.4 and 151 Ma determined in dike swarms north of the study area near 32°30'S (Irwin et al., 1987); and also in Lower Cretaceous bimodal dike suites (138+1 Ma) south of the study area (Willner et al., 2005).

4.6.       Structures in the Cretaceous ETDS

Unlike the Jurassic intrusions, the ETDS dikes do not show evidences of ductile deformation. Some outcrops contain dike -parallel joints in country rocks close to the dikes (Figs. 6a a, b). Some chlorite-epidote veins cross-cut by NW-striking dikes indicate dike opening normal to the walls (Figs. 6c, d, e, f). NW-striking dikes form sets of múltiple sub-parallel intrusions. At Punta de Tralca, dikes are more abundant and more closely spaced. The spacing between dikes in this locality is very low (0 to 0.3 m) and the abundance of dikes locally reach about 20% of the outcrop area. To the north and south, the abundance of dikes diminishes drastically (<2% of the outcrop at El Tabo) and spacing between dikes increase in the order of 2 to 10 m.

FIG. 6. Field features of the ETDS, with schematic representation of the outcrops at the right side of the photograph (Figs. b, d, f) a. NE-striking dike of the ETDS with associated dike -parallel joints in the granitoid country rocks , El Quisco beach, view to the NE, hammer for scale; c. NW-striking mafic dike of ETDS cut chlorite-epidote vein (chl-ep). This vein is displaced normal to dike walls. Punta de Tralca beach, horizontal section, pen for scale; e. near-vertical, zonated NW-striking mafic dike intruding chlorite-epidote vein, displaced normal to dike walls in vertical section. This section is cut and normally displaced by another, gently-dipping, NW-striking dike . Punta de Tralca beach, magnetic compass for scale.

Trie orientations of both NW- and NE-striking dike sets are homogeneous and do not show similarities with orientation of the country rock foliation mea-sured in El Tabo, Punta de Tralca and Las Cruces (Fig. 2g to 2i).

5.       AMS fabrics of dike swarms and Laguna Verde diorites

The AMS (anisotropy of magnetic susceptibility) represents the directional variability of the magnetic susceptibility of a sample (e.g., Tarling andHrouda, 1993). Thisisrepresentedby asecond-order tensor with a magnetic ellipsoid defined by three eigenvectors (K1>K2>K3), where K1 represents the magnetic lineation and K3 represents the pole of the magnetic foliation plane (K1-K2 plane). The mean magnetic susceptibility K3 corresponds to the arithmetic mean of the magnitude of three vectors (K3 = [K1+K2+K3]/3). The degree of anisotropy of the magnetic ellipsoid (%P') corresponds to the P. defined by Jelinek (1981). The shape parameter T for the magnetic ellipsoid indicates oblate shapes when 0≤T≤1 and prolate shapes when -1≤T≤0.

In most igneous rocks , the magnetic susceptibility is related to the presence of ferromagnetic minerals and to a lesser degree to the presence of paramagnetic phases. The source of the AMS could come from 'crystalline anisotropy' (variations in magnetiza-tion controlled by the distribution of cations in the crystal structure), 'distributionanisotropy', derived from magnetic interaction among magnetic grains (when they tend to f orm clusters of grains) and shape anisotropy, defined by the variation of susceptibility in nonequidimensional grains, where K1 tends to be parallel to the long axis of the particle. In the last case the AMS ellipsoid tends to show a good corres-pondence with the shape fabric ellipsoid, because the individual ferromagnetic grains (e.g., magnetite) tend to be late phases in the cry stallization sequence of igneous rocks and occupy the space betweenthe rock -forming minerals.

5.1.       Magnetic properties and AMS ellipsoids

The magnetic properties and AMS directions of the CMDS and ETDS were described in detail by Creixell et al. (2006, 2009, respectively). Details of the new analyses are given in table 2 of supplementary data.

