The Acapulco intrusion is a composite pluton that belongs to the coastal batholithic belt of southern Mexico, intruding the Xolapa metamorphic complex and cropping out in the neighboring area of Acapulco city. The Acapulco intrusion has been considered as an anomaly based on its age, which contrasts with the surrounding plutons and the general age trend from the coastal batholithic belt and corresponds to an Eocene–Oligocene age. It ranges in composition from granite (sensu stricto) to syenite and diorite. The most distinctive characteristic of the Acapulco intrusion is the rapakivi texture developed in the granites, which are characterized by biotite, amphibole, allanite, and fluorite as distinctive minerals, plus titanite, zircon, and apatite as accessory phases.
Geochemically, the Acapulco intrusion varies from metaluminous to peraluminous, and displays the distinctive signatures of arc-related magmas. The studied rocks show strong negative Sr, Ba, and Eu anomalies, coupled with incompatible element enrichments and high Ga/Al ratios, which are typical characteristics of A-type granites that underwent strong plagioclase fractionation from a formerly metaluminous magma.
Initial isotopic ratios (87Sr/86Sr from 0.7035 to 0.7100, and εNd from +5.50 to +1.78) indicate a range from depleted mantle compositions to compositions consistent with crustal contamination by continental crust, particularly from the surrounding Xolapa Complex. U-Pb geochronology in zircons by laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) established crystallization ages of 49.40 ± 0.40 Ma, 50.20 ± 1.0 Ma, 50.42 ± 0.39 Ma, and 50.56 ± 0.39 Ma for different lithologies of the Acapulco intrusion. These geochronological data, together with previous published works, confirm that post-Laramide plutonism between 50 and 60 Ma is widespread in the southern continental margin of Mexico as a major magmatic event.
Finally, new thermobarometric determinations established emplacement conditions of ∼700°C at 8–10 km depth (2.08–2.8 kbar), indicating an exhumation rate of ∼0.21 km/m.y. between 50 and 20 Ma, which is slower than the previous estimated rate of 0.44 km/m.y. These results call for a review on models suggesting fast and/or slow exhumation of the southern Mexico coastal batholitic belt.
The active continental margin in southwestern Mexico has been continuously evolving at least since the Jurassic as a result of the eastward subduction of the Pacific-Farallón-Cocos and Rivera plates under the continental crust of the North American plate (e.g., Ortega-Gutiérrez et al., 1994; Dickinson and Lawton, 2001; Morán-Zenteno et al., 2007). Whereas the post-Eocene, subduction-related magmatism is exposed as a volcanic arc (e.g., Martiny et al., 2000; Morán-Zenteno et al., 2007), its plutonic counterpart for the Mesozoic and early Tertiary is mainly exposed along the Pacific coast (Morán-Zenteno et al., 1999). This belt, which broadly extends from Puerto Vallarta to Huatulco, is known as the coastal batholithic belt (Schaaf et al., 1995; Morán-Zenteno et al., 1999, 2005; Martiny et al., 2000; Solari et al., 2007; Martini et al., 2009; Pérez-Gutiérrez et al., 2009). The tectonic evolution of the plutonic belt of southwestern Mexico broadly corresponds with the Laramide orogeny of the western Cordillera in North America and Canada. Locally it has been associated with terrane accretion (e.g., Campa and Coney, 1983; Talavera-Mendoza et al., 2007) or shearing during eastward arc migration (e.g., Martini et al., 2009), combined with shear transmission between lower and upper plate during subduction (e.g., Solari et al., 2007).
In southwestern Mexico, undeformed granitic bodies postdate the end of the Laramide shortening. In general, and at least for the studied area, previous works established the end of the Laramide deformation at ∼55 Ma (e.g., Solari et al., 2007; Cerca et al., 2007).
Yet, geochemical and petrological data of those igneous bodies are scant and mainly focused on a few studied Oligocene rocks such as the Rio Verde Batholith (Hernández-Bernal and Morán-Zenteno, 1996) and the Tierra Colorada pluton (Schaaf, 1990; Herrmann et al., 1994), or on the Tertiary volcanic arc (e.g., Morán-Zenteno et al., 1999; Martiny et al., 2000).
Here, we present new geologic, geochemical isotopic, geochronologic, and thermobarometric data for the Acapulco intrusion that has been considered as an anomaly based on its age, composition, and petrologic characteristics that contrast with the surrounding plutons (mainly calc-alkaline granodiorites) and the general age trend from the coastal batholithic belt (between 35 and 30 Ma, Ducea et al., 2004a; Morán-Zenteno et al., 2007; Valencia et al., 2009). The aim of this paper is to elucidate the main petrogenetic processes involved in its evolution, as well as the tectonic implications of such an important intrusion that can provide valuable information for the post-Laramide magmatism and geological evolution in southern Mexico.
