Cumbre Vieja

Cumbre Vieja

Satellite photo of Caldera de Taburiente and Cumbre Nueva, La Palma, Canary Islands (south is above, north is below).
Highest point
Elevation 1,949 m (6,394 ft) [1]
Coordinates 28°34′N 17°50′W / 28.567°N 17.833°W / 28.567; -17.833
Geography
Location La Palma, Canary Islands,  Spain
Geology
Mountain type Stratovolcano
Last eruption 1971[2]

Cumbre Vieja (Spanish: Old Summit) is an active although dormant volcanic ridge on the volcanic ocean island of Isla de La Palma in the Canary Islands, Spain, that erupted twice in the 20th century – in 1949, and again in 1971.

The ridge of the Cumbre Vieja trends in an approximate north-south direction and covers the southern two-thirds of the island. Several volcanic craters are located on the summit ridge and flanks.

Volcanic history

La Palma is a volcanic ocean island, located on the African Plate and is currently - along with Tenerife, one of the most volcanically active of the Canary Islands.[3] Historical eruptions on the Cumbre Vieja occurred in 1470, 1585, 1646, 1677, 1712, 1949 and 1971.

Since ~125 ka, all sub-aerial eruptive activity has been associated with the Cumbre Vieja with eruptions ranging over the whole ~25 kilometres long ridge. The Cumbre Vieja is known from submarine surveys to continue south of Punta de Fuencaliente (the Point of the Hot Fountain). Volcanic activity connected with the submarine extension has not been observed or recorded.

Detailed geological mapping shows that the distribution and orientation of vents and feeder dykes within the volcano have shifted from a triple rift system (typical of most volcanic ocean islands) to one consisting of a single north-south rift.[4][5] It is hypothesised that this structural reorganisation is in response to evolving stress patterns associated with the development of a possible detachment fault under the volcano's west flank.[6][7] Siebert (1984)[8] showed that such failures are due to the intrusion of parallel and sub-parallel dykes into a rift. This causes the flanks to become over-steep and this inevitably causes the structure of the volcano to become unstable and catastrophic failure may occur. There is no evidence that the 1949 section of the rift extends in a north-south direction beyond its surface expression, nor that there is a developing detachment plane. Research is ongoing.

1949 eruption

The onset of the eruption was witnessed by a shepherd who was tending sheep and goats on the flank of the Nambroque. He was startled to hear noises emanating from the Duraznero vent and became extremely alarmed when material started being expelled from the vent. In a state of panic he fled the area and sought refuge as far from the vent as he could. The only contemporaneous account of the eruption was published in 1950 by one of the scientists - Juan Bonelli-Rubio[9] who witnessed the eruption first hand and recorded details of the various phenomena that occurred during the eruption. All other published accounts are based upon Bonelli-Rubio's observations. The next report regarding the eruption was a joint publication by Ortiz and Bonelli-Rubio published in 1951.[10] This drew heavily on Bonelli-Rubio's observations and also analysis of various phenomena associated with the eruption. Both accounts are published in Spanish.

The eruption started on 24 June 1949 – the feast day of St John, which is why in Spanish texts the eruption is referred to as "la erupcion del Nambroque o San Juan," which in English is "The Eruption of the Nambroque or St John's volcano." During the 1949 eruption, eruptive activity was located at three vents —Duraznero, Llano del Banco, and Hoyo Negro — mild strombolian activity occurred at the Duraznero vent. Lava was erupted from the Llano del Banco vents, whilst only mild phreatomagmatic emissions occurred at the Hoyo Negro vent. Then on 30 July - the last day of eruptive activity, lava was erupted at the Duraznero fissure and vent. During the eruption on 1 and 2 July, two strong earthquakes with an estimated intensity of VIII on the Modified Mercalli Scale also occurred, the epicentre was calculated to be near Jedey. Following the earthquakes a fracture was noted and it had a length of approximately one and half kilometres. It was traceable to the Hoyo Negro and Duraznero vents, making a total length of about two and half kilometres or about 1/10 of the exposed length of the Cumbre Vieja, and parts of the western half of the Cumbre Vieja ridge had apparently moved about 1 metre sideways and 2 metres downwards towards the Atlantic Ocean. It was only in the vicinity of the Duraznero and Hoyo Negro vents that the vertical displacement attained about 4 metres.[9] As of 2008, the fracture is still visible and still has the same dimensions recorded in 1949.