Examination of selected samples of CrMDS under SEM (scanning electron microscopy) and EMPA (electron microprobe analyses) allows us to detect the presence of low-Ti magnetite as independent crystals in the oriented groundmass of dikes and small inclusions of pyrrhotite in primary hornblende, in a similar way as observed in thin dikes of CMDS. The presence of magnetite is confirmed by IRM expenments in which magnetic saturation was reached at approximately 250 mT (Fig. 7a). The presence of low-Ti magnetite is also suggested by demagnetization expenments and Curie temperatures near 570°C (Fig. 7b). In these experiments, demagnetization close to 320°C in some samples of CrMDS indicate the presence of monoclinic or mixed monoclinic-hexagonal pynhotite (e.g., Martín-Hernández et al., 2008) which agrees with petrographic observations.

FIG.7. a. IRM curves for CrMDS samples; b. Demagnetization experiments in CrMDS samples, showing two marked demagnetization temperatures near 320°C and 570°C, suggesting the presence of pyrrhotite and low-Ti magnetite in the samples; c. Bulk magnetic susceptibility (Km) versus magnetic anisotropy degree (%P') in samples from CrMDS. Samples from ETDS and CMDS are shown for comparison; d. Shape parameter (T) versus Bulk magnetic susceptibility in samples from CrMDS; e. Shape parameter (T) versus magnetic anisotropy degree (%P') in samples from CrMDS. Samples from ETDS and CMDS are shown for comparison; f. Detail from e. for samples of CrMDS from Punta Suspiro locality (sites ET05 and ET06), showing the correlation between T and %P' in these samples (grey arrow).

Samples of the four sites of CrMDS show weak fenomagnetic behavior, with K3 between 824 and 394x10-6 [SI] (Fig. 7c). CrMDS dikes have low but variable %P' (0.7-3.5%) at relatively constant Km values, suggesting that intensity of magnetic fabric is not controlled by composition, e.g. magnetite content (Fig. 7c). %P' tends to be higher in sites ET05 and ET06 from Punta Suspiro. This is well conelated with field observations of incipient internal shape foliation in these dikes, which was not clearly observed in sites at Panul. The shape parameter T varies independently of Km values in dikes in the Panul area. In both sites at Punta Suspiro, most ellipsoids are oblate, with variations not conelated with variations in Km (Fig. 7d). This also suggests, as for the anisotropy degree, that the shape of the magnetic ellipsoids (T) is not controlled by magnetic susceptibility (e.g., magnetite or pynhotite content). Indeed, the shape parameter T tends to be conelated with anisotropy degree %P', especially in sites ET05 and ET06 of Punta Suspiro, where %P' is higher (Fig. 7e, f).

Significant differences were found between the AMS ellipsoids of ETDS and CMDS samples. Km and %P' are strongly conelated in thick CMDS dikes (Fig. 7c). In these dikes, higher %P' tends to correspond to triaxial to prolate ellipsoids (Fig. 7e). These relations indicate that higher susceptibility rocks are also more anisotropic. The magnetic ellipsoids of thin dikes of CMDS tend to be similar to those of the CrMDS, because we can observe a tendency to positive correlation between %P' and T (Fig. 7e) and variations of %P' independently of Km values (Fig. 7c). Magnetic properties of ETDS are distinguishable from CMDS and CrMDS. ETDS samples are characterized by low Km between 544 to 841 x 10-6 [SI] in NW-striking dikes and 651 to 901x10-6 [SI] in NE-striking dikes, whereas most AMS ellipsoids are dominantly óblate with low low %P'(close to 1%). The weak ferrimagnetic behavior of these dikes has not been studied in terms of contributions of magnetite and paramagnetic minerals in the source of magnetic susceptibility.

5.1.1.      Directional data

In sites ET05 and ET06 from Punta Suspiro, the magnetic foliation is near parallel to the dike walls and magnetic lineation plunges steeply to the NE (Fig. 8). The fact that these dikes are cutby reverse shear zones will be discussed below in terms of the origin of these fabrics. In site CT01 from Panul, magnetic lineation gently plunges to the SW, whereas the magnetic foliation poles are well-clustered, with foliation planes (K1-K2 planes) striking NNW-SSE, clock wise oblique to the dike trend (Fig. 8), in a pattern similar to that observed in the magnetic and shape fabrics of the CMDS (Creixell et al., 2006). In site CT02, the AMS ellipsoids, which vary between weakly prolate and weakly óblate, show well clustered magnetic axes K1, K2 and K3.

