Heterogeneous magmas of the Quaternary Sierra Chichinautzin volcanic field (central Mexico): the role of an amphibole–bearing mantle and magmatic evolution processes

 

Magmas heterogéneos del campo volcánico Cuaternario de la Sierra de Chichinautzin (México central): el papel de un manto con anfibol y los procesos de evolución magmática

 

Lorenzo Meriggi^1,*, José Luis Macías¹, Simone Tommasini², Lucia Capra³, and Sandro Conticelli^2,4

 

¹ Instituto de Geofísica, Universidad Nacional Autónoma de México, Ciudad Universitaria, Delegación Coyoacán, 04510, México D.F., México. * meriggi@geofisica.unam.mx

² Dipartimento di Scienze della Terra, Universitá degli Studi di Firenze, Via La Pira 4, Firenze, 1–5012, Italy.

³ Centro de Geociencias, Universidad Nacional Autónoma de México, Campus Juriquilla, Apartado Postal 1–742, 76001 Querétaro, Qro., México.

⁴ Istituto di Geoscienze e Georisorse, Sezione di Firenze, Consiglio Nazionale delle Ricerche, Via La Pira 4, Firenze, 1–50121, Italy.

 

Manuscript received: May 16, 2007
Corrected manuscript received: January 10, 2008
Manuscript accepted: January 13, 2008

 

ABSTRACT

The Quaternary Sierra Chichinautzin volcanic field (SCVF) is located at the volcanic front of the Trans–Mexican Volcanic Belt (TMVB), 350 km from the Middle American trench where the Cocos plate subducts beneath the North American plate. The SCVF is characterized by more than 200 monogenetic centers, ranging in composition from rare basalts to dacites. Less evolved terms have aphyric to porphyritic textures with phenocrysts of euhedral olivine (± Cr–spinels inclusions) + cpx, –whereas evolved terms have porphyritic textures with phenocrysts of pyroxene (cpx>opx), xenocrysts of corroded quartz, and sieve–textured plagioclase from the local basement. Regardless of the degree of magmatic evolution, plagioclase occurs as microphenocrysts or in the groundmass.

New geochemical and isotopic data presented in this work are in good agreement with previous analyses; however, a new division for the SCVF mafic rocks (MgO >6.0 wt.%) is proposed. In fact, although concentrations of large ion lithophile elements (LILE) and light to medium rare earth elements (REE) are roughly constant in mafic rocks, TiO₂ and other high field strength elements (HFSE) such as Nb are scattered and vary from 0.8 to 1.8 wt.% and from 5 to 30ppm, respectively. These characteristics allow grouping the SCVF rocks in two main magmatic series with different TiO₂–HFSE enrichment: high(H)–TiO₂ and low(L)–TiO₂, with subordinate transitional samples. Additionally, a cinder cone with shoshonitic affinity and extremely high LILE/HFSE ratio is reported for the first time in central Mexico. Compositional variability is also observed among the mineral phases of these mafic rocks (e.g., the Cr# of spinel hosted in olivine phenocrysts), and the ⁸⁷Sr/⁸⁶Sr ratios that progressively increase from the H–TiO₂series (0.70307–0.70425) to the L–TiO₂ series (0.70365–0.70434), up to the shoshonitic scoria (0.70456).

The calc–alkaline affinity, LILE, and Pb positive anomalies of the magmas confirm the occurrence of a subduction–related metasomatised mantle wedge beneath the studied area (particularly for the shoshonitic scoria), but enrichments in TiO₂ and other HFSE are controversial. These enrichments are not common in subduction–related magmas because these elements are not easily removed by aqueous fluids from the subducted slab. However, recent works have demonstrated that HFSE can be relatively soluble in high–temperature fluids/melts arising from the slab, and the presence of TiO₂–rich Cr–pargasite in Iherzolite xenoliths of the Valle de Bravo area prove the existence of a mantle phase with high–HFSE concentrations. Therefore, partial melting of such hydrated peridotite could explain the genesis of H–TiO₂ magmas as suggested by the proposed REE model.

Moreover, isotopic ratios and variations in major and trace element concentrations of–western SCVF rocks indicate that fractional crystallization plus crustal assimilation are the main evolution processes in the studied area.

Key words: volcanic rocks, high–TiO₂, Sr and Nd isotopes, magmatic evolution, Sierra Chichinautzin, Trans–Mexican Volcanic Belt, Mexico.

 

RESUMEN

El campo volcánico de la Sierra de Chichinautzin (CVSC) está ubicado en la porción frontal del Cinturón Volcánico Transmexicano (CVTM) a 350 km de distancia de la Fosa Mesoamericana. El CVSC está compuesto por más de 200 centros monogenéticos cuyas rocas varían desde basaltos a dacitas. Las rocas menos evolucionadas tienen texturas desde afincas hastaporfiríticas confenocristales euhedrales de olivino (± inclusiones de Cr–espinela) + cpx, mientras que las rocas más evolucionadas tienen textura porfirítica confenocristales de piroxeno (cpx>opx), xenocristales de cuarzo parcialmente reabsorbidos y plagioclasa con textura de tamiz provenientes del basamento. Independientemente del grado de evolución magmática, las plagioclasas aparecen exclusivamente en la matriz de las rocas.

Los nuevos datos geoquímicos e isotópicos de este trabajo concuerdan con estudios previos. Sin embargo, con el análisis de rocas máficas del CVSC (MgO >6.0% en peso) se propone una nueva subdivisión. Aunque la concentración de los elementos litófilos de radio iónico grande (LILE) y de las tierras raras (REE) ligeras y medianas es relativamente constante en las rocas máficas, el TiO₂y otros elementos de alto potencial iónico (HFSE) como el Nb presentan una mayor variación (0.8–1.8 % en peso y 5–30 ppm, respectivamente). Estas características permiten la subdivisión de los magmas del CVSC en dos series magmáticas principales con diferentes concentraciones de TiO₂ y HFSE (series de alto(H)–TiO₂ y bajo(L)– TiO₂), además de algunas muestras de afinidad transicional. Asimismo se reporta por primera vez en el centro de México un cono de escoria con afinidad shoshonítica y relaciones elevadas de LILE/HESE. Estas heterogeneidades composicionales se reflejan también en las variaciones del Cr# en las espinelas presentes en fenocristales de olivino y en las relaciones ⁸⁷Sr/⁸⁶Sr que aumentan paulatinamente de los productos de la serie H–TiO₂ (0.70307–0.70425), a aquellos de L–TiO₂ (0.70365–0.70434) hasta los valores de 0.70456 de la shoshonita.

