SciELO - Scientific Electronic Library Online

 
vol.36 issue1First record of megafloras and palynology in the Tarija Formation (Pennsylvanian), Aguas Blancas creek, Salta Province, Argentina: Description of two new speciesTsunamigenic, earthquake-triggered rock slope failures during the April 21, 2007 Aisén earthquake, southern Chile (45.5°S) author indexsubject indexarticles search
Home Pagealphabetic serial listing  

Andean geology

On-line version ISSN 0718-7106

AndGeo vol.36 no.1 Santiago Jan. 2009

http://dx.doi.org/10.4067/S0718-71062009000100009 

Andean Geology 36 (1): 125-129. January, 2009 

Andean Geology
formerly Revista Geológica de Chile
www.scielo.cl/rgch.htm

GEOLOGICAL NOTE

 

The 2008 eruption of the Chaitén Volcano, Chile: a preliminary report

 

La erupción 2008 del volcán Chaitén, Chile: informe preliminar

 

Luis E. Lara

Servicio Nacional de Geología y Minería, Chile, Avda. Santa María 0104, Providencia, Santiago, Chile. lelara@sernageomin.cl


ABSTRACT. On May 2, 2008 a Plinian eruption began on Chaiten volcano. Dome growing stage would have started on May 10-12 and extensive lahars and floods affected Chaiten town (ca. 5,000 inhabitants) on May 12. A volume up to ca. 4 km3 (non DRE) of rhyolitic magma would be extruded mostly during the explosive phase. Eruptive activity has not completely finished by the end of November. Because of the wide impact of this type of volcanism, this eruption poses a series of questions regarding explosive volcanism that should be addressed in the near future.

Key words: Chaiten volcano, Plinian eruption, Chile, Southern Andes.


RESUMEN. El 2 de mayo se inició una erupción pliniana en el volcán Chaitén. Entre el 10 y el 12 de mayo, se habría iniciado la construcción de un domo y el día 12 de mayo lahares e inundaciones afectaron la ciudad de Chaitén (ca. 5.000 habitantes). Aproximadamente hasta 4 km3 de magma riolítico (no ERD) habría sido evacuado principalmente durante la fase explosiva. Hacia fines de noviembre, la actividad eruptiva no había terminado por completo. Esta erupción plantea una serie de interrogantes científicas que deberían ser enfrentadas en un futuro cercano dado el amplio impacto que este tipo de volcanismo representa.

Palabras clave: Volcán Chaitén, Erupción pliniana, Chile, Andes del Sur.


 

1. Introduction

On May 2,2008 a large volcanic eruptionbegan in the southern Andes without significant precur-sory activity and, due to some conspicuous features (rhyolitic nature of the magma; long durationof the explosive phase, e.g., Sparks etal, 1997; extensive impact with-5000 people evacuated), capturedthe interest of the scientific community (Fig. 1). This was also the first rhyolitic eruption to be recorded by geophysical tools (seismology, remote sensing) despite the isolation of the place where it happened. The more than 9 month long eruptive 2008 episode -not yet finished by late November- has posed severa! challenges for the scientific understanding of the event, short-term forecast capacity and crisis management. This arricie is intended as abrief, non exhaustive overview of the entire volcanic eyele based on the contributions of many people who worked hard to get the most relevant data in near real-time. Extensive overview and scientific arricies should be written in the near future, when eruptive activity declines completely. The first account for scientific aspeets is due to Carn et al. (2008) and several contributions would be presented to the 2008 AGU Fall Meeting. Technical reports on the ongoing eruption were timely uploaded at the SERNAGEOMIN institutional web page (www.sernageomin.cl).

2. Geology and eruptive history of Chaitén volcano

The small Chaitén volcano (42.83°S, 72.65°W, alt. 1,122 m) is located in the southern Andes and its background geology is poorly known apart from the reconnaissance work done by Moreno (1995)1 andbased on a study of aerial photographs. The last known major eruption occurred at ca. 9.4 ka BP (Naranj o and Stern, 2004) and would have produced a small caldera (~3 km diameter) accompanied by ejection of pyroclastic flows and ash fall deposits containing rhyolite pumice (74 wt% Si02). Afterthe caldera collapse event, a large (~0.4 km3) obsidian lava dome was built inside. No recent activity has been reported although growing evidence points to historical episodes. Prior to the 2008 eruption there were no evident signáis of volcano unrest. Chaitén volcano is one among more than 120 active volcanoes of continental Chile but its threat was not considered at a high priority level, mostly by the lack of reported recent eruptions (Lara et al, 2006) and consequently it remained unmonitored until the beginning of the eruption.