The magnetic lineation plunges to the SW and the magnetic foliation planes trend NE-SW, being both perpendicular to the dike trend (dike orientation: 313783°SW, Fig. 8). Apossible explanation is an interchange of the position of magnetic axes, caused by the presence of inverse AMS fabrics that are a relatively common feature of low Km mafic rocks , in which single-domain magnetite is the dominant magnetic phase (e.g., Ferré, 2002). This hypothesis is supportedbecause magnetite occurs as fine-grained crystals (5 to 80 µm) in samples of this site.

FIG. 8. AMS stereoplots (lower hemisphere projection) of magnetic ellipsoids of mafic dikes of CrMDS (CT01, CT02, ET05 and ET06) and ETDS (ET01, CT03, CT04 and CT05), including 95% confidence cone for each mean magnetic axis (K1>K2>K3). Solid lines represent dike orientation.

Unlike CMDS and CrMDS dikes, ETDS dikes do not have oblique asymmetrical AMS fabrics. In most cases, magnetic lineation and magnetic foliation planes tend to be parallel to the dike walls and are interpreted to reflect magma flow, where flow vectors are near vertical (upward) inthe central part of the dike swarm (at Punta del Tralca) and SE- and NW-directed at El Tabo and north of Punta del Tralca, respectively, away from the central part of the swarm (Creixell et al., 2009).

5.2.      Magnetic properties and AMS ellipsoids of Laguna Verde diorites

In both sites from Laguna Verde (LV01 and LV02), demagnetization temperatures near 560°C and IRM experiments with saturation of magnetic residual near 180 mT suggest that magnetite is the main ferromagnetic phase that controls the AMS signal of the samples (Fig. 7b). Site LV01 of Laguna Verde (Playa Chica) shows weak ferromagnetic behavior (619 to 1374x10-6 [SI]), in contrast with high Km values of site LV02 (4490 to 81960x10-6 [SI], Fig. 9a). In site LV01 there is no clear correlation between Km and %P' (Fig. 9a) but this correlation is more clear in site LV02, where %P' is higher (>15%, with a mean of 46%). In site LVO1 most AMS ellipsoids are óblate. InLV02 prolate ellipsoids are dominant, and shape parameter tend to be well correlated with %P' (Fig. 9b).

FIG. 9. a. Bulk magnetic susceptibility (Km) versus magnetic anisotropy degree (%P') in samples from Laguna Verde diorites, b. Shape parameter (T) versus magnetic anisotropy degree (%P') inthe same samples, showing good correlation between these parameters in site LV02.

The AMS orientation differs between the sites. LV01 show well-clustered AMS axes, with WNW-striking magnetic foliation planes (mean of 305787°N) and steeply SE-plunging like magnetic lineation (Fig. 10). In site LV02, the dominant prolate ellipsoids have magnetic lineation plunging to the SW. Magnetic foliation planes strike NNW-SSE, with a mean of 170748°W. In general terms, the AMS directional and shape (T) data are well correlated with structures measured in the field (foliation and lineation, Fig. 2f).

FIG. 10. AMS stereoplots (lower hemisphere projection) of magnetic ellipsoids of Laguna Verde diorites (LVOl and LV02), including 95% confidence cone for each mean magnetic axis (K1>K2>K3).

6.      Geothermobarometry

Composition of minerals used for geothermo-barometry is given in table 3 (supplementary data). For Laguna Verde diorites, temperatures estimated using the hornblende-plagioclase geothermometer of Holland and Blundy (1994) give results between 640° and 694°C, consistent with ductile deformation observed in these rocks. Semi quantitative geother-mobarometry formulated for mafic rocks, based on TiO2 and A1203 contents of amphibole (Ernst and Liu, 1998) can be applied in these rocks, because the mafic/intermediate whole-rock composition and the presence of quartz and a Ti-saturated phase (titanite). The Ernst and Liu (1998) geothermobarometry method gives temperatures between 700° and 770°C and pressures between 4.8 and 7.6 kbar for amphibole rims. The same method applied to amphibole cores gives temperatures between 730° and 795°C and pressures between 3.5 and 4.8 kbar. As evident from these calculations, pressure results are largely variable in these rocks, and therefore are considered as poorly constrained. Previous results in Jurassic granitoids vary widely between 3.5 and 6.5 kbar (Araneda, 1999). Gana and Tosdal (1996) reported hornblende crystallization pressures between 4.1 and 5.4 kbar for Middle Jurassic granitoids, located directly to the east of Laguna Verde diorites. The same authors reported lower pressures, between 2.8 and 3.6 kbar, for Upper Jurassic units located to the east. These eastern units are younger than Laguna Verde and Sauce units (Gana and Tosdal, 1996).