La afinidad calcialcalina y las anomalías positivas de LILE y Pb confirman la presencia de un manto metasomatizado en el área estudiada, aunque los enriquecimientos de TiO₂ y HFSE no pueden explicarse fácilmente. Estos enriquecimientos son raros en magmas de zonas de subducción, ya que estos elementos no pueden ser transportados por fluidos a través de la cuña del manto. Sin embargo, se ha demostrado recientemente que los HFSE pueden ser relativamente solubles en los fluidos/fundidos de alta temperatura que ascienden de la placa en subducción. La ocurrencia de xenolitos peridotíticos con Cr–pargasita rica en TiO₂ en el área de Valle de Bravo confirma la existencia de una fase cristalina del manto que contiene concentraciones altas de elementos HFSE. Por lo tanto, la fusión parcial de esta peridotita hidratada podría explicar las anomalías de TiO₂ en los magmas de la CVSC, como se demuestra en el modelo presentado.

Asimismo, las relaciones isotópicas y las variaciones de los elementos mayores y trazas indican que la cristalización fraccionada acoplada a contaminación cortical son los principales procesos de evolución en el área estudiada.

Palabras clave: rocas volcánicas, high–TiO₂, isótopos de Sr y Nd, evolución magmática, Sierra de Chichinautzin, Cinturón Volcánico Trasmexicano, México.

 

INTRODUCTION

Magmas generated at convergent plate margins are characterized by typical chemical fingerprints: higher large ion lithophile element contents (LILE; e.g., Cs, Rb, K, Ba, and Pb) with respect to high field strength element contents (HFSE; e.g., Nb, Ta, Zr, and Hf) and lower FeO_totrelative to other sub–alkaline rocks such as MORB (e.g., Gill, 1981; Wilson, 1989; Arculus, 2003). The processes that bring to these chemical characteristics are still a matter of debate, but they might be related to (1) partial melting of mantle peridotite containing a Tirich phase as titanate or amphi–bole in the residuum of partial melting (e.g., Nicholls and Ringwood 1973; Hofmann 1988); or more probably to (2) partial melting processes of a mantle wedge metasomatised by fluids/melts released by the subducting slab (e.g., Turner et al, 1997; Walker et al, 2001). Both aqueous fluids and melts from subducted sediments are capable to decrease the solidus of the peridotite of the mantle wedge triggering partial melting (e.g., Saunders et al, 1980, Pearce and Peate, 1995), enriching the mantle wedge source and producing magmas with high LILE with respect to HFSE (e.g., Tatsumi et al., 1983; Elliott et al.,1991; Patino et al., 2000, Walker et al, 2001). Besides, partial melting of altered subducted oceanic MORB lithosphere has been claimed for the generation of silica–rich magmas (e.g., dacites and rhyolites) that produce magmatic rocks with high Sr/Y ratios and other incompatible elements, called adakites (e.g., Drummond and Defant 1990; Defant and Drummond, 1990; Gómez–Tuena et al., 2007). At continental plate margins, however, rhyolites with high LILE/HFSE values might also be generated by partial melting of the lower crust or by magmatic evolution of a high–alumina basaltic magma through fractional crystallization plus crustal assimilation (AFC) processes (e.g., Francalanci et al., 1993; Castillo et al., 1999; Xuet al., 2002).

The study of mantle–inherited features is a difficult task in subduction–related magmas because of the paucity of magmas that have been little modified after their genesis (primitive magmas). A magma in equilibrium with its mantle source should have Mg# values higher than 65 (Green, 1971), FeO_tot/MgO less than 1 (Tatsumi et al, 1983), MgO >6 wt.% (Luhr, 1997), and Ni = 235–400 ppm (Sato, 1977), characteristics rather unusual in many arc–related magmas.

At convergent plate margins, besides typical arc magmas (e.g., arc tholeiites, cale–alkaline), alkaline mafic magmas with either subduction–related or intra–plate characteristics can be found (e.g., van Bergen et al, 1992; Green, 2005). Potassic and ultrapotassic magmatic rocks with evident HFSE depletion have been found in central Italy (e.g., Conticelli andPeccerillo, 1992; Conticelli 1998; Conticelli et al, 1997, 2002, 2007), in the Aeolian Arc, south Italy (e.g., Francalanci et al, 1993, 1999, 2004), in the Sunda–Banda Arc (e.g., van Bergen et al, 1992) and in the Trans–Mexican Volcanic Belt (e.g., Carmichael et al, 1996). On the other hand, OIB–like alkali basalts have been found in the Cascade Range (e.g., Reiners etal, 2000; Smith and Leeman, 2005); high–TiO₂ lavas are present in the Central America volcanic arc (e.g., Walker et al, 1990); and intra–plate alkaline magmas have been found in the Trans–Mexican Volcanic Belt (e.g., Luhr, 1997; Ferrari et al., 2000). Production of magmas with transitional to OIB–like geochemical characters at convergent plate margins have been explained as follow: 1) different magma genesis mechanisms, e.g., flux vs. decompressional melting (e.g., Reiners et al, 2000); 2) mantle heterogeneity at small scale (e.g., Feigenson and Carr, 1993; Strong and Wolff, 2003); 3) roll–back of the subducted plate with slab window opening (Ferrari et al, 2001); 4) continental rifting (e.g., Verma, 2000, 2002); 5) uprise of a deep–seated mantle plume (e.g., Márquez et al, 1999a, 199b; Márquez and De Ignacio, 2002).

In this context, the Sierra Chichinautzin volcanic field (SCVF) (Figure 1) represents a unique site to perform petrological and geochemical studies to address the problem of contemporaneous presence of within–plate and subduction–related magmas at a destructive plate margin because of the abundant presence of fairly primitive magmas (MgO >6.0 wt.%), with different LILE/HFSE ratios, despite the thickness of the continental crust (45 km, e.g., Urrutia–Fucugauchi and Flores–Ruiz, 1996). The aim of this paper is to investigate the magma genesis and the evolution processes of the Tenango area, located in the westernmost SCVF, between the late Pliocene Sierra de Las Cruces volcanic chain (Figure 1c; Bloomfield, 1974, 1975; Osete et al., 2000) and the late Pliocene to Holocene Nevado de Toluca volcano (García–Palomo et al., 2002a), where both primitive magmas and evolved lava flows coexist. Although this area has been previously studied by other authors (Bloomfield, 1974; 1975; García–Palomo et al, 2000; 2002a; Martinez–Serrano et al., 2004) we present new geochemical and petrographic data of Chapultepec, Villa Metepec, Emerenciano and Sta. Cruz cinder cones and a more exhaustive sampling of Texontepec and the Tenango lava flow (Figure 1c).