3. Chronology of the 2008 eruption and eruptive products

Only 36 hours of precursory seismic activity were detected by distant instruments, located more than 300 km away from the Chaitén volcano. On April 30, some large volcano-tectonic (VT) earth-quakes with coda magnitude up to 5 were located up to 20 km from Chaitén volcano. The number of large VT events reached up to 20 per hour on May 2, coinciding with an initial Plinian eruption which began approximately at 8:00 UT (04:00 local hour) and lasted ca. 6 hours with an eruptive column that rose up to 21 km as reported by eyewitness (Fig. 2). Seismicity declined abruptly by May 3, but sus-tained emission of ash plumes continued until May 6 when a second Plinian column reached 20 km in altitude(12:32UT)andagainonMay8(03:36UT). Despite the reported máximum column height (which is minor when constrained by satellite data, e.g., Carn et al., 2008), these Plinian eruptions produced only minor column-collapse pyroclastic flows res-tricted to local áreas within the caldera and notably to the northern flank of the volcano. Ash columns were fed by several craters formed on the preexis-ting obsidian dome, mostly on its northern flank. Probably on May 10-12, extrusión of a new dome began although this was not confirmed until May 21. Dome growing at high rates (>20 m3/s) continued through late October, accompanied by lower ash columns (<3.5 km altitude) and steam emissions. For comparison, Soufriére Hills dome grew at ca.6 m3/s during 1979 and 1986 cycles (Huppert et al., 1982) and Mount Saint Helens did it at ca. 10 m3/s in 1980 (Murase et al., 1985). Dome extrusión has beenaccompaniedby weakbut sustained seismicity with a new swarm of VT earthquakes that began in late June and continued through Jury. Random increments of ash emissions occurred on July and August but as part of a long-term falling trend (Fig. 3). By September, seismicity declined and ash columns were no higher than 2 km.

FIG. 2. Four stages of Chaitén 2008 eruption. A. Plinian column on May 2 (courtesy of http://www.throughthetube.com/) taken from Argentina; B. Active craters during the Plinian stage on May 6, now partially concentrated on the northern flank of the older dome (photo by Daniel Basualto); C. New dome (reddish) recognized on May 21 on the northern flank extruded over remnants of the ancient one (photo by L.E. Lara); D. Aerial view of a reduced although still active ash column on September 4 (photo by L.E .Lara).


If máximum reported heights are taken into account, from empirical power law models that relates height of eruptive columns and discharge rates (e.g.. Sparks et al, 1997), the cumulated volume during the Plinian phase (2-8 May) would have reached up to ca. 4 km3 of magma (non DRE), but it would not be higher than 1 km3 if duration of Plinian columns is considered (Carn et al, 2008). Volume estimates from ash thicknesses recorded at distal áreas prior to erosión (80-150 km away from the source) yield valúes of about 4 km3 as well. Volcanic Explosivity índex (Newhall and Self, 1982) was estimated in the range of VEI4-5.

Chaitén ashfalls revealed a very fragmented magma with up to -12% vol of respirable (<4μm) fine particles (Horwell etal., 2008)2 whichbecomes a respiratory health risk. Ash, pumice and obsidian samples of the 2008 eruption indicate a crystal-poor rhyolitic magma (74-76% Si02), similar to the previous dome and related pyroclastic deposits. No compositional changes were observed from the early Plinian phase to the present dome growing stage. Very low S02 emissions were measured on the eruptive plume by remote sensing (Carn et al., 2008).

4. Eruption response and impacts

On May 4, SERNAGEOMIN (the Chilean Geological Survey) installed a seismic network around Chaitén volcano. In late May, real-time telemetered broadband seismometers were added with assistance from the U.S. Geological Survey (USGS) Volcano Disaster Assistance Program (VDAP). Parallel tracking of ash emissions was done by the Buenos Aires Volcanic Ash Advisory Center (VAAC) and the Universidad de Chile using satellite data. NASAs satellite constellation also provided direct measurement of volcanic clouds (ozone, SiO2, ash mass loading).

Crisis assessment was carried out by SERNAGEOMIN in cióse relation with both regional and national authorities. Active media releases kept national and international communities informed. Preventive evacuation of ca. 5,000 residents was ordered on May 4-5 and two security radius were defined at 30 and 50 km on May 6 based on scientific advice. This was done 6 days before the Chaitén city was affected by floods on May 12. A volcanic hazards map was done during the crisis to advice emergency management (Moreno and Lara, 2008)3.

Impacts of the eruption were extensive in Chile and Argentina. Floods and lahars inundated the al-ready evacuated Chaitén town on May 12 and up to US$12 millions are the estimated economic losses only by insured public buildings. Ash clouds shut down regional airports and forced the cancellation of hundreds of domestic flights and several international flights in Argentina and Chile. Floods also disrupted the backbone road of continental Chile and the active aquiculture industry was severely affected (Fig. 4). More than US$36 millions have been allocated for the social support to evacuated people.

 

FIG 4. Extensive damage in Chaitén town generated by floods and lahars. A. Satellite image acquired on May 19 shows both the inundated área and the suspended sediment due to the coastal drift (courtesy of NASA at http://earthobservatory.nasa.gov); B. Severe damages on the urban infrastructure (photo by L.E. Lara).