Crystallization temperatures in mafic dikes were calculated using compositions of hornblende-plagioclase pairs, with the calibration of Holland and Blundy (1994). Groundmass tschermakitic amphibole from the CrMDS dikes (Fig. 11 a), yields temperature estimates between 768° and 819°C, probably corresponding to solidus temperatures, whereas probable solidus pressures (for the same amphiboles), estimated using semiquantitätive geobarometer of Ernst and Liu (1998) varies between 3.1 and 5.5 kbar, reflecting the important variability in Si and Al content of these amphiboles (Figs. 11a and 11b).

FIG. 11. a. Amphibole classification diagram (Leake et al., 1997) based on Mg/(Mg+Fe2+) ver sus Si content (atoms per formula unit). for amphiboles with atomic content CaB>1.5 and (Na+K)A<0.5; b. Variation diagram of Ti versus A1IV (atoms per formula unit) in amphiboles from dikes and Laguna Verde diorites.

In CMDS, amphibole composition from thick dikes varies largely. In spite that some retrograde actinolitic amphibole has been detected, most of them correspond to Mg-hornblende (Fig. 11a). Amphibole from thin dikes tends to be slightly enriched in Ti and Mg than those from thick dikes (Figs. 11a, b).

In thin dikes of the CMDS, crystallization temperatures for hornblende vary between 683° and 715°C. In thick dikes of CMDS, crystallization temperatures for hornblende-plagioclase rim compositions vary between 620° and 690°C. Temperatures for core compositions of hornblende-plagioclase pairs are consistently higher, varying between 724°-771°C, representing magmatic equilibrium temperatures. Triese amphibole cores have a slight tendency to show higher Ti contents than amphibole rims (Fig. 11b). Pressure estimates using Ernst and Liu (1998) geobarometer, are indistinguishable between rims and core compositions of amphiboles and vary between 2 and 4.7 kbar.

Brown amphiboles from NW-striking dikes of the ETDS are characterized by the highest Mg/(Mg+Fe2+) ratios and Ti contents (Figs. 11a and 11b), and consistently with it, the magmatic temperatures estimated are also high, between 790° and 910°C, using the geothermometer of Otten (1984). Estimations with the geothermobarometer of Ernst and Liu (1998) yield temperatures around 850°C and pressure of crystallization between 2.8 and 3 kbar.

7.      Discussion

7.1.      Significance of shape and AMS fabrics of dike swarms: insights into emplacement mechanisms

Microscopic examination of selected samples of dikes allows recognizing magnetite as isolated (locally elongated) grains from each other in the groundmass of these rocks. This suggests, in conjunction with Km values of the samples, that AMS is controlledby shape anisotropy of magnetite. Where field structures are well observed, e.g., in Laguna Verde diorites and CMDS, a correlation between AMS and shape fabrics is clearly documented, and then AMS fabrics are a good proxy of the orientation of the finite strain ellipsoid of the rocks.

7.1.1.      Emplacement under transtension in CMDS and CrMDS

Thick dikes of the CMDS show abundant evi-dences of ductile deformation of crystals at microscopic scale, however, some dikes also show a well developed magmatic microfabric, not affected by solid-state recrystallization. Evidences for ductile deformation presented by Creixell et al. (2006) and in this work, mostly show that the dike matrix is affected by important dynamic recrystallization including grain-size reduction (Figs. 3a, b). Beside this, internal fractures of plagioclase phenocrysts are filled by magmatic minerals (mostly hornblende and oligoclase), suggesting the presence of fluid during fracturing and deformation (e.g., Bouchez et al., 1992). The coexistence in equilibrium of high-temperature ductile deformation and fractures filled by a possible melt suggests that the microfabrics register the strain occurred from the submagmatic state to high-temperature solid state deformation. We consider submagmatic deformation as the ductile strain occurred in the presence of proportion of residual melt below the necessary to allow magmatic flow (Paterson et al., 1989). These observations are in agreement with temperature estimates between 620° and 690°C that are close to slightly below solidus for intermediate compositions (Piwinskii, 1968; Huang and Wyllie, 1986; Schmidt, 1993).

