Volcanic evolution of the island of Tenerife (Canary Islands) in the light of new K-Ar data

Ancochea, Eumenio; Fúster, José-Maria; Ibarrola, Elisa; Cendrero, Antonio; Coello, José Manuel de Pablos; Hernán, Francisco; Cantagrel, J. M.; Jamond, Colette

doi:10.1016/0377-0273(90)90019-c

Cited by 441 publications

(460 citation statements)

References 21 publications

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“…The evolution of volcanic activity on Tenerife can be summarized as: (1) a basaltic shield that forms about the 90% of the island and is still growing through two main rift zones (Abdel-Monen et al 1972;Ancochea et al 1990;Thirlwall et al 2000), (2) a Central Complex (> 3.5 Ma to present, Fúster et al 1968;Araña 1971;Ancochea et al 1990;Martí et al 1994), which comprises the Las Cañadas edifice (> 3.5 to 0.19 Ma), a composite basaltic to phonolitic volcano with abundant explosive eruptions and up to three caldera collapse episodes (Martí et al 1994(Martí et al , 1997Martí and Gudmundsson 2000), and (3) the currently active Teide and Pico Viejo stratovolcanos (0.19 Ma to present).…”

Section: Volcanological Backgroundmentioning

confidence: 99%

Magma storage conditions of the last eruption of Teide volcano (Canary Islands, Spain)

2009

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Phase equilibrium experiments were performed to determine the pre-eruptive conditions of the phonolitic magma responsible for the last eruption (about 1150 yr B.P.) of Teide volcano. The Lavas Negras phonolite contains 30 to 40 wt% of phenocrysts, mainly anorthoclase, diopside, and magnetite. We have investigated pressures from 100 to 250 MPa, temperatures from 750 to 925 o C, water contents from 1.3 to 10 wt%, at an oxygen fugacity (fO 2 ) of 1 log unit above the Ni-NiO solid buffer. Comparison of the natural and experimental phase proportions and compositions indicates that the phonolite was stored at 900 ± 20ºC, 150 ± 50 MPa, 3 ± 0.5 wt% dissolved H 2 O in the melt. The fO 2 was probably close to the fayalite-magnetite-quartz solid buffer judging from results of other experimental studies. These conditions constrain the magma storage depth at about 5 ± 1 km below current summit of Teide volcano. Given that the island has not suffered any major structural or topographic changes since the Lavas Negras eruption, any remaining magma from this event should still be stored at such depth and probably with a similar thermal and rheological state. 3 3

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Section: Volcanological Backgroundmentioning

confidence: 99%

Magma storage conditions of the last eruption of Teide volcano (Canary Islands, Spain)

2009

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“…The subaerial part of Tenerife was originally constructed by fissure eruptions of ankaramite, basanite and alkali basalts, that occurred between 12 and 3.3 Ma (Ancochea et al, 1990). According to Hausen (1956), the 'basaltic tableland series' products of these eruptions, are crossed by numerous dikes and outcrop at the three corners of the island, Anaga, Teno and Roque del Conde (Figure 2).…”

Section: Geological Settingmentioning

confidence: 99%

“…The valley of Güimar and shortly afterwards the Orotava valley were formed by large landslides after 0.8 Ma, and probably before 0.6 Ma. The Cañadas caldera may have had several collapse phases and the present caldera was formed by a landslide since 0.2 Ma (Ancochea et al, 1990). However, the key aspects of the history of the flanks of Tenerife are controversial, including the number of landslide events, their timing and nature and their possible relationship with onshore structures.…”

Section: Geological Settingmentioning

confidence: 99%

Morphological and structural analysis in the Anaga offshore massif, Canary Islands: fractures and debris avalanches relationships

Llanes

Muñoz²,

Muñoz-Martı́n

et al. 2003

Mar Geophys Res

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As part of the 'National Hydrographic and Oceanographic Research Plan for the Spanish Exclusive Economic Zone', multibeam bathymetry and seismic reflection profiles were obtained in the Canary Islands aboard the R/V Hespérides. The submarine flanks of the Anaga offshore extension of Tenerife Island are here studied to analyze its geomorphology. In the north sector of the Anaga submarine massif, the extension of the Anaga Debris Avalanche has been mapped for the first time, and a volume of 36 km 3 was calculated. The relationship between the Anaga and Orotava Debris Avalanches is also described. Faulting has been recognized as a key process for the occurrence of debris avalanches and the growth of volcanic lineaments. Moreover, faulting affects previous structures and the channelling of debris flows. Structural analysis shows the typical radial pattern of an oceanic island. In addition, a NE-SW dominant direction of faulting was obtained, consistent with the Tenerife Island structural trend seen in the Anaga Massif and Cordillera Dorsal. NW-SE and E-W are two other main trends seen in the area. Special interest is manifest in two long faults: 'Santa Cruz Fault' bounds the southern edge of Anaga offshore Massif with a length of 50 km and a direction that changes from NE-SW to almost E-W. The Güimar Debris Avalanche was probably channeled by this fault. The 'Guayotá Fault' was recognized in several seismic profiles with a N-S direction that changes towards NW-SE at its southern end. This fault affects the more recent sediments with a vertical offset of 25-30 m, along 60 km. It has been interpreted as a transpressive strike-slip fault.

