Publication: ¿Dónde y por qué se producen terremotos en la Península Ibérica?
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2011
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Asociación Española para la Enseñanza de las Ciencias de la Tierra
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La Península Ibérica presenta una sismicidad baja a moderada, causada por fallas activas que se mueven con tasas del orden de 10-2-10-1 mm/año. Las magnitudes potenciales máximas son de entre 6,0 y alrededor de 7,0, y los periodos de recurrencia de los seísmos catastróficos, para cada falla, del orden de 103-104 años. La zona más activa es la Cordillera Bética, donde la convergencia con la placa Africana se acomoda en un gran número de fallas, causantes de varios terremotos históricos de intensidad = X. Destacan los desgarres sinistrorsos NE-SO de Carboneras, Palomares y Alhama de Murcia (terremotos de Vera, 1526, o Lorca, 2011), o fallas inversas como la del Bajo Segura (terremoto de Torrevieja, 1829), fallas extensionales E-O como la de Zafarraya (terremoto de Arenas del Rey, 1884) y NW-SE como la de Baza (terremoto de Baza, 1531). La compresión que se transmite por Iberia a partir de su margen sur reactiva asimismo grandes desgarres en el Macizo Ibérico (fallas de Manteigas-Vilariça-Bragança –con evidencias de paleosismos holocenos superiores a 7,0– y Plasencia). El este peninsular está afectado por la extensión cortical ligada a la extensión (rifting) del surco de Valencia, que activa fallas normales en las Cadenas Costero-Catalanas y Sierras Transversales (fallas del Camp y Amer, esta última causante de los seísmos de Olot, 1427-1428) y en la Cordillera Ibérica centrooriental (fallas de Concud –con evidencias de paleosismos del Pleistoceno superior de magnitud potencial próxima a 6,8–, Teruel o Maestrat), aquí sin terremotos recientes catastróficos. La tectónica activa en el Pirineo se debe a la interacción de la extensión ligada al rift, la compresión intraplaca y los movimientos isostáticos. La mayor sismicidad se da en la vertiente norte de los Pirineos occidentales (Lourdes-Arette) y en el Pirineo central (terremoto de Vielha, 1923, en la falla norte de la Maladeta).
The Iberian Peninsula shows low to moderate seismicity caused by active faults that move at rates of the order of 10-2-10-1 mm/y. Maximum potential magnitudes range from 6.0 to 7.0, and the recurrence periods of the major seisms, for each fault, are of the order of 103-104 years. The Betic chains are the most active zone, where the convergence with the African Plate is accommodated by a high number of faults, responsible for several historic earthquakes with intensity = X. The most conspicuous ones are left-lateral, NE-SW strike-slip faults such as Carboneras, Palomares, Alhama and Bajo Segura faults (seisms of Vera, 1526, Torrevieja, 1829, or Lorca, 2011) and E-W extensional faults such as Zafarraya (Arenas del Rey earthquake, 1884). The compression propagated through Iberia from its southern margin also reactivates large strike-slip faults at the Iberian Massif (Manteigas-Vilariça-Bragança –with evidence of Holocene paleoseisms over M = 7.0– and Plasencia). Eastern Iberia undergoes crustal extension linked to the rift at the Valencia trough, which activates normal faults in the Catalonian and Transversal ranges (El Camp and Amer faults, the latter being responsible for Olot seisms, 1427-1428) and the central-eastern Iberian Chain (Concud –with evidences of Late Pleistocene paleoseisms with potential magnitude close to 6.8–, Teruel or Maestrat faults), in this case without recent catastrophic seisms. Active tectonics in the Pyrenees is caused by interaction between rift extension, intraplate compression and isostatic movements. Main seismicity occurs at the north face of the western Pyrenees (Lourdes-Arette) and at the central chain (Vielha earthquake, 1923, in the northern Maladeta fault).
The Iberian Peninsula shows low to moderate seismicity caused by active faults that move at rates of the order of 10-2-10-1 mm/y. Maximum potential magnitudes range from 6.0 to 7.0, and the recurrence periods of the major seisms, for each fault, are of the order of 103-104 years. The Betic chains are the most active zone, where the convergence with the African Plate is accommodated by a high number of faults, responsible for several historic earthquakes with intensity = X. The most conspicuous ones are left-lateral, NE-SW strike-slip faults such as Carboneras, Palomares, Alhama and Bajo Segura faults (seisms of Vera, 1526, Torrevieja, 1829, or Lorca, 2011) and E-W extensional faults such as Zafarraya (Arenas del Rey earthquake, 1884). The compression propagated through Iberia from its southern margin also reactivates large strike-slip faults at the Iberian Massif (Manteigas-Vilariça-Bragança –with evidence of Holocene paleoseisms over M = 7.0– and Plasencia). Eastern Iberia undergoes crustal extension linked to the rift at the Valencia trough, which activates normal faults in the Catalonian and Transversal ranges (El Camp and Amer faults, the latter being responsible for Olot seisms, 1427-1428) and the central-eastern Iberian Chain (Concud –with evidences of Late Pleistocene paleoseisms with potential magnitude close to 6.8–, Teruel or Maestrat faults), in this case without recent catastrophic seisms. Active tectonics in the Pyrenees is caused by interaction between rift extension, intraplate compression and isostatic movements. Main seismicity occurs at the north face of the western Pyrenees (Lourdes-Arette) and at the central chain (Vielha earthquake, 1923, in the northern Maladeta fault).