The timeline for the eruption, according to Bonelli-Rubio,[9] is as follows: The first reported seismic activity was noted on the rim of the Caldera de Taburiente on 23 July 1936, with further activity noted over the next two days. During the following years periodic seismic activity occurred, but due to the absence of monitoring equipment, the only reports are those recorded in the media. Then at about 09:00 (local time) on 24 June 1949, the Duraznero vent opened with mildly explosive activity, venting of gases, and rocks; with eruptive activity continuing in this manner until 6 July. During this phase a strong earthquake occurred on 1 July and again on 2 July with an estimated intensity of VIII on the Modified Mercalli Scale. Visits to the summit region revealed a crack about 1.5 km (~1 mile) long which extended in a northerly direction from the Hoyo Negro (Black Hole) and about 1 km (~0.5 mile) south to the Duraznero vent making a total length of about 2.5 km (~1.6 mile), (this crack is the subject of research and heated debate as to whether it indicates initial failure of the western flank - or not). Later analysis placed the epicentre north of the township of Jedey. Eruptive activity at the Duraznero vent ceased on 6 July with only degassing continuing. No eruptive activity occurred on 7 July. On 8 July eruptive activity commenced at the Llano del Banco vents - about 4 km (~2.5 miles) north of the Duraznero vent, as lava was erupted and flowed down the western flank. The vents opened progressively up the barranco (ravine), forming a series of en echelon (diagonally side by side), vents. On 10 July the westward flow of lava from the Llano del Banco vents reached the coast at Puerto de Naos and entered the Atlantic Ocean, forming a lava delta, the velocity is estimated at ~14 metres (approximately 46 feet) per sec. On 12 July mildly explosive activity commenced at the Hoyo Negro (Black Hole) with emissions of rocks, fumes and some phreatomagmatic activity indicating that the eruption had encountered ground waters. Activity at the Hoyo Negro ceased on 22 July, but continued at the Llano del Banco vents until 26 July. Only residual fumarolic activity and thermal emissions then occurred until 30 July when the Duraznero vent and fissure re-activated. Lava then flowed from the Duraznero vent and fissure, filling the adjacent crater of El Fraile and created a lava lake. This subsequently overflowed and the lava flowed down the eastern flank towards the ocean. It finally stopped about 1 km (about 0.5 mile) from the ocean. Also later on, on 30 July all eruptive activity ceased and only residual fumarolic activity continued until 4 August; thereafter there was only thermal emissions. It is estimated that approximately 60 million cubic metres of lava was erupted during the eruption.[9][11]

Volcanic Explosivity Index

The eruption style ranged from effusive - mildly explosive at the Duraznero and Llano del Banco vents to mildly explosive at the Hoyo Negro vent and was strombolian in style. It therefore is classed as having a Volcanic Explosivity Index (VEI) of 1 or 2.[12]

The earthquakes of 1 and 2 July

The process creating the earthquakes of 1 and 2 July is considered to have been driven by the pressure caused by the rising magma super-heating water trapped within the edifice of the volcano.[6] It is unlikely that the trapped waters could vapourise due to being under considerable pressure. What is postulated is that the waters were heated to a point where they could not absorb further thermal energy in the available space. Continuing heating required the water to expand further and the only way it could do so was to move the flank of the volcano. This caused the two earthquakes that were reported as occurring during the eruption along with the development of the crack.

That the entrapped (within the edifice) water did not vapourise is shown by the absence of phreatomagmatic explosions except the mildly explosive eruptive activity that occurred at the Hoyo Negro vent from 12 July to 22 July: steam escaping explosively from the ground is often a precursor of volcanic activity. Further evidence that vapourisation did not occur is that when Rubio Bonelli visited the rift the following day, the newly opened fissure "... Was not issuing fumes, vapour, steam, ashes, lava or other materials ..."[9] In fact at no time during or after was steam or phreatomagmatic activity reported. This reinforces the claim that the waters trapped within the edifice never vapourised, which they would do if the pressure had fallen sufficiently to allow the super-heated water to flash into steam. Only at the Hoyo Negro did any phreatomagmatic activity occur.