Inside this deformed matrix of the thick dikes of CMDS, magnetite occurs as isolated grains su-rroundedby titanite rims (Fig. 3b). The magnetite grains are oriented and elongated following the deformation of the groundmass. These textural arrangements imply that: a. AMS fabrics, developed by the presence of magnetite, are controlledby the shape anisotropy of this mineral ratherthan distribution anisotropy. This is consistent with the good correspondence between AMS and shape fabrics of dikes (Creixell et al., 2006); b. the AMS fabrics, and then the asymmetrical pattern they represent, are representätive of the shape fabric of the dikes, specifically the fabric of the deformed matrix. Because the matrix was deformed in the submagmatic state (ductile deformation in the presence of small amount of melt), the asymmetrical fabric was acquired mainly in the late stage of crystallization of the dikes, probably close to emplacement. In the case of CrMDS dikes from Panul, that exhibit magmatic textores and temperature estimations >700°C, acquisition of asymmetrical fabric occurred during magmatic crystallization.

Thick dikes of CMDS and dikes of CrMDS from Panul area (Fig. 1e) have asymmetrical magnetic fabrics, with near-vertical foliations clockwise oblique to dike walls, and shallow plunging magnetic lineations. At dike margins, the magnetic foliation in most cases is parallel to dike walls. Following the models of Blumenfeld and Bouchez (1988). Hutton (1992) and Correa-Gomes et al. (2001), this pattern of fabric reflects the effeets of sinistral deformation along dike walls during emplacement and also indicates that the influence of magma flow dynamics was minor on fabric development.

To understand the meaning of the low-plunging lineations in the studied dikes, these magmatic bodies need to be considered as dike-shear zones, taking into account that sinistral deformation was fundamental in fabric development and took place during or close to it emplacement (e.g., dikes were emplaced along active sinistral fractures). Theoretical models of lineation development in shear zones (Tikoff and Greene, 1997; Teyssier and Tikoff, 1999) predict that near-horizontal lineations with vertical foliations are produced during both transtension and transpression, depending on the magnitudes of pure and simple shear and the orientation of the shear zone with respect to the external deformation field. Specifically, fabrics characterized by vertical foliations and horizontal lineations can be originated by deformation dominated by simple over pure shear, as suggested in the previous paragraphs, or by deformation that registered a low cumulative strain (Teyssier and Tikoff, 1999). We have not enough data to discrimínate more exactly between these mechanisms. In spite of this, for the thick dikes of the CMDS and the CrMDS, the sinistral deformation fabric was developed during or close to emplacement implying that the left-lateral movement was coetaneous with a component of horizontal dilation along the host fractures, needed to accommodate the dike thick-nesses, that cumulatively represents around 3.5 km of extension (Creixell, 2007). This occurrence of coetaneous sinistral displacement and horizontal dilation across the host fractures indicates that the dikes were emplaced during sinistral transtension . Finally, if the magnetic lineations are representa-tive of stretching during fabric acquisition, they indicate oblique opening in NNW-SSE direction (Fig. 12a), consistent with some field evidence of oblique opening of dikes (section 4.4).

FIG. 12. a. Schematic cartoons of dike emplacement forthick dikes of CMDS and CrMDS, and b. Thin dikes of CMDS and horizontal dikes of CMDS and CrMDS.

7.1.2.      Emplacement under transpression in CMDS, CrMDS and Laguna Verde diorites

Thin dikes of CMDS are characterized by magmatic fabrics, without evidence of solid state deformation. Dikes of the CrMDS from Punta Suspiro show local evidence of high-temperature solid-state fabrics that will be explained in detail below. In the same way as observed in thick dikes of the CMDS, in all these dikes magnetite occurs as isolated grains in the ground-mass, in intergrowth relation with silicate minerals, suggesting that the AMS ellipsoid is controlled by the orientation of these magnetite grains and could be representätive of the rock fabric.