Southern Mexico is composed of a mosaic of contrasting crustal blocks that range in age from Grenvillian (Oaxacan Complex, e.g., Solari et al., 2003), to Paleozoic (Acatlán Complex, e.g., Ortega-Gutiérrez et al., 1999), and Mesozoic (Guerrero arc succession, Talavera-Mendoza et al., 2007; Centeno-García et al., 2008; Martini et al., 2009) (Fig. 1), which are the basis on which southern Mexico has been subdivided into several tectonostratigraphic terranes (e.g., Sedlock et al., 1993; Dickinson and Lawton, 2001; Keppie, 2004). The absence of forearc rocks toward the southern Pacific coast from Paleocene until Miocene times has been interpreted as the truncation of the continental margin of southern Mexico, and it was first observed and discussed by De Cserna (1965). Later studies focused on the tectonic reshaping of southwestern Mexico during the late Mesozoic and Tertiary, involving the displacement of the Chortís block from southern Mexico to its current position, combined with an important contribution of subduction erosion (e.g., Schaaf et al., 1995; Morán-Zenteno et al., 1996; Meschede et al., 1996; Ducea et al., 2004a; Keppie and Morán-Zenteno, 2005; Morán-Zenteno et al., 2005; Nieto-Samaniego et al., 2006; Solari et al., 2007; Keppie et al., 2009).
Active subduction along the southern margin of Mexico took place since the Early Jurassic (∼180 Ma), but significant variations in subduction rates and in the age of the subducted lithosphere were produced since the Oligocene due to the fragmentation of the subducting Farallon plate into Nazca, Cocos, and Rivera (Engebretson et al., 1985).
The coastal batholithic belt intrudes the Xolapa Complex along its southeastern section. As first described by De Cserna (1965), the Xolapa Complex is a 600-km-long and 50–100-km-wide metamorphic belt that parallels the Pacific coast of southern Mexico (Fig. 1), composing the basement of the Xolapa terrane (Campa and Coney, 1983). The Xolapa Complex is made of a sequence of amphibolite-facies metamorphic rocks, repeatedly intruded by deformed and undeformed calc-alkaline plutonic rocks. Recent works by Solari et al. (2007) and Pérez-Gutiérrez et al. (2009) limited the definition of the Xolapa Complex to those rocks affected by migmatization and ductile deformation, which predate the ∼130 Ma intrusion of unmetamorphosed granites (e.g., El Pozuelo granite).
The Acapulco intrusion has been considered as an enigmatic feature in the magmatic evolution of Mexico mainly because its age does not follow the regional trend from the coastal batholithic belt and because of its peculiar rapakivi texture. Nonetheless, modern analytical data are not available, and its tectonic framework remains poorly understood. The Acapulco intrusion was first recognized by De Cserna (1965) as a composite stock with a composition ranging from monzogranite to quartz syenite. The first isotopic age reported on the granitic unit of this pluton was a Rb-Sr isochron calculated at 43.4 ± 0.9 Ma by Schaaf et al. (1995). Later on, Ducea et al. (2004a) dated the quartz-syenite unit of the Acapulco intrusion by LA-ICP-MS in zircons at 54.9 ± 2.0 Ma.
RECOGNIZED LITHOLOGIC UNITS
The lithologic units of the study area include (1) metamorphic basement, including those units that were originally sedimentary or igneous; (2) the Tamuchis deformed granite; and (3) the Acapulco intrusion.
The exposed Xolapa Complex lithologies in the neighboring area of Acapulco (Fig. 2) correspond to those previously studied by Pérez-Gutiérrez et al. (2009). They are characterized by the occurrence of metasediments and orthogneisses with high-grade (amphibolitic) fabrics and a general WNW-trending, NNE-dipping metamorphic foliation (Fig. 3A).
The Tamuchis granite is a ductile deformed pluton that intrudes orthogneisses of the Xolapa Complex to the north of Acapulco city (Figs. 2 and 3B). NE-trending, SE-dipping metamorphic foliations are defined by amphibole and mica. Though no geochronological data are available, the Tamuchis granite is distinguished from the Acapulco intrusion by its deformed nature, and the lack of characteristic minerals that are present in the Acapulco granite (see below). The Tamuchis granite resembles the ∼130 Ma deformed granites cropping out farther to the north, which slightly postdate the migmatization event (e.g., Solari et al., 2007).
The Acapulco composite pluton was divided into three units based on their texture and composition.
