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Clay Diagenesis and Low-Grade Metamorphism of Tithonian and Berriasian Sediments in the Cameros Basin (Spain)

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Clay Diagenesis and Low-Grade Metamorphism of Tithonian and Berriasian Sediments in the Cameros Basin (Spain) View metadata, citation and similar papers at core.ac.uk brought to you by CORE provided by EPrints Complutense Clay Minerals (2001) 36, 325–333 Clay diagenesis and low-grade metamorphism of Tithonian and Berriasian sediments in the Cameros Basin (Spain) J. F. BARRENECHEA1,*, M. RODAS1 ,M.FREY2 , J. ALONSO-AZCA´ RATE3 4 AND J. R. MAS 1 Departamento de Cristalografı´a y Mineralogı´a, Universidad Complutense de Madrid, 28040 Madrid, Spain, 2 Mineralogisch-Petrographisches Institut, Basel University, CH 4056 Basel, Switzerland (deceased), 3 Facultad de Ciencias del Medio Ambiente, Universidad de Castilla-La Mancha, Fa´brica de Armas, 45071 Toledo, Spain, and 4 Departamento de Estratigrafı´a, Universidad Complutense de Madrid, 28040 Madrid, Spain (Received 29 February 2000; revised 13 October 2000) ABSTRACT: The clay mineral assemblages of the Tithonian and Berriasian sediments (Tera and Oncala Groups) in the eastern part of the Cameros basin are investigated at seven localities. The lowest-grade assemblage, located on the southern border of the basin, contains calcite + quartz + hematite + kaolinite + mixed-layer illite-smectite (R = 1, 65À85% illite layers) + discrete illite (IC = 0.5À0.65D82y). Systematic increases in the illite and chlorite crystallinities suggest increasing metamorphic grade from the northwest part of the basin to the southeast. This trend does not follow the pattern previously described for the overlying late Berriasian–early Aptian sediments (Urbio´n and Enciso Groups), which exhibit a higher metamorphic grade. This may result from local variations in sedimentary facies, as well as the circulation of hot migratory fluids. Tertiary compression occurring long after the main metamorphic event is considered to be responsible for the enhanced illite and chlorite crystallinities measured in the SE extreme of the basin. KEYWORDS: diagenesis, low-grade metamorphism, clay minerals, illite crystallinity, chlorite crystallinity. The pattern of low-grade metamorphism displayed calculated a temperature of 3768Cforthe by the sediments in the eastern part of the Cameros metamorphism. These authors suggested that the basin is important in understanding the evolution of circulation of hot migratory fluids was important in the basin. Guiraud & Seguret (1985) defined two the development of the metamorphism of the isometamorphic zones, roughly concentric, and Cameros Basin. This hypothesis is based on: (1) estimated maximum temperature and pressure the age of the main thermal event (Middle to Upper ranges of 420À5208C and 0.5À4 kbar, respectively. Cretaceous), which post-dates the sedimentary They considered the metamorphism to be dynamo- filling of the basin; (2) the close relationship thermal and contemporaneous with the sedimentary between the permeability and porosity of the filling of the basin. rocks, and the pattern of mineral assemblages and Casquet et al. (1992), Barrenechea et al. (1995) illite and chlorite crystallinity; (3) the abnormally and Alonso-Azca´rate et al. (1995) estimated high geothermal gradient; (4) the presence of huge maximum temperature and pressure of ~3408C concentrations of large pyrite crystals with inclu- and 1À1.5 kbar. Alonso-Azca´rate et al. (1999) sions of chloritoid crystals in the Barremian Depositional Sequence at the NE sector of the basin (Alonso-Azca´rate et al., 1999); and (5) the variation in the composition of fluid inclusions * E-mail: [email protected] between different units within a given area # 2001 The Mineralogical Society 326 J. F. Barrenechea et al. (Mantilla Figueroa et al., 1998). Mata et al. (1996) the Tera and Oncala Groups from a series of related the low-grade metamorphic event to the stratigraphic profiles along the eastern sector of the crustal thinning associated with the extensional basin. Special attention is paid to illite and chlorite regime that occurred during the development of the crystallinity data, in order to estimate the degree of basin. diagenesis or low-grade metamorphism in each Most of the studies performed thus far area. Finally, the results are compared with the concerning the distribution of mineral assemblages distribution obtained by previous studies for the and metamorphic conditions (Barrenechea et al., overlying Urbio´n and Enciso Groups. 