The AMS fabrics of thin dikes of the CMDS are asymmetrical, with magnetic foliation clockwise oblique to dike trend, with a pattern indicative of sinistral shear (e.g., Blumenfeld and Bouchez, 1988; Hutton, 1992; Correa-Gomes et al., 2001), but steeply-plunging lineations are dominant. Dikes from Punta Suspiro are characterized by steeply dipping magnetic foliation and also steeply-plunging magnetic lineations. High plunge of magnetic lineations in shear zones are developed under transpression (Tikoff and Greene, 1997; Teyssier and Tikoff, 1999). If we consider these dikes as emplaced along active shear fractures, as evidenced by AMS fabrics, an important component of horizontal shortening was associated to their emplacement. Indeed, this horizontal shortening is evidenced by a. field indicators of reverse shearing along dike walls in vertical sections (Creixell et al., 2006) and b. occurrence of subhorizontal thin dikes of the CMDS and CrMDS (Fig. 5c, d). These horizontal dikes are interpreted as a product of near vertical dilation and therefore a component of shortening in the horizontal plane (Fig. 12b). Horizontal shortening is also deduced from near-vertical mafic dikes of the CrMDS from Punta Suspiro that are displaced by E-W striking reverse shear zones (Fig. 5a). These reverse shear zones mostly show fragüe deformation, but these dikes are deformed in highly ductile conditions where they are cut by these faults, suggesting that reverse activity of these faults occurred shortly after dike emplacement.

In the coeval Laguna Verde diorites, we have not enough detailed data to reconstiuct the history of emplacement and deformation of these rocks, but the registered ductile structures are characterized by NW-SE sinistral shear zones with near-vertical foliation and steeply-plunging lineations (site LVO1 and Fig. 2f) and coeval folds with horizontal axes and reverse shear zones. The microfabrics and geo-thermometry suggest that deformation occurred at high temperature below solidus.

Finally, the combination of sinistral shear along NW-SE striking structures occupied by dikes and diorites, with a coeval component of horizontal shortening, indicate that emplacement and deformation of thin dikes of the CMDS, CrMDS dikes from Punta Suspiro and Laguna Verde diorites occurred in a regime of sinistral transpression.

7.1.3.      Fabrics and emplacement of ETDS

Two perpendicular sets of dikes were recognized in the ETDS. Dike-parallel joints and chlorite-epidote veins cut by dikes are evidence of emplacement at shallow depth. Since these structures are not wides-pread at regional scale, they probably were directly associated to dike emplacement. The presence of dike-parallel joints in dikes has been described as evidence of dike propagation as self-generated fractures, where these joints were causedby tensile stress produced near and away from propagating dike tip (Delaney et al., 1986). This implies that the dikes were emplaced along tensional fractures, perpendicular to the least principal stress direction (a3). Consistently with this hypothesis, we can observe that the homogeneous orientation of each dike set in the ETDS does not follow the variation in fabric orientation of the country rock (Figs. 2g to 2i), and therefore, emplacement of such dikes was not controlled by the country rock fabrics, a least at the exposed crustal level. Also, passive markers observed mostly at Punta de Tralca suggest that opening occurred normal to dike walls (Figs. 6c to 6f), as expected for tensional fracturing or tension gashes (e.g., Anderson, 1951; Emerman and Marrett, 1990).

Taking these observations into account, the presence of two nearly coeval and perpendicular dike systems in the ETDS indicates two directions of crustal dilation. Horizontal radial extension cannot account as a mechanism that explains the emplacement of ETDS, simply because radial extension (with vertical maximum stress axis σ1) produces radial sets of dikes or fractures. A more possible tensional regime is that each dike generation was associated to changes in the stress pattern, with interchange of σ2 and σ3 during emplacement of each dike generation (with σ2a ~σ 3 lying in the horizontal plane, Fig. 13). Apossible explanation for this model is that the pressure imposed by magma intrusion allows inversion of horizontal stress axes at the local scale. This is possible if differential stress in the horizontal plane is sufficient small to be modified by the intrusion of dikes. This mechanism could be efficient for this kind of minor intrusions, such as the ETDS, at shallow crustal levels. A similar mechanism was proposed by Vigneresse et al. (1999) to explain inversion of vertical and horizontal stress axes in a tensional regime associated with magma intrusion . The area of higher dike density and lower dike spacing in NW-striking dikes coincides with vertical magma flow vectors determined from the AMS (Creixell et al., 2009), and probably corresponds to the central portion of the swarm. Away from it, magma flow vectors become gently-plunging and dike density decreases (Fig. 13).