 

GEOLOGICAL BACKGROUND

The Trans–Mexican Volcanic Belt (TMVB) is a 1,200–km long volcanic chain that transects Mexico from the Pacific Ocean to the Gulf of Mexico (Figure 1a). The oldest Trans–Mexican Volcanic Belt products are Miocene in age and form a widespread mafic to intermediate volcanic arc with cale–alkaline to slightly alkaline affinity (Ferrari et al., 2000). Miocene to present–day volcanism in the TMVB consists of large stratovolcanoes and dispersed mono–genetic volcanic centers that have erupted calc–alkaline, Na–alkaline and K–alkaline magmas. In some regions the monogenetic cones are associated with poly genetic volcanoes (e.g., Colima volcano; Luhr and Carmichael, 1981), but in other regions they are scattered to form extended volcanic fields as in Michoacán–Guanajuato (Hasenaka and Carmichael, 1985; Luhr and Carmichael, 1985), Zitácuaro–Valle de Bravo (Blatter and Carmichael, 1998a, 1998b, 2001), Los Tuxtlas (Nelson and González–Caver, 1992), Apan–Tezontepec (García–Palomo etal, 2002b), and Sierra Chichinautzin (Bloomfield, 1974, 1975; Swinamer, 1989; Martin–del Pozzo, 1982; Wallace and Carmichael, 1999; Verma, 1999, 2000; Velasco–Tapia and Verma, 2001a, 2001b; Márquez and De Ignacio, 2002; Cervantes and Wallace, 2003a, 2003b; Martinez–Serrano et al, 2004; Siebe et al., 2004a, 2004b, 2005).

The SCVF is a volcanic area of about 2,400 km² bounded by the Sierra Nevada to the east and by the Nevado de Toluca volcano to the west. Nevado de Toluca volcano has an efficient volcanic plumbing system controlled by the intersection of three important tectonic features: the San Antonio fault system, the Taxco–Querétaro fault system, and the Tenango fault system, which that also feeds the monogenetic lava flows of the western portion of the SCVF (García–Palomo et al, 2000). The SCVF is characterized by more than 200 scattered monogenetic centers, mainly scoria cones with associated lava flows, shield volcanoes, and minor fissural lava flows and domes (Martin–del Pozzo, 1982; Márquez et al, 1999a, 1999b).

The chronology of the SCVF magmatic rocks is poorly known. Only about 8 % of the SCVF products have been dated by ¹⁴C, therefore the age of the beginning of volcanic activity is still unknown (Bloomfield, 1975; García–Palomo et al., 2000a; Siebe et al., 2004a and references therein). This problem limits the accuracy of estimations of the effusion rates at the volcanic front of this part of the Trans–Mexican Volcanic Belt and makes difficult to understand the relationship between monogenetic activity and the older volcanic products.

In the western portion of the SCVF, in the vicinity of the Tenango village, the products of monogenetic activity are interbedded with pyroclastic deposits of the Nevado de Toluca volcano, such as the 10.5 ka Upper Toluca Pumice (UTP; Figure 1e; Arce et al, 2003; García–Palomo et al, 2002a). A few geochronological data of these products provide ages between 38.6 and 19.5 ka for the ancient cones (pre–UTP phase: Tezontle, Pehualtepec, Chapultepec, Villa Metepec, Volcán Emerenciano, La Silva, Tomasquillo, Volcán Negro, Volcán Cuautl, Volcán La Mesa, Los Cuates–Capulhuac system, Lama dome and La Esperanza lava flow) and around 8.5 ka for Tenango, Tres Cruces–Holotepec, Tepexingo, Texontepec and Lagunilla lava flows (post–UTP phase; Bloomfield, 1974, 1975; Meriggi, 1999; García–Palomo et al, 2000).

Previous works (e.g., Wallace and Carmichael, 1999 and Verma, 2000) showed that the mafic SCVF rocks are characterized by chemical heterogeneity and include products with both calc–alkaline and OIB–type affinity, whose origin is still under debate. For the aim of this work, we use the Tezoyuca cinder cone as the primitive end–member of the OIB–type magmatic series, and the Pelagatos cinder cone as representative of the low(L)–TiO₂ series, in agreement with Márquez and De Ignacio (2002) (Figure 1b).

 

ANALYTICAL TECHNIQUES

Forty one samples were analyzed for major and trace elements at the Dipartimento di Scienze della Terra of the Universitá degli Studi di Firenze (Italy) by X–Ray Fluorescence (XRF) with a Philips PW 1480 spectrometer using the Franzini et al. (1972) method, along with several trace elements. International reference samples and internal standards were used to evaluate accuracy and precision. The uncertainty for trace elements was estimated to be less than 10% for Y, Nd, Ba, Nb, and Cr, and less than 5% for all other trace elements. MgO, K₂O and Na₂O contents were determined by Atomic Absorption Spectrometry (AAS). FeO was determined by titration following Shapiro and Brannock (1962), and lost on ignition (LOI) by the gravimetric method.

Nineteen samples (d–10, d–25, d–37, d–42, d–45, d–47, d–50, d–51, d–53, d–54, d–56, TEB, ScO2, ScO5, ScO8, ScO9, Mxl4, XTN and L2) were analyzed for major, trace and REE elements by Inductively Coupled Plasma Emission Spectrometry (ICP–ES) and Instrumental Neutron Activation Analysis (INAA) at Activation Laboratories, Ancaster, Canada. The analytical error was less than 0.01% for major and trace elements (Ba, Cr, Cu, Ni, Sr, Ta, V Y, Zn); less than 1 ppm for Zr; 0.5 ppm for Cs, Hf, Tb, U; and 20 ppm for Rb. The detection limit for Sm, Eu, and Yb was 0.1 ppm.

Mineral chemistry was detrmined at the C.N.R., Istituto di Geoscienze e Georisorse of Firenze (Italy) by using a JEOL JXA 8600 automated microprobe using 15–kV accelerating voltage and 10–nAbeam current with variable counting times. Matrix correction was performed using the Bence and Albee (1968) and Albee and Ray (1970) method. Analytical errors are similar to those reported by Vaggelli etal (1999).