This granitic unit is the largest and widespread on the studied area (Fig. 2). It consists of gray-colored granite with some pinkish zones and dark-gray schlieren textures, with 5-cm-thick bands along the entire unit. It contains pink orthoclase (Or), quartz (Qtz), and plagioclase (Pl) with hornblende (Hbl) and biotite (Bt) as accessory minerals. The principal characteristic of this granite is the development of rapakivi texture, i.e., potassic feldspar (Kfs) immersed in sodic plagioclase mantle (Fig. 3C) (Haapala and Ramö, 1990). Black to dark-gray mafic magmatic enclaves (MME) are abundant in this particular unit of the Acapulco intrusion. They are mostly made up of Bt, Hbl, and Pl with some Kfs crystals.
Whereas the albitic (Ab) plagioclase is only restricted to rapakivi mantles in this granite (sensu stricto) (Fig. 4A), oligoclase composition is found in plagioclase crystals present elsewhere in the groundmass (Fig. 4B). Every Kfs crystal within the rapakivi texture presents mesoperthitic textures as well (Fig. 4A). The most distinctive accessory phases under microscope are allanite (Aln) and fluorite (Fl) (Figs. 4C and 4D). Aln occurs as prismatic brown to pinkish crystals and are often zoned. Colorless and isotropic crystals of Fl are generally surrounded by Bt and Hbl (Fig. 4D). Other important accessory phases are titanite (Ttn), zircon (Zr), Ti-Fe oxides (e.g., magnetite [Mag] and ilmenite [Ilm]), and apatite (Ap). Ap shows two different shapes, some stubby to rounded, whereas other crystals are thin and elongated (Fig. 4C).
Under the microscope, the mafic enclaves are quartzodioritic to tonalitic in composition, with diffuse contacts with the granitic host rock and smaller crystal size (Fig. 4E). Big fine-grained clusters of Bt + Hbl + Ap + Tnt can be observed within a coarser Pl + Qz groundmass.
The northwestern and eastern edges of the Acapulco intrusion are composed of quartz syenite (Fig. 2), but an intrusive contact with gneisses and schists of the Xolapa Complex can only be recognized at the southeastern edge (Fig. 2). Both quartz syenites are greenish to gray in color, with a phaneritic texture that allows macroscopic recognition of Kfs, amphibole, and Qz as the main mineral phases (Fig. 3D).
Under the microscope, they can be classified as quartz syenites. Microcline and Qz were identified as principal minerals, displaying mirmekitic textures. Albitic Pl is restricted to perthites within Kfs, where it can constitute up to 30% of the entire crystal. Most common accessory minerals are Hbl with relic orthopyroxene cores, minor biotite, allanite, Ti-Fe oxides, and zircon (Figs. 4F and 4G).
Two previously unidentified dioritic units were recognized within the Acapulco intrusion (Fig. 2). They are dark gray to black in color, showing a phaneritic texture made up of amphibole and Pl crystals with minor pyroxene. We named El Derrumbe diorite a body that crops out along the road that connects Acapulco city with the town of Pie de la Cuesta (Fig. 2). This diorite is intruded by the rapakivi granite (Fig. 3E), which shows some dioritic xenoliths near the contact zone. On the other hand, we also named another body that crops out at the center of the studied area mingled with the rapakivi granite as the Carabalí diorite (Fig. 3F). Interestingly, some crystals with rapakivi texture can also be found within the diorite bodies.
Both mafic intrusives are mainly composed of Pl (labradoritic in composition) with minor Qz (Figs. 4H and 4I). Their characteristic dark color is given by the high amount of mafic minerals, dominated by Hbl and Bt, with the former more abundant than the latter (Fig. 4I).
A total of 17 samples were collected for geochemical analyses. Major elements were determined by X-ray fluorescence (XRF) spectroscopy using a Siemens SRS-3000 instrument installed at the Laboratorio Universitario de Geoquímica Isotópica (LUGIS, Universidad Nacional Autónoma de México [UNAM]), following the procedures described by Lozano-Santa Cruz et al. (1995). Trace-element data were obtained by inductively coupled plasma–mass spectrometry (ICP-MS) at Laboratorio de Estudios Isotópicos (LEI), at Centro de Geociencias (CGEO, UNAM), using a Thermo X Series II instrument. Because most of the studied intrusive rocks contain zircon, the digestion procedure described by Mori et al. (2007) for low-pressure vessels was modified to ensure complete solution. Rock powders were first digested in a mixture of HF + HNO3 and then diluted to 3 mL in 4N HNO3 and further centrifuged. Solid residuals were separated and re-digested in 500 μl of HF and 250 μl of 8N HNO3 and put into a high-pressure Parr vessel at 200°C for a period of four days. Digested residuals were dried and refluxed overnight with concentrated HNO3 to break down insoluble fluorides. The two sample splits were then mixed together, evaporated to dryness, and later diluted to 1:2000 to provide adequate concentrations within the instrument detection limits and to yield the correct signals required for high-precision data. Data acquisition procedures and typical reproducibility follow those described by Mori et al. (2007).