5. Challenging scientific aspects

Plinian eruptions are scarce and occur at a rate of a few per century around the world. Rhyolite magmas are scarcerthanbasalt-andesite suites and the driving processes for rhyolitic eruptions are an important field of research. The large quiescence periodbefore the eruption without any unrest signáis is also remarkable. Onthe otherhand, most historie Plinian eruptions ended no later than 36 hours after the paroxysmal stage (e.g., Sparks et al, 1997). The long duration of the explosive phase with repeated Plinian columns and sustained explosions that still accompany the dome growing is uncommon. The very short period of seismic activity before the onset of the eruptive activity is also intriguing. Extremely low S02 emissions measured in the eruption clouds, lower than expectedeven for rhyolitic magmas, still require explanation. Finally, abetterknowledge of long-term evolution of Chaitén volcano and basic geology is urgently needed.

Acknowledgements

I thank M. Suárez, Chief Editor of Andean Geology, the invitation to prepare a note on the Chaiten eruption. H. Moreno, D. Basualto, R Peña, C. Delgado and C. Gallegos, the staff of the OVDAS (Observatorio Volcanológico de los Andes del Sur) from SERNAGEOMIN were part of the task forcé that worked hard on the crisis and much of the trend analysis is based on their reports. J. Muñoz was responsible for coordination and support in the área and maintained a close relationship with the local authorities. R. White, A. Lockhart, J. Marso and J. Power from VDAP-USGS assisted with the monitoring network and data retrieval and analysis. J. Pallister and J. Ewert from VDAP-VHP (USGS) also contributed with many ideas aboutthe ongoing volcanic crisis. R. Aguilera (Universidad de Chile) andA. Pavez shared satellite images and tracked the ash dispersión. R. Wall and W. Vi vallo supervised the eruption response as executive officers of SERNAGEOMIN. G. Villarrosa (Universidad Nacional del Comahue) shared valuable data of ash thickness in Argentina before the extensive erosión. Students of GL-611 at the Universidad de Chile were involved in volunte estimations as part of their basic training. J. Caballero and M. Soto (SERNAGEOMIN) managed the media releases putting in simple words the technical reports. Valuable field assistance was provided by Carabineros de Chile (especially J. López andA. Villablanca) and Armada de Chile and many thanks go to them. Without the support from all of these people this contribution would not have been possible. This modest work is dedicated to Chaitén's residents, whose lives were severely disrupted by the eruption.

NOTAS

1 Moreno, H. 1995. Estudio fotogeológico escala 1:100.000 de los volcanes de la X Región Sur. Proyecto Carta Metalogénica de la X Región Sur, Servicio Nacional de Geología y Minería (unpublished).

2 Horwell, C; Michnowicz, S.; Le Blond, J. 2008. Report on the mineralogical and geochemical charactensation of Chaitén ash for the assessment of respiratory health hazard. University of Durham-IVHHN-Natural Environmental Research Council (unpubhshed): 36 p.

3 Moreno, H.; Lara, L.E. 2008. Peligros volcánicos potenciales del volcán Chaitén (erupción de mayo 2008), Región de los Lagos. Servicio Nacional de Geología y Minería, 1 mapa escala 1:500.000 (unpublished).

References

Carn, S.A.; Pallister, J.S.; Lara, L.E.; Ewert, J.; Fromm, M.; Watt, S.; Prata, A.J.; Thomas, R. In press. The awakening of Chaiten volcano, Chile. EOS.        [ Links ]

Huppert, HE.; Shepherd, J.B.; Sigurdsson, H.; Sparks, R.S.J. 1982. On lava dome growth, with application to the 1979 lava extrusión of the Soufriére of St. Vincent. Journal of Volcanology and Geothermal Research 14: 199-222.        [ Links ]

Lara, LE.; Clavero, J.; Hinojosa, M.; Huerta, S.; Wall, R.; Moreno, H. 2006. NVEWS-CHILE: Sistema de Clasificación semicuantitativa de la vulnerabilidad volcánica. In Congreso Geológico Chileno, No. 11, Actas 2: 487-490. Antofagasta.        [ Links ]

Murase,T;McBirney,A.; William,G.M. 1985. Viscosity of the dome of Mt. St. Helens. Journal of Volcanology and Geothermal Research 24: 193-204.        [ Links ]

Naranjo, JA.; Stern, Ch. 2004. Holocene tephrochronology of the southernmostpart(42o30'-45°S)oftheAndean Southern Volcanic Zone. Revista Geológica de Chile 31 (2): 225-240.        [ Links ]

Newhall, C.G.; Self, S. 1982. The volcanic explosivity index (VEI): An estimate of explosive magnitude for historical volcanism. Journal of Geophy sical Research 87: 1231-1238.        [ Links ]

Sparks,R.S.J.;Bursik,M.I.;Carey,S.N.;Gilbert,J.S.;Glaze,L.S.; Siggurdsson,H.;Woods,AW. 1997. Volcanic Plumes. John Wiley and Sons: 574 p. New York.        [ Links ]

Manuscript received: October 01, 2008; accepted: November 06, 2008