Due to the lack of seismic monitoring equipment on the island - apart from reports in the media, no record exists of any seismic activity that occurred pre-, syn- or post- eruption. Therefore, any claims about seismic activity are based upon personal observation and may not be reliable.

1971 eruption

The 1971 eruption occurred at the southern end of the Cumbre Vieja at the Teneguía vent. The eruption was mainly strombolian in style. Lava was also erupted. Seismic activity did occur before and during the 1971 eruption, but was not on the scale associated with the 1949 eruption. Residual thermal emissions continue.

Future threats

BBC's megatsunami

Satellite photo of La Palma, Canary Islands (north is in the lower right). The crater in the centre is the Caldera de Taburiente. The Cumbre Vieja is the ridge to the south (upper left) of the caldera and between them is the Cumbre Nueva.

Day et al.; (1999),[6] indicated that the Cumbre Vieja may be in the initial stages of failure. The authors of the paper also claimed that the geological development of La Palma had undergone changes due to the southerly migration of the hotspot, and the collapse of the earlier volcanoes. Subsequent to this a triple arm rift system had evolved with the eventual closing down of volcanic activity associated with two of the arms - the north-west and north-east rifts. The reasons can only be hypothesised. This caused the southern arm - the Cumbre Vieja to be the sole source of volcanic activity. As a result, they postulated that the western flank may be in the initial stages of failure.

In October 2000, the British Broadcasting Corporation (BBC) transmitted a "Horizon" programme called "Mega-tsunami; Wave of Destruction",[13] which suggested that a future failure of the western flank of Cumbre Vieja would cause a "mega-tsunami".

On 18 April 2013, the BBC transmitted a follow-up programme entitled Could we survive a Mega-Tsunami? The programme was presented in a "Breaking News" reporting style. It claimed that the western flank of the Cumbre Vieja had collapsed and that the initial wave had an amplitude of about 1,000 metres. The programme uses computer generated graphics to present a storyline that is based on a hypothesis.[14] The programme "interviewed" several scientific personnel attempting to give credence to the story - which according to one of the scientists involved "This is a true story - only it hasn't happened yet!"

Day et al; (1999),[6] Ward and Day (2001);[7] and Ward and Day (2005)[15] hypothesize that during an eruption at some unascertained future date, the western half of the Cumbre Vieja—approximately 500 km3 (5 x 1011 m3) with an estimated mass of 1.5 x 1015 kg—will catastrophically fail in a massive gravitational landslide and enter the Atlantic Ocean, generating a so-called 'mega-tsunami'. The debris will continue to travel along the ocean floor as a debris flow. Computer modelling indicates that the resulting initial wave may attain a local amplitude (height) in excess of 600 metres (2,000 ft) and an initial peak to peak height that approximates to 2 kilometres (1 mi), and travel at about 720 kilometres per hour (450 mph) (approximately the speed of a jet aircraft), inundating the African coast in about 1 hour, the southern coastlines of the British Isles in about 3.5 hours, and the eastern seaboard of North America in about 6 hours, by which time the initial wave will have subsided into a succession of smaller ones each about 30 metres (100 ft) to 60 metres (200 ft) high. These may surge to several hundred metres in height and be several kilometres apart while retaining their original speed. The models of Day et al; (1999),[6] Ward and Day (2001),[7] suggest that the event could inundate up to 25 kilometres (16 mi) inland. If the model is correct, then this scale of inundation would greatly damage or destroy cities along the entire North American eastern seaboard, including e.g. Boston, New York City, Miami, etc., and many other cities located near the Atlantic coast.

Criticism

There is controversy, however, about the threat presented by the Cumbre Vieja. Current indications are that recent landslides may have been gradual, and therefore may not generate tsunamis unless they increased in magnitude. Studies of possible local 'mega-tsunamis' in the Hawaiian Islands draw distinctions between the tsunami wave periods caused by landslides and subduction-zone earthquakes, arguing that a similar collapse in Hawaii would not endanger Asian or North American coastlines.[16]

Sonar surveys around many volcanic ocean islands including the Canary Islands,[17] Hawaii, Réunion etc., have mapped debris flows on the sea floor. Many of these debris flows are about 100 km or about 60 miles long, and up to 2 km or about 1.25 miles thick, contain mega-blocks mixed up with finer detritus. The debris flows are now considered to be a normal process where a volcano sheds excess material to make itself more stable. It is also known to occur on all volcanoes based on the land, in or under the sea.