Isotopic determinations were performed at LUGIS (UNAM) for both WR and feldspar separates. Sr, Sm, Nd, and Pb isotopic ratios were obtained using isotope dilution–thermal ionization mass spectrometry (ID-TIMS) following the standard methods described by Schaaf et al. (2005) and Solari et al. (2004), using a Finnigan MAT262 mass spectrometer equipped with eight Faraday detectors. Rb isotopic ratios were measured with a National Bureau of Standards (NBS)-type single collector mass spectrometer as described by Schaaf et al. (2000). Zircons separated from four samples were dated by LA- ICP-MS U-Pb geochronology at LEI, using the instrumentation and procedures described in Solari et al. (2010). Unknown ages were calculated employing the 91500 standard zircon (Wiedenbeck et al., 1995) as bracketing standard. The Tuff-Zirc algorithm (Ludwig and Mundil, 2002) was used to calculate the mean 206Pb/238U ages and their errors, as well as to filter for outliers. Such age calculation is preferred for Phanerozoic ages obtained by LA-ICP-MS, due to the uncertainty of 207Pb determination.
Electron-microprobe analyses were performed at Stanford University using a JEOL JXA-733A superprobe fitted with five wavelength-dispersive spectrometers and a Be-window SiLi energy-dispersive detector, and 15 kv, 20 nA, and 20 s as instrument settings. Standards and crystals used were: Na (albite), Mg (olivine), Al (spessartine), Si (wollastonite), K (orthoclase), Ca (wollastonite), and Fe (hematite). Plagioclase analyses were performed with a defocused electron beam at 10 μm due to the complexity of Na measurements. Each crystal was analyzed three times for statistical control. Quantitative analyses were performed using the CITZAF matrix correction algorithm (Armstrong, 1988). Relative standard deviations for major oxide components were 1%, 10% for minor elements, and 15% for trace elements.
Major- and Trace-Element Geochemistry
Major- and trace-element abundances are reported in Table 1. In general, the Acapulco intrusion rocks vary between 51.49 and 76.95 wt% SiO2, whereas Al2O3 is in the range 12.25 to 17.06 wt%, K2O from 1.40 to 5.10 wt%, Na2O from 3.36 to 5.31 wt%, CaO from 0.28 to 7.43 wt%, MgO from 0.10 to 6.23 wt%, TiO2 from 0.07 to 1.26 wt%, FeO* from 1.32 to 10.19 wt%, and P2O5 from 0.01 to 0.28 wt%. Major elements show negative correlation with SiO2 except for K2O and Na2O (Fig. 5). This behavior may represent crystal fractionation of plagioclase, apatite, ilmenite, and titanite during the crystallization of the Acapulco intrusion.
The Acapulco samples can be classified as diorite, granite, and syenite in a total alkali versus silica (TAS) diagram for plutonic rocks according to Wilson (1989) (Fig. 5A), and belong to the calc-alkaline series in an AFM diagram (Irvine and Baragar, 1971). Using the Shand's index of alumina saturation, the Acapulco intrusion classifies as metaluminous (e.g., diorites) to slightly peraluminous granite (Maniar and Piccoli, 1989) (Fig. 5B).
Eu and Sr contents correlate negatively with SiO2, whereas Nb, Ta, U, and Th have positive correlations due to the highly incompatible behavior of the lithophile elements (Fig. 5). Rocks from the Acapulco intrusion have high large-ion lithophile to high field strength element (LIL/HFSE) ratios that are common in subduction related magmas, but often display strong Ba, Sr, and Eu negative anomalies in primitive-mantle–normalized trace-element diagrams (Fig. 6A). They also show enriched light rare-earth element (LREE), flat heavy rare-earth element (HREE) patterns in CI-chondrite normalized diagrams (Fig. 6B). Such high LREE values (La = 12.72–82.15 ppm) and low Yb (2.33–11.73 ppm) represent La/Yb rations between 1.4 and 25.1.
Even though the Acapulco rocks show arc-related trace-element patterns, they plot at the limit between volcanic arc granites (VAG) to within-plate granites (WPG) in a Y + Nb versus Rb diagram (Pearce et al., 1984) (Fig. 7A). A similar behavior can be found in the classic I&S type and A-type granite discrimination diagram (Whalen et al., 1987) (Fig. 7B). Nonetheless, the most mafic diorite samples invariably plot within the field of arc-related magmas in both diagrams (Figs. 7A and 7B).