FIG. 13. Schematic cartoon of dike emplacement for ETDS. Magma flow directions (white arrows) as determined by AMS fabrics by Creixell et al. (2009). Opening direction of dikes determined by field data. Mínimum principal stress direction (ol) is near vertical.

7.2.       Geodynamic and tectonic setting of emplacement of dike swarms

7.2.7.       CMDS and CrMDS: Middle-Late Jurassic changefrom transtension to transpressional deformation and associated compositional variations of magmas

From the data and discussion presented in the previous sections, we envisage two distinct regimes of magma emplacement that were active during Middle-Late Jurassic times in the area. Afirst regime of sinistral transtension across NW-SE to WNW-ESE

structures was followed by sinistral transpression along similar fracture systems. Abundant field data supports this sequence of deformation in the area:

  a.  In CMDS, thick dikes, emplaced under transtension, are systematically intruded by thin dikes, emplaced in transpression.
  b. In CrMDS, reverse faults postdate dike emplacement.
  c. Horizontal dikes are everywhere associated with dikes emplaced in transpression.

This temporal sequence of deformation implies that host fractures of dikes quickly change their tectonic behavior between 163 and 157 Ma. This change is correlated with important compositional variations observed in the dike swarms. Dikes emplaced during transtension (e.g., thick dikes of CMDS) have an enriched geochemical signarme (high Ti, Nb, Zr and other incompatible elements) with respect to dikes emplaced during transpression, that show a more primitive signature, with higher MgO, Cr and Ni (Creixell et al., 2009). These changes are also accompanied by variations in magnetic mineralogy, where the first group of dikes is dominated by the presence of low-Ti magnetite and dikes emplaced in transpression contain magnetite and sulphide phases, such as pyrrhotite and pyrite. This implies that the changing tectonic behavior of structures promoted magma extraction from different reservoirs, where more primitive magmas ascend through dikes during transpressive deformation, probably associated to higher magma overpressures.

7.2.2.       Emplacement and compositional variations in ETDS

The field and AMS data on the ETDS indicate that both NE and NW-striking dike sets were emplaced along self-generated tensile fractures. As discussed above, the emplacement of these dike sets occurred in successive stages of modification of the stress field. As in the Jurassic dike swarms, structural variations in different dike sets are correlated with compositional changes. NE-striking dikes are Ti-enriched, whereas NW-striking dikes are comparatively poorer in Ti and other elements such as Nb, Zr and REE (Creixell et al., 2009). Another difference is that NE-striking dikes are systematically thicker than NW-striking dikes (section 4. and Fig. 13). According to recent results in mafic dike swarms in Greenland (Klausen and Larsen, 2002) and in the Deccan Traps (Ray et al., 2007), differences indike thickness can be controlled by the depth of magma reservoirs, but also by differences in magma viscosity (Wada, 1994). where deeper reservoirs or also more viscous magmas can produce thicker dikes. Since major elements geochemistry and therefore magma viscosity is not dramatically different between NE and NW-striking dikes, we suggest that differences in dike thickness are controlled by injection of magmas from reservoirs located at different depths.

7.3.       Regional implications

7.3.1.       Changes in the axis of the CoastalBatholith

The current results give preliminary insights into the tectonic evolution of the Mesozoic magmatic arc of central Chile. The structures observed inthe dike swarms and diorites show that the evolution of this western part of the batholith took place in several stages.