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“…El Edificio Cañadas se ha levantado sobre el escudo volcánico central de Tenerife (Carracedo 1979;Ancochea et al, 1990;Guillou et al, 2003) en los últimos 3-3,5 Ma (Ancochea et al, 1999), pasando por sucesivos episodios en que alternan los colapsos gravitatorios y el relleno de las cuencas de deslizamiento. El último de estos episodios ha dado lugar a la actual caldera de Las Cañadas y el complejo volcánico del Teide y sus aparatos asociados (figs.…”

Section: Introductionunclassified

“…Son numerosos los estudios dedicados al Edificio Cañadas, que incluyen abundantes dataciones radiométricas (Ancochea et al, 1990(Ancochea et al, , 1999Mitjavila y Villa, 1993;Martí et al, 1994). Sin embargo, los trabajos publicados sobre el Teide y el sistema de rifts, la actividad eruptiva más reciente de la isla, son escasos y apenas incluyen dataciones absolutas, especialmente en el caso del Teide.…”

Section: Introductionunclassified

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Carracedo¹,

Paterne²,

Guillou³

et al. 2003

Estud. geol.

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RESUMENEl Teide, el edificio volcánico más alto del planeta (3.718 m sobre el nivel del mar, > 7 km desde el fondo oceánico) después del Mauna Loa y Mauna Kea en las islas Hawaii, forma un complejo volcánico en el centro de la isla de Tenerife. Su actividad eruptiva reciente (últimos 20 Ka) está asociada con la rama NO del rift triple (120°) que ha configurado la etapa reciente de construcción de la isla. La mayoría de las erupciones de Tenerife en este período se han localizado en estas estructuras volcánicas, generando frecuentes y extensas coladas máficas y félsicas, muchas alcanzado la costa e invadiendo lo que es ahora una de las zonas más densamente pobladas de Tenerife y, probablemente, de cualquier isla oceánica del planeta. Sin embargo, y a pesar de los numerosos estudios y proyectos previos, falta aún información geológica básica para este importante sistema volcánico, en particular la datación de las diferentes erupciones que lo componen, con objeto de reconstruir el marco geocronológico indispensable para conocer su evolución y determinar científicamente los riesgos volcánicos, de perentoria necesidad habida cuenta de su naturaleza y entidad, y de la población potencialmente afectada. Nuevas dataciones de Carbono-14 y K/Ar aportan ahora importante información a este respecto. La mayoría de las erupciones de los últimos 20 Ka no están relacionadas con el estratovolcán Teide, que sólo ha tenido una hace 1.240 ± 60 años ---entre 663 y 943 AD una vez calibrada la edad-, sino con el volcán Pico Viejo (17.570 ± 150 a BP), los centros eruptivos adventicios fonolíticos de la base del Teide (Mña. Abejera centro alto, 5.170 ± 110 a BP; Mña. Abejera centro bajo, 4.790 ± 70 a BP; Mña. de La Angostura inicial, 2.420 ± 70 a BP; Mña. de La Angostura, 2.010 ± 60 a BP y Roques Blancos, 1.790 ± 60 a BP), y en el Rift NO (Mña. Chía, 3.620 ± 70 a BP). Aunque la actividad volcánica de los últimos 20 Ka incluye al menos 7 erupciones fonolíticas de gran volumen de centros eruptivos situados en la cara norte del Teide, supuestamente muy inestable, esto no parece haber generado respuesta alguna del sistema volcánico. Más bien ha contribuido a asegurar la estabilidad estructural del conjunto, al aumentar y reforzar la base del estratovolcán. Por el contrario, la ocurrencia de estas erupciones y las del Rift NO imponen un elevado riesgo por flujo de coladas en el norte y oeste de Tenerife, zona ahora densamente poblada y que ha sido casi totalmente recubierta con lavas en los últimos 20.000 años.

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Volcanic evolution of the island of Tenerife (Canary Islands) in the light of new K-Ar data

Cited by 441 publications

References 21 publications

Magma storage conditions of the last eruption of Teide volcano (Canary Islands, Spain)

Magma storage conditions of the last eruption of Teide volcano (Canary Islands, Spain)

Morphological and structural analysis in the Anaga offshore massif, Canary Islands: fractures and debris avalanches relationships

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