Results for Sr-Nd-Pb isotopic determinations are shown in Table 2. Initial isotopic ratios for the Acapulco intrusion samples are highly variable for 87Sr/86Sr from 0.7035 up to 0.7100, while 143Nd/144Nd ratios are almost constant, ranging from 0.51266 to 0.51272, except for El Derrumbe diorite, which has a ratio of 0.51285. Samples plot along the coastal batholithic belt field of Morán-Zenteno et al. (1999) (Fig. 7C). Even with such variations, most Acapulco samples fit within the normal mantle array represented by mid-ocean ridge basalts (MORBs) and ocean island basalts (OIBs), with the Sierra Nevada of California rocks representing a continental magmatic arc suite (Fig. 7C). On the other hand, Pb isotopes show an almost homogenous behavior with slightly higher 206Pb/204Pb and 207Pb/204Pb values compared to Pacific-type MORB ratios (Ito et al., 1987), although they are lower than those from the Xolapa Complex (mid-crust basement, Herrmann et al., 1994; Pérez-Gutiérrez et al., 2009), displaying a positive trend almost parallel to the Grenvillian Oaxacan Complex (lower-crust basement, Solari et al., 2004) (Fig. 7D).
Zircons separated from three samples of the rapakivi granite and one more from the quartz syenite are generally euhedral, prismatic, and colorless to amber. They show D, P5, and P4 morphologies according to Pupin (1980, 1988), with a maximum elongation ratio of 3:1 and general size of ∼200 μm. Cathodoluminescence (CL) images of these samples show oscillatory zoning indicative of a magmatic origin, which sometimes grows around inherited, igneous cores. Results of U-Pb dating by LA-ICP-MS are shown in Table 3. Using the Tera-Wasserburg diagrams plotted with Isoplot/Ex v. 3.60 (Ludwig, 2008), the samples from the rapakivi granite (Ac0702, Ac0707, and Ac0722) yield ages of 50.20 ± 1.0 Ma (Fig. 8A), 50.56 ± 0.39 Ma, and 50.42 ± 0.39 Ma, respectively (Figs. 8C and 8D). Zircons from the quartz syenite yield a 206Pb/238U mean age of 49.40 ± 0.40 Ma (Fig. 8B). All ages are interpreted as crystallization ages and constrain the emplacement of the Acapulco intrusion at ∼50 Ma. Those cores, which were also dated, are only slightly older than the obtained mean ages of 2–3 Ma. This indicates that such ages reflect the initial stage of zircon crystallization in the magma chamber, and that the Acapulco intrusion is practically devoid of xenocrystic, inherited nuclei belonging to the host rock. The age of ca. 50 Ma that we calculated for the Acapulco intrusion is slightly younger than the previous, 54.9 ± 2 Ma age obtained by Ducea et al. (2004a). We think that such difference reflects the variation of zircon crystallization and residence in the magma chamber, the same as in the case of the sample dated by Ducea et al. (2004a) has a spreading of 12 Ma (their Fig. 6a).
Thermometry and Barometry
Electron microprobe analyses were performed in different samples from the Acapulco granite, and the results are shown in Table 4. We analyzed coupled crystals (Pl and Hbl) in order to determine thermobarometric conditions following the methodology proposed by Anderson (1996), which requires emplacement temperatures to solve the corresponding geobarometric equations. In this study, we used Holland and Blundy (1994) Hbl-Pl thermometer “B” for the Edenite-Richterite system. Temperatures in Celsius degrees were calculated using HbPl v.1.2 software, yielding values between 692 and 737°C with no apparent reequilibration (Table 4). Furthermore, the Ti content in zircons from the LA-ICP-MS analyses was used (Table 3), in order to apply the Ti-in-zircon thermometric determinations following the equations of Ferry and Watson (2007) yielding average temperatures of 739°C (Table 3), which confirms the range of temperatures calculated with the Hbl-Pl geothermometer.
According to the mineral association observed in the rapakivi granite: two feldspars + quartz + biotite + hornblende + Fe-Ti oxides + titanite + apatite, we used the Al-in-hornblende barometer from Anderson and Smith (1995), modified from Schmidt (1992), with temperature as a parameter and the incorporation of experimental data of Johnson and Rutherford (1989). We applied these analysis to mineral clusters that show equilibrium textures, in particular with plagioclase that are not rapakivi texture related, and the main objective was to constrain a more accurate determination. All analyses together yield emplacement pressures between 2.08 and 2.84 kbar corresponding to 7.84–10.73 km depth (Table 4).
The new data presented in this study allow a better understanding of the emplacement and cooling conditions of the Acapulco intrusion, as well as the role of such plutons in the post-Laramide tectono-magmatic activity of southern Mexico. In this section we discuss the petrogenesis and evolution of the Acapulco intrusion and its implications, going from the microscopic scale to the regional tectonic context.
