| Título: | Petrography and geochemistry of the magnesites and dolostones of the EdiacaranIbor Group (635 to 542 Ma), Western Spain: Evidences of their hydrothermal origin |
| Autores: | Herrero Fernández, María Josefa ; Martín Pérez, Andrea ; Alonso-Zarza, Ana María ; Gil Peña, Inmaculada ; Meléndez Hevia, Alfonso ; Martín García, Rebeca |
| Tipo de documento: | texto impreso |
| Editorial: | Elsevier, 2011 |
| Dimensiones: | application/pdf |
| Nota general: | info:eu-repo/semantics/openAccess |
| Idiomas: | |
| Palabras clave: | Estado = Publicado , Materia = Ciencias: Geología: Petrología , Tipo = Artículo |
| Resumen: |
The 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 ?18O values ranging from +15.45 to +17.51‰ (SMOW) and ?13C 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 ?13C 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. |
| En línea: | https://eprints.ucm.es/id/eprint/19963/1/Herreroetal_01.pdf |
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