Sr and Nd isotope analyses were performed at the Dipartimento di Scienze della Terra of Firenze (Italy) using a Thermo Finnigan Triton–Ti thermal ionization mass spectrometer equipped with nine movable collectors (Avanzinelli et al, 2005). Sample powder (100–150 mg) was dissolved in a HF–HNO₃–HC1 mixture. Sr and Nd fractions were separated at the LUGIS laboratory of Instituto de Geofísica and Instituto de Geología, UNAM, Mexico City (Mexico) following standard chromatographic techniques using AG50W–X12 and PTFE–HDEHP resins with HC1 as solvent. The total procedural blank was <5 ng for Sr and <2 ng for Nd, making blank correction negligible. Sr and Nd isotope compositions were measured in dynamic mode and are reported normalized to ⁸⁶Sr/⁸⁸Sr = 0.1194 and ¹⁴⁶Nd/¹⁴⁴Nd = 0.7219, respectively. Exponential–law mass fraction–ation correction was used for all Sr and Nd isotopic data. Uncertainties in measured (m) isotopic ratios refer to the least significant digits and represent ±2a in–run precision. The external precision of NIST SRM987 was ⁸⁷Sr/⁸⁶Sr = 0.710251 ± 10 (2σ, n = 39), and that of the La Jolla standard was ¹⁴³Nd/¹⁴⁴Nd = 0.511845 ± 4 (2σ, n = 11).

 

PETROGRAPHY OF LAVAS AND XENOLITHS

Modal abundance of 12 representative samples was determined with the point counting method. Phenocrysts (Ph) are defined as crystals >0.3 mm, microphenocrysts (MPh), those between 0.3 and 0.03 mm, and groundmass (glass and microliths) those phases less than 0.03 mm. In the following sections we describe these rocks in groups defined by MgO contents and crustal xenoliths. Generally mafic samples are porphyritic with abundant pheno– and microphenocrystals of olivine and less abundant pyroxene (clinopyroxene>orthopyroxene). In more evolved rocks olivine is progressively substituted by orthopyroxene and xenocrysts/xenoliths of foreign provenance are fairly common. These mineral associations are similar to those described by Márquez and De Ignacio (2002); representative modal analyses of mafic to evolved samples are reported in Table A1 in the electronic supplement.

 

Mafic magmas (MgO >6.0)

Mafic rocks (e.g., Los Cuates–Capulhuac system) have a porphyritic index (PL) between 10–15 vol. % with abundant phenocrysts of euhedral olivine, dotted by Mg–chromite inclusions (rarely partially altered to iddingsite) ± clinopyroxene (Table A1). The same mineral phases appear in the groundmass along with microphenocrysts of plagio–clase, opaque minerals and abundant clear to brown glass.

Glomeroporphyritic aggregates of olivine + clinopyroxene are relatively abundant. These rocks contain rare quartz–bearing xenoliths or, when disaggregated, isolate quartz xenocrysts surrounded by clinopyroxene coronas, whereas orthopyroxene coronas are found around olivine phenocrysts. Scoria from the Sta. Cruz cinder cone (samples Mxll and d–10) represents an exception among mafic magmas due to the absence of olivine as aphenocrystphase. Euhedral clinopyroxene is the only phenocryst observed, and is embedded in a groundmass composed of microcrystals of pyroxene, apatite, glass and rare clinopyroxene glomeroporphyritic assemblages. As in other pre–UTP samples, plagioclase is observed only as microliths in the groundmass.

 

Intermediate to felsic magmas (MgO <6.0 wt %)

Intermediate rocks constitute an isolated cinder cone (e.g., Chapultepec) and thick lava flows (Tenango, Tepexingo, Lagunilla) or small shield volcanoes (Tres Cruces/Holotepec) (Figure 1c). These rocks are characterized by the highest porphyritic index (P.I.) <15 vol. %, with sparse phenocrysts and microphenocrysts of olivine, generally without spinel inclusions, orthopyroxene and clinopyroxene microphenocrysts. The groundmass consists of glass and abundant microliths of plagioclase and opaque minerals arranged intrachytic textures. These lavas are also characterized by abundant xenocrysts of deeply resorbed, centimeter–sized plagioclase with sieve texture and thin overgrowths, ghosts of relict hornblende, clinopyroxene–rimmed quartz and almost totally resorbed subcentimetric clinopyroxene.

Felsic rocks (e.g., La Esperanza lava flow) have aphyric textures (P.I. <5 vol. %) with sparse microphenocrysts of orthopyroxene set in a felsic microcrystalline groundmass made of thin laths of plagioclase.

 

Crustal xenoliths

The Lama dome and Tenango lavas host two types of xenoliths of heterogeneous size and provenance. The first type consists of centimetric–sized green conglomerates common in the southernmost part of the Tenango andesite (sample XTN). In thin section they show a clastic texture made of sub–angular grains (<0.3 mm) constituted by feldspar, pyroxene, calcite, and dolomite set in a groundmass of chlorite, calcite and sparce epidote.

The second type consists of light–gray centimetric–sized quartz–diorites, common in the Lama dome. These xenoliths have ovoidal shapes surrounded by thin (0.5 mm) dark rims in contact with the host lava. They show coarse equigranular texture with disequilibrium features, especially close to the contact with the host magmas. They are constituted by clinopyroxene, anhedral quartz (<1 cm in length) with undulate extinction and annealing texture, zoned and twinned plagioclase with accessory zircon, mafic phases (biotite?) completely substituted by fine aggregates of spinel and hercynite, and abundant rhyolitic glass with variable amounts of K₂O. Minor ilmenite, sillimanite and rare titanite are present too, as revealed by electron micro–probe analysis. The petrographic and chemical characteristics of these xenoliths are similar to the dioritic intrusive body of the Guerrero Terrane described by De Cserna et al. (1974).

 

MINERAL CHEMISTRY

Olivine. Crystals observed in rocks from the western SCVF are Fo_87–81 with euhedral and rarer skeletal habits. They are slightly normally zoned (3–10 Fo mol. %; Table A2 in the electronic supplement). More fayalitic olivine (Fo_79–65) occurs in the groundmass as microphenocrysts. No evident differences exist in the major element composition of the analyzed olivine crystals, but the Tenango lava phenocrysts are always rimmed by thin laths (<5 µm) of orthopyroxene.