Significance of Accessory Minerals
The presence of fluorite in the Acapulco intrusion indicates the magmatic fluids evolved under fluorine saturation conditions. According to the observed crystallization order, hydrous minerals (particularly Bt and Hbl) preceded Fl (Fig. 4D), suggesting Fl crystallized in a later stage at lower magmatic water contents. This behavior has been explained as the entrapment of halogens in the silicic dry magma until reaching the saturation point, which usually occurs after the final crystallization of hydrous phases (Kilinc and Burnham, 1972; Frost and Frost, 1997). On the other hand, fluorine, along with Kfs, reduces the viscosity of the magma, affects the diffusion rate in Na-K system, and decreases the melting point of feldspars (Giordano et al., 2004). As a result, Kfs crystals exsolve their molar albite fraction developing the observed perthitic textures (Snow and Kidman, 1991). Thus, we consider that fluorine played a key role in the development of the characteristic mineralogy in the Acapulco intrusion, as also reported in other felsic magmatic systems (e.g., Agangi et al., 2010).
It is also known that Aln can control LREE content (e.g., Ce and La) and Th as well in granitic magmas (Deer et al., 1986; Gieré and Sorensen, 2004; Hoshino et al., 2005). Beyond its effect in the trace-element distribution, the occurrence of Aln in metaluminous rocks with high-aluminum content suggests that crystallization of this magma took place between 600 and 800°C (Chesner and Ettlinger, 1989; Gieré and Sorensen, 2004), which is in accordance with our thermometric determinations of 700–730°C.
Development of the Rapakivi Texture
The origin of Kfs crystals immersed in a Pl mantle, better known as rapakivi texture, has been under debate for several decades since it was first described (Stimac and Wark, 1992, and references therein). Sensu stricto, a rapakivi texture is defined as ovoid-shaped Kfs crystals surrounded by Pl rims with an average composition of Ab90–70. In the case of the Acapulco granite, euhedral Kfs crystals are rimmed by albitic Pl giving place to a pseudo-rapakivi or rapakivi texture sensu lato (Dempster et al., 1994). The metaluminous to peraluminous character of the Acapulco granite, with pyroxene relicts and general crystallization temperatures around 700°C, corresponds to a typical rapakivi granite, which is subsaturated in water and emplaced at a maximum depth of 10 km (Haapala and Ramö, 1990; Emslie, 1991; Stimac and Wark, 1992).
Different models have been proposed for the origin of the rapakivi texture. In general, two interpretations dominate: (1) a magmatic origin and (2) a subsolidus origin (Dempster et al., 1994). The magmatic process invokes immiscibility between two types of melts, metasomatic replacement, magma mixing or assimilation of mafic rocks, and fluid saturated magma degassification (Stimac and Wark, 1992; Dempster et al., 1994; Ramö and Haapala, 1996; Frost and Frost, 1997; Calzia and Ramö, 2005). Although there are many inconsistencies in those models, and considering that the rapakivi granites represent large batholiths, such mechanisms seem to be unrealistic due to the thermal and volumetric implications (Dempster et al., 1994). On the other hand, what has been called the subsolvus mechanism can present some problems to exsolve sodic plagioclase from alkaline feldspar due to the low diffusion rate of alkalis in the Kfs (Snow and Kidman, 1991; Dempster et al., 1994).
Therefore, we propose a model for the Acapulco granite rapakivi texture based on our petrologic, mineral, and chemical observations. At the early stage of crystallization, Kfs crystals were stable and well developed (Fig. 9A). Later, during the initial stage of crystallization of the hydrous phases, the concentration of halogens increased. Fluorine saturation favored Kfs instability, forcing it to exsolve its Pl molar fraction, mainly of oligoclase composition, developing perthites and further lamellae textures (Figs. 9B and 9C). Albitic plagioclase was exsolved later, forming the phenocrystic rims of the rapakivi texture (Fig. 9D).
Is the Acapulco Intrusion Part of an A-Type, Alkaline Magmatic Pulse in Southern Mexico?
Since the first description of the Acapulco granite by De Cserna (1965), this pluton has been considered part of an alkaline magmatic event within the coastal batholithic belt. There are many factors that support this interpretation, including the rapakivi texture, Fl occurrence, and pyroxene relicts. It is not unusual to associate alkaline rocks with continental rift and post-collision magmatism, because such rocks show mantle-like isotopic signatures and hypersolvus, as well as the typical rapakivi textures that normally form at shallow depths (Anderson, 1983; Kemp and Hawkesworth, 2004). This evolution is not congruent, however, with the geological setting of the coastal batholithic belt that has been interpreted as a continental magmatic arc (Schaaf et al., 1995).