At a regional scale from north to south between 33° and 34°S, the axis of the Middle-Upper Jurassic coastal batholith changes from ca. N-S to NW-SE, coincident with the close occurrence of NW-SE structures crossingthe Coastal Cordillera (Fig. 1b). The current results suggest that magma ascent in the batholith, marked by the presence of the dike swarms, have been controlled by NW-SE structures, at least during the first stages of growth of the batholith (163-157 Ma). As a preliminary hypothesis, we propose that these structures controlled and focused the emplacement of Middle-Upper Jurassic plutons in the area, to the east of the dike swarms and caused the change in the axis of the batholith to a NW-SE orientation. In contrast, this change in the orientation of the plutonic belt is not observed inLower Cretaceous plutons, that are distributed continuously along a N-S belt in the eastern slope of the Coastal Range of central Chile (SERNAGEOMIN, 2002). Detailed fabric studies in one of these plutons (Caleu pluton) do not detect the influence of oblique (NW-striking) structures in its emplacement (Parada et al., 2002). This is a preliminary suggestion that the NW-SE structures of the area were more active during the Middle-Late Jurassic.

7.3.2.       Implications for the evolution of NW- to WNW-trending lineaments of central Chile

Several authors note the presence of important NW-SE to WNW-ESE structures oblique to the Andean orogen (e.g., Glodny et al., 2008), that are distributed along most of the central and southern Andes, but have an outstanding density in the 33o-34°S segment, coincident with the transition between the 'flat-slab' segment to the north and the southern volcanic zone to the south (e.g., Yáñez etal., 2001, among others). These structures control the evolution of volcano-tectonic basins during the Cenozoic as transtensional and probably normal faults (Wall et al., 1996; Rivera and Cembrano, 2000). Our current results, combined with observations made by Godoy and Loske (1988) indicate that these large Cenozoic structures are inherited from structures that are at least as old as Middle Jurassic that hosted and de-formed the mafic dike swarms and diorites studied here. Indeed, the western end of most of the main NW to WNW-striking lineaments between 33° and 33°45'S coincides with the localization of the dike swarms studied here or with the contact between Jurassic and Late Paleozoic intrusions.

8.       Concluding remarks

Field data and AMS fabrics indicate that the CMDS and CrMDS were emplaced in two stages, a first sinistral-transtension, followed by sinistral transpression. The transpressive structures are also observed in the Middle-Upper Jurassic Laguna Verde diorites which show evidence of ductile deformation close to its emplacement. The changes in deformation kinematics were associated with compositional changes inthe mafic dikes, with the more primitive magmas emplaced during the transpressive stage. This suggests extraction of magmas from different reservoirs during each deformation event.

The Lower Cretaceous mafic dikes (ETDS) were emplaced along tensional structures, with different dike orientations (NW- and NE-striking mafic dikes) associated to different composition and thicknesses of dikes, pointing again to extraction of magmas from different reservoirs, related to low and high-Ti basaltic magmas.

Finally, a general framework for the tectonic evolution of the Jurassic magmatic arc of central Chile has been envisaged here, with different styles of deformation in several stages. The current results suggest that occurrence of NW- to WNW-trending lineaments played a fundamental role in the emplacement and deformation of Middle-Upper Jurassic dike swarms during the first stages of growth of the Jurassic batholith between 33° and 34°S. The current results, in addition to previous works, suggest that these regional scale oblique structures that crosscut the Andes between 33° and 33°45'S were inherited in part from Jurassic structures, which were reactivated during the Cenozoic.

9.       Acknowledgments

This research was founded by Fondecyt N°1031000 (D.M.) and was a part of the Ph.D. Thesis of the first author, carried out with financial assistance from ME-CESUP and CONICYT grants. Microprobe analyses at Zelmi Laboratory were financed by TU-Berlin and a DAAD studentship for the first author. These analyses were performed under guidance of Prof. G. Franz. The authors want to thank R. Santelices, C. Valenzuela, M. Calderón, N. Astudillo and M. Belmar for sharing with us some days in the field. The authors also want to thank J. Vargas for assistance in mineral separation and F. Galbert and I. Preuss for assistance with microprobe analyses at Zelmi Laboratory, TU-Berlin. J. Cembrano, F. Hervé and C. Mpodozis made valuable comments on early versions of the manuscript. This paper was substantially improved by the reviews made by J. Bartley, A. Willner and H. Diot


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Manuscript received: February 05, 2010; revised/accepted: April 29, 2010.

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