Equilibrium between melt and olivine was tested by plotting the whole–rock Mg# vs. Fo content of olivine (Figure 2). The exchange distribution coefficient (K_D = [X_FeO/X_MgO]^Olivine[X_FeO/X_MgO]^Liquid) following Toplis (2005) yield values of 0.36–0.38, in agreement with previous works (e.g., Wallace and Carmichael, 1999). As shown in Figure 2, olivine phenocryst cores straddle the equilibrium line whereas phenocryst rims and groundmass crystals are Fo–poor and fall slightly above the line, suggesting late crystallization.

Clinopyroxene. This is the second most abundant phase in the mafic rocks (Table A3 in the electronic supplement.). Clinopyroxene phenocrysts show fairly constant compositions with En_42–52Wo_35–42 (Figure 3) and are usually normally zoned up to 10 mol. % in En. In intermediate to evolved lavas as the Tenango andesite, clinopyroxene microcrysts are also present as rims around quartz xenocrysts and show similar En contents but lower A1₂O₃ (Table A3).

Rare unstable clinopyroxene phenocrysts occur in the crustal xenoliths collected at the Lama dome, which have constant compositions of En_42–36Wo_38–41, variable A1₂O₃ contents (0.7–2.2 wt.%), and low Cr₂O₃.

Phenocrysts of clinopyroxene also occur in the Sta. Cruz cinder cone with cores of constant composition (En_49–40Wo_42–46) and strong normal zoned rims up to 20% in enstatite.

Orthopyroxene. This mineral phase is not common in magmas of the western SCVF, and only a few phenocrysts are observed. It commonly appears as microphenocrysts or as rims in olivine phenocrysts, in particular in intermediate to evolved samples with remarkably constant compositions (En_84–62) and normal zoning of up to 24 % in enstatite (Figure 3 and Table A3). In the crustal xenoliths of the Lama dome and Tenango lavas, orthopyroxene is less enriched in MgO (En_66–55) and have higher values of A1₂O₃ (up to 7.83 wt.%) and FeO, but with very low Cr₂O₃.

Hornblende. The Tenango lava flows and the Lama dome show a widespread presence of ghosts of euhedral hornblende (up to 0.5 mm) totally replaced by minute oxide aggregates unsuitable for microprobe analysis. Therefore, it is difficult to interpret their origin (e.g., phenocrysts vs. xenocrysts), although tschermakitic as well as Mg–hastingsitic hornblende have been reported in the central and eastern portion of the SCVF by Velasco–Tapia (2002).

Plagioclase. One of the main features of SCVF rocks is the absence of plagioclase phenocrysts although it represents the main mineral phase in the groundmass. Most plagioclase has labradoritic core compositions (Table A4 in the electronic supplement, and Figure 4). Few grains are large enough for multiple analyses with the electron microprobe and show a slight normal zoning with compositions between An₆₄ and An₅₀. Millimeter to centimeter–long plagioclase crystals (up to 1.5 cm in diameter) observed in the Tenango lava and Lama dome show thick sieve–textured rims, cores with lower CaO contents (An_42–29), and thin (2 µm) unresorbed overgrowths with anorthite contents similar to those of the groundmass laths (Table A4 and Figure 4).

Oxides. Opaque phases are common in the primitive products of the pre–UTP rocks (e.g., Los Cuates–Capulhuac system; Figure 1c) and also are observed in few intermediate rocks (e.g., Tepexingo). They are Mg–chromites and less abundant spinels, with variable Cr# (0.45–0.68), whereas spinels, Ti–magnetite, and ilmenites are common in the groundmass of all analyzed lavas. The xenoliths from the Lama dome contain abundant sub–idiomorphic spinels and hercynite that are interpreted as the result of reaction of ancient mafic phases (Table A5 in the electronic supplement.).

 

WHOLE ROCK CHEMISTRY

We have analyzed 60 samples of lava flows, scoriae, domes, and two crustal xenoliths (Table A6 in the electronic supplement.). Several authors (e.g., Wallace and Carmichael, 1999; Siebe etal. 2004b; Schaaf et al, 2005) described the presence of alkaline magmas in the SCVF by using the MacDonald and Katsura (1964) line. However, by using the Irvine and Baragar (1971) line it is clear that most samples have a sub–alkaline affinity (Figure 5) and only a few samples have a mild alkaline affinity (also enriched in HFSE and other incompatible elements). Tezoyuca (d–37) and Pelagatos (d–25) cinder cone rocks were included in this study for references purposes (Table A6), because they were considered as representative of the cale–alkaline and OIB–like magmatic series of the SCVF (Márquez and De Ignacio, 2002).

Intermediate to evolved samples of the SCVF have similar chemical characteristics, however, mafic samples with MgO >6.0 wt.% are more heterogeneous. By using their HFSE contents it is possible to discriminate between a high(H)–TiO₂, and a low(L)–TiO₂ magma series, as well as a few transitional products (Figure 6). In this Figure, most of the mafic samples from western Sierra Chichinautzin display a H–TiO₂ to transitional affinity, although they do not extend to the highest H–TiO₂ contents found elsewhere in the SCVF. In the total alkali versus silica diagram of Figure 5 the analyzed samples are in good agreement with previous works following a linear trend from basalts (Los Cuates–Capulhuac system, 52.3 – 53.5 wt.% SiO₂) to dacites (La Esperanza, 60.3–66.0 wt.% SiO₂). The western SCVF magmas follow the typical calc–alkaline trend on the AFM diagram (although this kind of diagram should be used with caution, Sheth et al., 2002) and plot in the medium–K field of the K₂O versus silica diagram of Peccerillo and Taylor (1976) of Figure 7. All but two samples are hy–normative according to the CIPW calculation (Table A6). Moreover, as noticed by Wallace and Carmichael (1999), an important feature of the studied rocks is their high concentration of MgO at given silica contents. For instance, andesites of the SCVF have MgO contents of 5.39 – 9.38 wt.%, higher than typical values of cale–alkaline andesites (e.g., <4.4 wt.%, Gill, 1981; Wilson, 1989). These high–MgO andesites are relatively uncommon but they have been found at subduction–related environments (e.g., Shimoda et al., 1998; Tatsumi, 2001).

The Santa Cruz cinder cone is anomalous in composition as compared to other samples from the SCVF. It has higher K₂O contents that plot in the shoshonitic field of Figure 7. Although Wallace and Carmichael (1999) previously reported high–potassium magmas in the western SCVF (e.g., Cerro el Perico near the city of Toluca, Figure 7), the Santa Cruz cone is the first shoshonitic cone found in central Mexico.