1995; Alonso-Azca´rate et al., 1995; Mata, 1997) focused on the so called Urbio´n and Enciso Groups GEOLOGICAL SETTING defined by Tischer (1965) and Beuther (1965). However, no specific work has been done on the Figure 1 shows that the stratigraphic profiles mineralogical composition of the underlying Tera studied are distributed along a NWÀSE transect and Oncala Groups. Using fluid-inclusion data from through the eastern sector of the Cameros basin, quartz-calcite veins from the Oncala Group, close to the border between the provinces of Soria Mantilla Figueroa et al. (1998) concluded that the and La Rioja. regional temperatures were probably lower than in The Cameros basin was developed under an the overlying Urbio´n Group, and that the composi- extensional regime during the latest Jurassic–early tion of the fluids was different in both realms. Cretaceous. Its fill constitutes >5000 m of sedi- The aim of this paper is to present the first data ments deposited between the Tithonian and the on the distribution of mineral assemblages and Early Albian. Most of the sediments are continental crystal-chemical parameters of the phyllosilicates in (fluvial and lacustrine) with minor marine inter- LOGROÑO BURGOS Arnedo MOV CER MAT Tarazona ARA AO AE SORIA Aranda de Duero ALM Hercynian Cameros basin fill 1.1to6 Upper Cretaceous basement Depositional Sequences 01020304050km Triassic and Utrillas Fm. Tertiary Jurassic FIG. 1. Geological map of the study area, showing the location of the stratigraphic profiles: Mataseju´n (MAT), Montenegro-Villoslada (MOV), Almajano (ALM), Aguilar del Rı´o Alhama (ARA), east Agreda (AE), west Agreda (AO) and Cervera del Rı´o Alhama (CER). Modified after Guimera´ et al. (1995). Diagenesis and low-grade metamorphism 327 calations. During the Palaeogene and early and limestones with green to grey mudstones and Miocene, the basin was inverted by thrust with a quartzites (interpreted as flood-plain deposits in a displacement of ~30 km over the Tertiary Ebro meandering fluvial system). A progressive increase basin in the north, and a system of thrusts over the in the proportion of marls and limestones with some Almaza´n basin at the southern margin. mudrocks is observed at the top of the profile, According to Mas et al. (1993) the sedimentary where we find grey laminated limestones rich in record constitutes a large megasequence bounded by ostracods and bivalves. two main unconformities at the base and the top Finally, a set of samples collected in different (Tithonian–early Albian), and can be further sub- stratigraphic profiles from the south-eastern extreme divided into six depositional sequences (DS1 to DS6 of the basin were grouped under the denomination in Fig. 1) separated by minor unconformities. The SE sector. The East-Agreda (AE), West-Agreda substratum consists of marine Jurassic (generally (AO), and Aguilar del Rı´o Alhama (ARA) profiles Malm) and very occasionally Triassic sediments. correspond to the Tera Group, whereas the Cervera The Tera and Oncala Groups correspond to the del Rı´o Alhama (CER) section includes sediments Tithonian-Berriasian depositional sequence (DS1), from the Tera and Oncala Groups. The profiles are whereas the Urbio´n and Enciso Groups comprise characterized by alternating limestones, marls and the late Berriasian to early Aptian depositional calcareous breccias, with scarce mudstones and sequences (DS2 to DS5). The unconformable sandstones. contact between the Oncala and the Urbio´n Groups is represented everywhere by a thick bed METHODS of black shales. 100 g samples were ground in a tungsten-carbide swing-mill for 20 s. Carbonate was removed with Sedimentological framework and samples 5% acetic acid. The <2 mm fraction was separated A brief description of the stratigraphic profiles using differential tubes and millipore filters. studied (simplified from Go´mez Ferna´ndez, 1992) is Following Ca-saturation, air-dried oriented aggre- given below, starting from the northwestern to the gates (<2 mm) were prepared by pipetting suspen- southeastern border of the basin. sions (~5 mg/cm2) onto glass slides. These were The Montenegro-Villoslada profile (MOV) solvated with ethylene glycol and in some cases comprises medium-grained sandstones, with were heated to 5508Cfor1h. scarce, thin conglomerate layers, interbedded with X-ray diffraction patterns of non-oriented red, grey and green mudstones. These sediments powders and oriented clay aggregates were were considered by Go´mez Ferna´ndez (1992) as collected in a Siemens D5000 diffractometer, representative of a meandering fluvial system. equipped with a graphite monochromator, using Towards the top of the profile, the amount of Cu-Ka radiation and the Siemens SOCABIM marls and limestones present increases gradually, Diffract AT3.2 Software. together with massive, black, marly layers. The full width at half maximum (FWHM) of the The Almajano profile (ALM) is apparently out of (001) peak of illite and the (002) peak of chlorite (IC the NWÀSE band roughly drawn by the rest of the and ChC, respectively) were determined. In some profiles. These sediments belong to the Tera Group cases the IC values were estimated after using a and represent the beginning of the filling of the deconvolution routine
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