As we established earlier, Ca, Ba, Sr, and Eu depletion was controlled by fractional crystallization in equilibrium with Pl (Fig. 10A). Such effect could produce incompatible element enrichment (Kemp and Hawkesworth, 2004), but the less evolved unit of the intrusive (diorites) still maintains chemical characteristics of arc-related rocks (Fig. 10A). The incompatible elements enrichment is considered a diagnostic feature for A-type granites together with extremely high Zn content (>>80 ppm) combined with high Ga/Al ratios (Collins et al., 1982; Whalen et al., 1987). Samples belonging to the Acapulco intrusion are not within this range, though their (Ga/Al) × 104 ratios are as high as 3.32, a feature that may have resulted from fractional crystallization of plagioclase (Kemp and Hawkesworth, 2004). This behavior may be a convergence between highly fractionated metaluminous I-type granites and A-type granites, as is shown in Figure 10B. Furthermore, by comparing the Eu anomaly (Eu/Eu*) with Th content, it is clear that the Acapulco intrusion belongs to a suite of I-type granites according to Eby (1992) (Fig. 10C). Even though all these classifications are considered empirical, we believe that they can be applied in order to understand graphically those chemical differences between the A-type granites and the Acapulco intrusion (Fig. 10).
Role of Crustal Assimilation
The geological and analytical data provided in this paper suggest that the Acapulco granite was emplaced during a magmatic stage related to the Laramide subduction process. This interpretation differs from the traditional idea of an alternative tectonic scenario related to intra-plate magmatism (e.g., Morán-Zenteno et al., 1996). The high Pb/Ce (0.06–0.27) and Th/Nd (0.07–1.38) ratios of the Acapulco granite are not typical of intraplate magmatism and suggest either a crustal or subducted sediment contribution in a subduction setting. Yet the relatively constant Nd and Sr isotopic compositions at variable Th/Nd and 87Sr/86Sr ratios are inconsistent with sediment additions, because all these elements are similarly mobile in the subduction flux and thus should enrich the source at the same time (Gómez-Tuena, et al., 2007). Crustal contamination will modify the isotopes concurrently with fractionation only if a large isotopic contrast exists between the primitive magma and the contaminant. Since the only significant isotopic distinction between the Acapulco granite and the local basement (Xolapa Complex) is observed in the Sr isotopes (Fig. 7), and especially in its micas, the effects of crustal contamination can be better constrained using this isotopic system (Fig. 10D). Thus, we conclude that contamination with the mica-rich lithology of the Xolapa Complex is responsible for the radiogenic Sr isotopic compositions observed in the most evolved syenites. Since mica does not incorporate Nd or Pb in significant quantities (Bebout et al., 2007), these isotopic systems will remain undisturbed during assimilation.
The origin of the high fluorine concentrations, permitting the crystallization of fluorite from the magma remains uncertain. The geochemical behavior of fluorine in subduction-related settings is generally considered to be conservative, because only ∼4% of it is recycled by dehydration of secondary amphibole carried by the subducted oceanic slab and released into the overlying mantle wedge (Ito et al., 1983; Straub and Layne, 2003). Thus, the excess fluorine in the Acapulco intrusion cannot be attributed to subduction-related processes alone. The variation in radiogenic Sr tends toward the composition of white mica (e.g., muscovite, Fig. 10D), which is contained in the older metasediments of the Xolapa Complex (>130 Ma, e.g., Morán-Zenteno, 1992; Solari et al., 2007). Thus, it is likely that the contamination of the Acapulco intrusion (in particular the quartz syenites) resulted from the interaction between released fluids from the host rocks and the granitic magmas. Such fluorine-enriched fluids can be explained by mica (muscovite) dehydration from the surrounding metasediments from the Xolapa Complex at temperatures above 700°C (e.g., Guggenheim et al., 1987). Furthermore, this process could provide an explanation for the presence and origin of the fluorine-rich fluids in the Acapulco magmatic system.
The Evolution of the Acapulco Intrusion and Its Tectonic Implications in Post-Laramidic Magmatism
The thermobarometric results obtained in this paper (e.g., 10 km maximum depth) allows the construction of an exhumation curve (Fig. 11A), which has been adjusted with those estimations for the Xolapa Complex for the past 20 Ma (∼3.6 km depth) based on (U-Th)/He thermochronology (Ducea et al., 2004b). We can establish two different exhumation rates that consist of a first period with a moderate rate of 0.21 km/m.y. and a second period of slower exhumation rate of 0.18 km/m.y. (Fig. 11A; Ducea et al., 2004b). These estimations differ from those obtained by Morán-Zenteno et al. (1996), who considered an emplacement depth between 13 and 20 km, calculating a constant exhumation rate of 0.44 km/m.y. before 20 Ma. The nearby younger and nondeformed plutons of Tierra Colorada, Xaltianguis, and San Juan del Reparo, show crystallization ages between 32 and 34 Ma (Herrmann et al., 1994; Ducea et al., 2004a; Hernández-Pineda, 2006). According to their chemistry, mineralogy and textural characteristics were probably emplaced at a maximum depth of ∼6 km (Fig. 11A).