Incompatible element pattern diagrams of representative mafic magmas (MgO >6.0 wt.%) of the transitional and L–TiO₂ series of the western SCVF and the Sta. Cruz cinder cone are shown in Figure 8a. The Sta. Cruz cinder cone shows anomalous enrichments in almost all incompatible elements. The other magmas from the Tenango area display similar patterns with clear troughs at Ta, Nb and Ti, and positive anomalies of Ba, Pb and Sr. All these characteristics are also observed in the multielement diagrams of Figure 8b, that shows the Pelagatos cinder cone and other subduction–related mafic magmas from different sectors of the Trans–Mexican Volcanic Belt (e.g., Cerro Colorado, Siebert and Carrasco–Núñez, 2005; and mono–genetic products from Mascota, Carmichael et al., 1996), as well as in the Stromboli and Alicudi magmas from the Aeolian Arc, Italy (Francalanci et al., 1993). As shown in Figure 8c, similar enrichments in Ba, Pb and Sr appear also in the multielement diagrams of the so–called OIB magmas from Garibaldi Volcanic Belt (northern Cascadia; Green, 2005) and the H–TiO₂ magmas of the SCVF (Tezoyuca and Tepetlapa cinder cones). However, it is worth mentioning that such characteristics are absent in the multielement diagrams of typical OIB magmas as those from Galapagos Islands (Reynolds and Geist, 1995) and Tubuai island (Chauvel et al., 1992).

The REE distribution in mafic samples of the Tenango area show similar patterns with slight enrichments in light REE [(La/Lu)_N = 7.0–10.0] and nearly flat heavy REE alignments. The Sta. Cruz cone shows higher values for the light to medium REE, whereas Tm, Yb and Lu abundances are comparable to those of the other samples (Figure 9).

 

Sr and Nd isotopes

Isotopic data for the H–MgO SCVF samples are sparse and only a few rocks have been studied in some detail. New (Table 1) and previously reported data show that mafic magmas (MgO >6.0 wt%) belonging to the H– and L–TiO₂ series show very similar ¹⁴³Nd/¹⁴⁴Nd ratios (0.51274–0.51298), but greater differences can be found in the ⁸⁷Sr/⁸⁶Sr ratio (Figure 10), although some overlap between samples from different series exist. Particularly, most mafic L–TiO₂ rocks gather in the right side of the mantle array due to their enrichment in radiogenic Sr (⁸⁷Sr/⁸⁶Sr >0.7041), with respect to the H–TiO₂ mafic rocks (Figure 10). The high K₂O rocks of Sta. Cruz cinder cone (sample d–10, MgO = 5.33 wt.%) show even a stronger enrichment in radiogenic Sr, with ⁸⁷Sr/⁸⁶Sr ratios falling outside of the mantle array of Figure 10. The xenoliths L2 and XTN (Table A6) fall inside the mantle array as well as the high–SiO₂ andesites and dacites from nearby stratovolcanoes of Nevado de Toluca and Popocatepetl (Figure 10b).

 

DISCUSSION

Magma genesis

The bulk rock composition of the mafic SCVF magmas is characterized by important variations in TiO₂ and HFSE represented by rocks belonging to three magmatic series: L–TiO₂, intermediate–TiO₂, and H–TiO₂ (Figure 6). These chemical variations are also observed in the composition of spinels hosted in olivine phenocrysts at given Fo contents (Figure 11). If the Cr# is used, it is clear that the spinels of Pelagatos cinder cone (L–TiO₂ series) have higher values than the spinels from Tezoyuca cinder cone (H–TiO₂ series). Following Arai (1994) such Cr# variations should reflect the presence of important heterogeneities in the mantle source, suggesting the existence of a more depleted source for the L–TiO₂ with respect to the H–TiO₂ magmas. The unusual high TiO₂ concentrations found in SCVF rocks encouraged some authors to propose that SCVF magmas were not related to the subduction of the Cocos plate beneath Mexico. In fact, Márquez et al. (1999a, 1999b) and Márquez and De Ignacio (2002) proposed the upwelling of a deep–seated mantle plume in central Mexico capable of generating OIB–like magmas, whereas Verma (2000, 2002) proposed the presence of a passive rift and the generation of magma through decompression melting of an unmetasomatized mantle wedge. On the contrary, other authors reconciled the presence of SCVF enriched magmas through subduction of the Cocos slab causing the advection of enriched mantle portions from the back–arc mantle (Wallace and Carmichael, 1999), or the presence of a slab window able to induce a deep mantle flow into the wedge region (Ferrari, 2004).

By using the trace element and Sr–Nd isotopic data of the mafic products of western SCVF (Pelagatos and Tezoyuca cinder cones) some alternative considerations can be made to explain these chemical features of the mantle source beneath Central Mexico. The multielement diagram of Figure 8a shows that the mafic L–TiO₂ and shoshonitic magmas from Sta. Cruz cinder cone are characterized by clear negative anomalies of HFSE such as Nb, Ta and Ti. These patterns suggest the occurrence of subduction–related metasomatic processes beneath SCVF, weakening the hypothesis of a rift–related magma genesis.

