Person: Herrero Fernández, María Josefa
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First Name
María Josefa
Last Name
Herrero Fernández
Affiliation
Universidad Complutense de Madrid
Faculty / Institute
Ciencias Geológicas
Department
Mineralogía y Petrología
Area
Petrología y Geoquímica
Identifiers
3 results
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Item Caracterización petrológica de los niveles magnesíticos y las dolomías encajantes de Edad Proterozoica Superior- Cámbrico Inferior, Grupo Ibor, Castañar de Ibor, Cáceres(Geogaceta, 2010) Herrero Fernández, María Josefa; Martín Pérez, Andrea; Gil Peña, Inmaculada; Alonso Zarza, Ana María; Meléndez Hevia, Alfonso; Martín García, RebecaDetailed petrographic observations of Upper Proterozoic –Lower Cambrian deposits of the Castañar de Ibor allows the characterization of the diagenetic history of these rocks. Graywackes, shales and limestones were deposited during the Upper Proterozoic-Lower Cambrian within a siliciclastic-carbonatic marine platform. Dolomite replaced mostly limestones, but also cemented the siliciclastic deposits. Later on magnesium-rich fluids circulating along stylolites, bedding planes and fractures partially replaced the dolostones and some siliciclastic beds. Finally, a new dolomitisation phase produced replacement of the magnesite by dolomite and dolomite cementation.Item Discriminating between tectonism and climate signatures in palustrine deposits: Lessons from the Miocene of the Teruel Graben, NE Spain(Earth-science reviews, 2012) Alonso Zarza, Ana María; Meléndez Hevia, Alfonso; Martín García, Rebeca; Herrero Fernández, María Josefa; Martín Pérez, AndreaThe Upper Miocene (Vallesian–Turolian) Unit II of the Teruel Graben comprises at its top a 25 m-thick sequence of palustrine deposits. Deposition of the entire unit commenced some 9 to 7 Ma ago in a halfgraben basin. Here, via a recent quarry, we examine in detail the lateral and vertical distribution of Unit II's palustrine facies and their features to determine the palaeogeography and main controls on deposit formation. Our findings suggest the deposits formed at a low-gradient lake margin with different energy levels. These energy levels controlled the type of primary deposit within the lake; wackestone to packstone sediments formed in low-energy conditions, whereas cross-bedded rudstones to floatstones formed under higher energy conditions, by erosion and redeposition of prior lacustrine deposits. Pedogenic and diagenetic modifications of the primary sediments took place during sedimentary discontinuities (SD) when the lacustrine sediments were subaerially exposed. These processes serve to explain the formation of eight different palustrine limestones: limestones with root traces, mottled limestones, brecciated limestones, flat pebble breccias, granular limestones, micro-karstified limestones with laminar calcretes, carbonate mounds and clayey limestones with laminar calcretes. Based on the features and thicknesses of the modified sediments five different morphological stages (I to V) of palustrine carbonates are defined. Stage I is characterized by incipient mottling and brecciation. Stage II shows mottling and strong brecciation that lead to the formation of intraclast breccias, in which the fragments are mostly “in situ”. In Stage III, the primary fabric is totally changed; intraclasts have moved and may have lost their initial morphology. This Stage III may also be characterized by the formation of micro-karst. Stage IV is typified by the presence of coated grains and thin root mats. The chronological data available suggest that the formation of Stage III (lacustrine deposition+palustrine modification) would require about 40,000 yr. Facies and the SD record changes across short horizontal distances, and thus reflect the topography of prior sedimentation/modification events. Small (50 cm) highs with micro-karst have their SD counterparts in lower areas of the lake, in which the SD is indicated by desiccation and mottling. The topographic differences of the micro-karst were filled by intraclastic rudstones sourced by the adjacent carbonate flats. The example examined not only clearly sketches the morphology of ancient palustrine systems or wetlands, it also provides evidence that recycling of previous carbonate deposits played an important role as a sediment source, apart from biogenic or physical–chemical production processes. Our geochemical data indicate LMC (Low Magnesian Calcite) as the main component and Fe contents lower than 1%, except for the mottled areas that are richer in FeO. Stable isotope compositions provide δ18O values close to −6.5‰ VPDB, and more varied δ13C (−3.39 to −6.97‰ PDB). Oxygen and carbon values reveal no covariation and clear trends are lacking. The homogeneity of δ18O values reflects the intense effects of meteoric waters. The deposition of these palustrine limestones took place under suitable semi-arid to sub-humid climates. Climate could also have a role in determining subaerial exposure periods. However, its imprint is not easy to detect neither in the geochemical signals nor in the vertical arrangement of the facies. This could be attributed to climate changes probably occurring over shorter periods than those that can be recorded in this type of sediment, such as the astronomical precession cycles, and suggests the unsuitability of palustrine carbonates for detailed palaeoclimate analyses. Tectonism controlled the location of the main lacustrine depocentre close to the basin's main fault. The activity of this normal fault during the sedimentation of Unit II determined long- and short-term sedimentary sequences. Such sequences are the response to small-scale subsidence pulses followed by the infill of the created accommodation space by shallow lacustrine deposits, which underwent early pedogenic and diagenetic processes after subaerial exposure.Item Petrography and geochemistry of the magnesites and dolostones of the Ediacaran Ibor Group (635 to 542 Ma), Western Spain: Evidences of their hydrothermal origin(Sedimentary Geology, 2011) Herrero Fernández, María Josefa; Martín Pérez, Andrea; Alonso Zarza, Ana María; Gil Peña, Inmaculada; Meléndez Hevia, Alfonso; Martín García, RebecaThe Ediacaran deposits (between 635 and 542 Ma) of the Central Zone of the Iberian Massif consist of alternating siliciclastic and carbonate beds. These carbonates are dolostones and magnesites which are interpreted to have been formed by the replacement of primary peritidal limestones. Through petrographic and geochemical analyses, we recognize different types of dolomites (D1 to D4) and magnesites (M1 and M2). Despite distinct petrographic features of the four types of dolomite, their oxygen and carbon isotopes overlap with δ18O values ranging from +15.45 to +17.51‰ (SMOW) and δ13C from −0.13 to 3.21‰ PDB. Sr isotope values for D1 and D2 range from 0.7028 to 0.7091. Magnesites (M1 and M2) show oxygen values higher than +17.87.0‰, and δ13C values show the same variability as for the dolomites. D3 and D4 oxygen isotope values are between +18.91 and 19.61, and the carbon isotope values range are similar to the other diagenetic phases. Sr isotope values for the magnesites and late dolomites (D3 and D4) are 0.7095 to 0.7104, being higher than those of the D1 and D2 dolomites. D1 is a relatively early dolomite phase formed by the replacement of fine grained peritidal limestones. The coarser crystal size of D2, which shows similar geochemical features as D1, suggests formation by dolomitization of coarser grained limestones. The replacement of D1 and D2 by M1 and M2 advanced along stylolites, fractures and bedding planes. This replacement is interpreted to have occurred by hydrothermal fluids, which is suggested by the presence of talc and forsterite. D3, a coarse dolomite, completely destroyed any previous texture and D4 (dolomite cement) post-dates magnesite formation. Interactions of hydrothermal fluids with the prior carbonates reset the oxygen isotopes of the earlier dolomite. The study of these magnesites and related dolostones may offer new insights into the model of formation of sparry magnesites hosted by mixed siliciclastic–carbonate platform deposits. The establishment of the factors and mechanism that control the diagenetic evolution of these carbonates has a great importance in order to understand and predicts porosity and permeability variations of rocks formed under similar geological conditions.