The Paleocene magmatic event in southern Mexico is still poorly understood due to the scarcity of outcrops (Morán-Zenteno et al., 2007). However, recent U-Pb zircon geochronological data from the coastal batholithic belt (e.g., Ducea et al., 2004a; Solari et al., 2007; Martini, 2008; Pérez-Gutiérrez et al., 2009; Valencia et al., 2009; and this paper), confirm the occurrence of a regional magmatic episode between 50 and 60 Ma for the central portion along the coast (e.g., between Zihuatanejo and Acapulco), which characterizes a post-Laramide magmatic event in this area of southern Mexico (Fig. 11B).
After cessation of the Laramide orogeny in southern Mexico, which, according to Cerca et al. (2007) and Solari et al. (2007), was characterized by flat subduction, the slab increased the angle of subduction producing a N-S migration toward the coast from 68 to 50 Ma in the Mezcala-Acapulco sector (Meza-Figueroa et al., 2003; Ducea et al., 2004a; Solari et al., 2007). This rearrangement in the subduction geometry increased the geothermic gradient giving place to the 60–50 Ma magmatic pulse (Fig. 11C).
The ascent and emplacement of the magmas from the Acapulco intrusion may have occurred during the extensional deformation represented near the studied area by La Venta shear zone, ∼30 km N from Acapulco, dated at 45–50 Ma (Solari et al., 2007) (Figs. 11A and 11C). This extensional event has been associated either with an oblique convergence between the Farallon and North American plates or with the separation of the Chortís block from southern Mexico (Herrmann et al., 1994; Schaaf et al., 1995; Morán-Zenteno et al., 1996). Such mechanism is well documented worldwide and associated with the generation of space that allows the ascent and emplacement of granitic magmas (Hutton et al., 1990; Vigneresse, 1995a, 1995b; Petford et al., 2000).
We presented geologic, geochemical, geochronologic, and thermobarometric data for the Acapulco intrusion as an example of post-Laramide magmatism in southern Mexico. Based on our results and those previously published, we propose a tectono-magmatic evolution summarized in Figures 11B and 11C in which the ∼50 Ma Acapulco intrusion is part of the post-Laramide magmatic event originated through the increment in the angle of subduction, which favors the north to south migration of the magmatism in the area. We also document the contribution of radiogenic Sr- and F-saturated fluid conditions recorded in the metaluminous-peraluminous Acapulco intrusion as a contamination feature of muscovite-bearing metasediments of the Xolapa Complex. This process occurred due to the remobilization during high-temperature emplacement of the Acapulco body. Furthermore, we propose a model for development of the rapakivi texture originated by the fractional crystallization of plagioclase, combined with high-fluorine fugacity. Finally, the combination of previously available data and those presented here allow us to establish two exhumation rates for the Acapulco intrusion: the first one of 0.21 km/m.y. since its emplacement at ∼10 km of depth, which is followed by a second stage of 0.18 km/m.y. starting in the Miocene, ∼20 Ma (Ducea et al., 2004b).
As a whole, the post-Laramide plutonism in southern Mexico, characterized by the absence of penetrative deformation, occurred in a quite long-lasting event from the latest Paleocene (e.g., Solari et al., 2007) to the earliest Oligocene (e.g., Schaaf et al., 1995; Ducea et al., 2004a). Thanks to our current work, the Acapulco intrusive is now one of the best characterized examples of this widespread plutonic event, which constitutes the eroded roots of the late Eocene to Miocene volcanic arc of Sierra Madre del Sur (e.g., Morán-Zenteno et al. 2007).
Fruitful discussions with F. Ortega-Gutiérrez, D. Morán-Zenteno, C. Mattinson, and F. Jenner allowed clarification of several aspects in this research. This paper benefited from funds granted to LAS from Consejo Nacional de Ciencia y Tecnologia (CONACyT) (54559 and J-39783) and PAPIIT IN101407. GAHP wants to thank J.G. Liou, W.G. Ernst, and U. Martens, from Stanford University, for all their support and advice during his stay in the 2008 winter quarter. GAHP was supported during his Master's thesis studies at UNAM by a CONACyT scholarship. We wish to thank R. Jones for assistance at the electron microprobe analysis laboratory at Stanford University. We would also thank P. Schaaf, G. Solís-Pichardo, J.J. Morales, M.S. Hernández-Bernal, and T. Hernández-Treviño from LUGIS for assistance and their participation during isotope analytical work and data acquisition. J. Callejas Moreno and R. Hernández Ordoñez are thanked for their assistance and company during fieldwork. We appreciate comments and reviews from the editor C. Frost and M. Valencia-Moreno, T. Toulkeridis, and an anonymous reviewer that helped to improve the manuscript.