On the other hand, the hypothesis of a mantle plume to explain the OIB–like signature of SCVF rocks can be tested by using the trace element patterns and Sr–Nd isotopic ratios of H–TiO₂ products. Zindler and Hart (1986) concluded that the genesis of OIB magmas could be modeled by the interaction (e.g., mixing) between variable amounts of a depleted mantle (DM; ¹⁴³Nd/¹⁴⁴Nd –0.5132; ⁸⁷Sr/⁸⁶Sr –0.702) and one (or more) end–members like a HIMU source (high µ, where µ = ²³⁸U/²⁰⁴Pb), markedly enriched in U, Th and HFSE, or the Enriched Mantle (EM) characterized by low ¹⁴³Nd/¹⁴⁴Nd values (<0.5124) and high ⁸⁷Sr/⁸⁶Srvalues (0.705 for EMI and >0.707 forEM2 types) (Figure 10a). Although the lower values of ⁸⁷Sr/⁸⁶Srof most mafic rocks belonging to the H–TiO₂ series could be taken as an evidence of HIMU component in the mantle source, several evidences argue against it. First of all, by comparing the incompatible elements of H–TiO₂ rocks (Tezoyuca cinder cone) with a typical HIMU magma as the Tubuai Island basalts (Chauvel et al, 1992) (Figure 8c), dramatic differences are found in Th, U, K, Ta, Nb, La, Ce, and Pb contents. Moreover, Cervantes and Wallace (2003a) found high H₂O contents (3.2 wt.%) in olivine glass inclusions of the H–TiO₂, high–Nb rocks of Tepetlapa (central SCVF; Figure 8c), characteristic absent in typical HIMU magmas (e.g., Nadeau et al, 1993; Dixon et al, 2002; Workman et al, 2006). Finally, although only few lead isotope data are available for the less evolved magmas of the SCVF, they show no differences between H–TiO₂ and L–TiO₂ series, and the values found (²⁰⁶Pb/²⁰⁴Pb=18.651–18.803; ²⁰⁷Pb/²⁰⁴Pb= 15.570–15.643 and ^20SPb/²⁰⁴Pb=38.426–38.656) are far from those expected in HIMU end members (²⁰⁶Pb/²⁰⁴Pb >21; ²⁰⁷Pb/²⁰⁴Pb >15.8 and ^20SPb/²⁰⁴Pb >40.5, Chauvel et al, 1992). Therefore, we argue against the occurrence of a HIMU contribution (e.g., for mixing at mantle level) in the Mexican mantle wedge. On the other hand, the negligible variations of ¹⁴³Nd/¹⁴⁴Nd ratios of mafic rocks of the SCVF (Figure 10a) suggest that these magmas might not be linked neither to an EM component at their source. In short, the occurrence of a mantle plume below central Mexico is also poorly supported by the available data.

At this point, it seems more plausible that the genesis of SCVF magmas is linked to the subduction of the Cocos plate beneath Mexico. Therefore, any new model should be able to explain the different enrichments in TiO₂ and other HFSE found in the area. Although these elements are considered immobile in aqueous fluids arising from the slab (e.g., Kogiso etal, 1997), many authors suggest that water–rich silicate melts from the subducted sediments and/or slab, could be an efficient medium to transport such conservative elements into the mantle wedge (e.g., Kepezhinskas et al, 1997; Walker et al, 2001; Green, 2005). In this context, the downward warping of the Cocos plate beneath central Mexico inferred by Pardo and Suárez (1995) and Manea et al. (2004) could induce a rapid heating of the slab, leading to important consequences for magma genesis in central Mexico. In particular, phase relations studies of Pawley and Holloway (1993) and Kessel et al. (2005) indicate that at high temperature, an eclogitic slab could generate fluxes of H₂O–SiO₂bearing fluids/melts able to transport high contents of incompatible elements such as LILEorHFSE through the mantle wedge. These fluids/melts are not only able to induce partial melting of the mantle peridotite, but may hydrate it with the consequent fractionation of mineral phases such as amphibole and/or micas as disseminated crystals or in centimeter– to meter–thick veins (Tatsumi, 1989; Arculus, 1994). Chemical data of amphibole–bearing xenoliths as well as experimental data (Brenan et al, 1995; Ionov and Hofmann, 1995; Tiepolo et al, 2000; 2001) demonstrated that calcic amphiboles such as kaersutite or pargasite as well as phlogopite, may crystallize in mantle conditions and host notable concentrations of LILE and HFSE otherwise highly incompatible in the anhydrous mantle mineralogy. Subsequently, partial melting of such hydrated peridotite could produce low density melts enriched in incompatible elements such as HFSE, REE and alkalis that resemble in composition the OIB and rift–related magmas (Menzies et al, 1987). In this context, the mantle xenoliths described by Blatter and Carmichael (1998b) and Mukasa et al. (2007) hosted in the nearby Quaternary products of Valle de Bravo (60 km west of studied area) are of noteworthy interest. Overall, the heterogeneous mineral assemblage of olivine + pyroxenes + spinel and Cr–pargasite confirms that a hydrous mantle wedge is present beneath central Mexico.

As shown in Figure 12a, 5–15% partial melting of a mantle source constituted by 37% olivine + 40% orthopyroxene + 16% clinopyroxene + 4% spinel + 3% of amphibole (kaersutite in our model), compositionally similar to the xenoliths X–30 and X–33 of Mukasa et al. (2007), is able to generate melts with steep REE patterns as those observed in the H–TiO₂ mafic magmas. To obtain the less fractionated pattern of the L–TiO₂ mafic magmas, the model needs lower degrees of partial melting (1–5%) of a depleted mantle similar to that proposed by Mukasa et al. (2007) and constituted by 33% olivine + 45% orthopyroxene + 19% clinopyroxene + 3% spinel (Figure 12b). However, this doesn't imply that hybrid mantle source portions could not exist beneath the SCVF. In fact, by using the two end–members mixing formula of Bryan et al. (1969) it was possible to reproduce most of the hygromagmatophile element contents found in the L–TiO₂, H–TiO₂ and transitional series of the mafic magmas SCVF (Figure 13). The existence of a hybrid mantle source is also supported by the differences found in spinel composition (Figure 11), and bulk rock analyses (Figure 6).

The genesis of Sta. Cruz magmas merits careful attention because of its special composition: an extremely high LILE/HFSE ratio with respect to nearby lavas (e.g., (Ba/Nb)_N ~10 times higher than samples from Los Cuates–Capulhuac complex), enrichment in K₂O, light REE, P₂O₅ and other incompatible trace elements, and high ⁸⁷Sr/⁸⁶Sr ratio. These characteristics suggest a stronger contribution of fluids or melts from the altered slab (e.g., De Paolo and Wasserburg, 1977). The chemical composition of Sta. Cruz rocks is similar to the lamprophyric magmas described by Luhr (1997) and Luhr et al. (1989) in western Mexico, which were interpreted as being formed by partial melting in the mantle wedge of phlogopite–bearing veins, generated by the interaction of hydrous melts with the peridotitic wall rock.

 

Magmatic evolution

The eruptive centers of the S VCF are scattered over an area of 2,400 km². Each vent represents a different magmatic source undergoing unique differentiation processes at crustal levels. Notwithstanding these considerations, a general crystallization history can be depicted by using the chemical composition and the isotopic ratios of the studied rocks.

Because the H–TiO₂ and L–TiO₂ series of the SCVF may be generated by different contributions from the slab, and because H₂O has significant effects during mantle melting processes influencing the SiO₂ contents of the mantle derived magmas (e.g., Kushiro, 1972; 1990; Hirose, 1997; Gaetani and Grove, 2003; Parmanand Grove, 2004), MgO was chosen as differentiation index in most chemical variation diagrams of Figures 14 and 15. Although MgO contents of L– and H–TiO₂ series of SCVF are comparable, the former series shows lower values of TiO₂, alkalis, and HFSE, whereas it appears slightly enriched in SiO₂, Al₂O₃/CaO and compatible elements such as Cr. On the other hand, the two series do not present significant differences in LILE concentrations (not shown).

In order to test the fractional crystallization process of the western SCVF magmas, we used the thermodynamic model MELTS of Ghiorso and Sack (1995) for major element composition. Samples Mx40 (H–TiO₂ series) and d–25 (L–TiO₂ series) were proposed as mafic end–members (Table A6, Figure 14a). By fixing the crystallization pressure between 8 and 1.5 kbar with H₂O contents of 3.5–5 wt.%, MELTS suggests the occurrence of olivine (Fo₈₆) + spinel as near liquidus phases at temperatures of 1,200–1,250 °C. Proceeding with the magmatic evolution at MgO contents of 4.5–5 wt.%, clinopyroxene (Di₅₃) appears in the melt, while olivine is progressively substituted by orthopyroxene (En₉₀). Labradoritic plagioclase and ilmenite appear later, at MgO concentrations of 4 wt.% or less. The good correlation between the MELTS calculation and the compositions of the mineral phases found in thin section, supports the fact that crystal fractionation is the main process occurring in western SCVF magmas. Moreover, MELTS calculates successfully several variations in the major element concentrations observed in the western Sierra Chichinautzin rocks (Figure 14a–c). In particular, the occurrence of Ti–magnetite at high temperature is able to drop the TiO₂ contents of the liquid from 1.52 wt.% to less than 1 wt.% after a fractionation of 7–8 wt.% of this mineral. One exception is represented by the quasi–compatible behavior shown by Zr in some mafic magmas, because its low partition coefficient values should produce an opposite trend. Nevertheless, the experimental work of Nielsen et al. (1994) indicate that the partition coefficients of Zr and other HFSE are far from being constant in magmatic systems and are probably correlated with the partition coefficients of Ti reaching values of >2 in Ti–magnetite. Therefore, the presence of Ti–bearing opaque phases during the early stages of crystallization could explain the compatible behavior of Ti and Zr.

However, the analyzed rocks show compositional characteristics that are difficult to explain with the occurrence of fractional crystallization as the sole mechanism. In particular, the SiO₂ increment is steeper with respect to values calculated by the MELTS algorithm (Figure 14d) and the fractionation of 01 + Px ± Ox ± Pig does not seem to be capable of varying significantly the ratios of incompatible elements such as Rb/Sr or La/Yb (Figure 15c–d).

Although high magma supply rates from the mantle can produce well–sustained conduits that would avoid important contributions of surrounding crustal rocks (e.g., Hansen and Nielsen, 1999), the inverse correlation between ⁸⁷Sr/⁸⁶Sr ratios and MgO suggests crustal contributions during the evolution of the Sierra Chichinautzin magmas (Figure 16). On the other hand, Figures 14, 15 and 16 indicate that the crustal xenoliths found in Tenango lava and Lama dome are not suitable candidates for contaminant of the western Sierra Chichinautzin magmas because of their low Rb contents, and LREE/HREE and ⁸⁷Sr/⁸⁶Sr ratios.

Verma (1999) suggested that high grade partial melting (50%) of a granulitic lower crust would be able to generate magmas with isotopic and REE compositions broadly similar to the dacitic rocks of the Sierra Chichinuatzin. However, lower crustal material is characterized by low concentrations of Rb (<30 ppm), Th (<5 ppm), La (<11 ppm) and low values of Th/Yb (<2), Rb/Sr (<0.1), Rb/Ba (<0.1), La/Yb (0.1) and Nd/Sm (<4) (e.g., Taylor and McLennan, 1985; Schaaf et al, 1994). Therefore, the higher values shown by the Sierra Chichinautzin magmas point to an upper, instead of a lower, crustal end–member (e.g., Figure 17). Nevertheless, one more thing need to be addressed: What kind of crust is required to generate only small changes in REE concentration as well as in ⁸⁷Sr/⁸⁶Sr values during the magmatic evolution (Figures 16, 17 and 18)? Although the nature of the crust beneath the Sierra Chichinautzin is poorly constrained, and therefore more exhaustive studies are needed, the granodioritic xenoliths found by Schaaf et al. (2005) in the nearby Popocatepetl volcano deposits, fulfill many of these requirements and consequently may represent possible contaminants of ascending magmas in central Mexico (Figure 18).

 

CONCLUSIONS

The Quaternary mafic magmatism of SCVF is characterized by important heterogeneities, such as the variable HFSE enrichments, that triggered the debate on the role of the subducting slab in the magma genesis of the entire Trans–Mexican Volcanic Belt and arc volcanism in general. In fact, although the L–TiO₂ series and the high K₂O rocks (Sta. Cruz cinder cone) are easily interpreted with a classical subduction model (e.g., Gill, 1981), the presence of mafic H–TiO₂ magmas would not fit the models for such a geo–dynamic setting. However, recent experimental data on the behavior of HFSE in hydrated mantle paragenesis reconciled such HFSE enriched compositions with magma generation processes in convergent margins. Hence, partial melting of a heterogeneous amphibole–bearing mantle seems to explain the whole rock composition range observed in the western SCVF. Finally, chemical and isotopic data suggest that fractional crystallization and crustal contamination are the main evolution processes in the studied area.

 

ACKNOWLEDGEMENTS

The authors wish to thank John Eichelberger, Peter Schaaf, Yuri Taran, Christopher Nye and Simon Hughes for stirring and focusing discussions; Gabriela Solís, Luisa Guarnieri, Riccardo Avanzinelli, and Elena Boari for their help during isotope analysis; Gloria Vaggelli and Filippo Olmi () for allowing access to microprobe facilities; Lilia Arana for the field work, and S. Verma for the valuable and insightful comments, as well as editorial handling. The reviews by A. Márquez and P. Wallace helped substantially to clear up ideas of this manuscript. This work is part of the Master Thesis of the senior author, which was partly supported by CNR bilateral grant (bando # 203.05.23) issued to Lorenzo Meriggi. This work was supported by CONACYT grant 47226 to J.L. Macías.

 

APPENDIX A. SUPPLEMENTARY DATA

Tables A1–A6 can be found at the journal web site <http://satori.geociencias.unam.mx/>, in the table of contents of this issue (electronic supplement 25–2–01).

 

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