Moore (1964)[18] was the first geologist to interpret such features depicted on a United States Navy bathymetric chart. The chart showed two features that seem to originate from the Hawaiian islands of Oahu and Molokai.

Moss et al.; (1999),[19] reported that the western flank is static and there is no indication that it has moved since 1949, confirming the dimensions provided by Bonelli-Rubio (1950).[9]

Carracedo et al.; (2001),[20] state that they consider the crack to be a surface expression which is of a shallow and inactive nature. They also indicate that it should be monitored, but consider the possibility that the edifice is unstable as being almost non-existent.

The Tsunami Society (2002),[21] claim that the model used by Day et al.; (1999)[6] and Ward and Day (2001),[7] and Ward and Day (2005)[15] is wrong. They cautioned about the claims made by Day et al.; and Ward and Day stating that there is no evidence of a mega-tsunami having been generated by volcanic edifice failure.

Ward and Day (2003),[22] reported on the only documented flank collapse of a volcanic island - Ritter Island, that occurred on 13 March 1888. Approximately 5 X 109 m3 (or about 2 orders of magnitude less than the claimed mass of the Cumbre Vieja), of material generated a landslide which entered the ocean and generated a westerly directed tsunami. The tsunami inundated adjoining islands and may have killed several hundreds of people. According to Cooke [23] damage was inflicted on islands several hundreds of kilometres from Ritter Island. There is no record of inundation occurring at trans-oceanic distances. The tsunami was witnessed by several Europeans living on many of the islands.

Murty et al.; (2005)[24] claim that it is almost impossible for a trans-oceanic tsunami to be generated in the basin of the Atlantic Ocean, which if correct supports the work by many other researchers that if the western flank of the Cumbre Vieja did fail it is unlikely to generate a "mega-tsunami."

Pérez-Torrado et al.; (2006)[25] indicate that marine deposits located between 41 and 188 m above sea level in the Agaete Valley of Gran Canaria resulted when ~3 x 1010 m3 - one order of magnitude less than that of models of Day et al.; (1999),[6] Ward and Day, (2001);[7] and Ward and Day, (2005),[15] of volcanic material collapsed forming the Güimar Valle on Tenerife ~830 ka and generated a tsunami. They indicate that the only plausible source is that collapse, and also report that there is no indication that the tsunami propagated beyond Gran Canaria.

Scientists at TU Delft in the Netherlands, reported in 2006 that the section of the western flank of the Cumbre Vieja that was conjectured as potentially failing and falling into the Atlantic Ocean to create the hypothesised La Palma mega-tsunami was both too small in mass and volume, and crucially it is currently far too stable to break away within the next 10,000 years.[26]

The Tsunami Society has issued a statement of caution regarding the Ward and Day research. This is supported by research at T U Delft. The TU Delft work and the Tsunami Society paper, along with several other studies, all disagree with the geological model of Ward and Day, favouring a different collapse. The Ritter Island collapse would seem to support the claim that the collapse of the western flank on La Palma is unlikely to trigger a tsunami with the potential to cause inundation at trans-oceanic distance. The Tsunami Society also consider that the models used by Ward and Day uses propagation modelling which is better suited to tsunamis generated by subduction zone (mega-thrust) earthquakes. Research continues.

Historical "mega-tsunamis"

On 9 July 1958 a 7.9 magnitude earthquake and landslide released ~3.1 x 107 m3 of rock and debris in Crillon Inlet at the head of Lituya Bay, Alaska. The mass impacted the water with a force of ~8.8 x 1010 N m2 and this generated a massive plume and surge - (which has since become known as the Lituya Bay 'mega-tsunami'), with an estimated initial height of about 300 metres (980 ft). As the water collapsed it generated a wave which then surged onto the headland opposite, rising to a height of approximately 520 metres (1,710 ft), stripping trees and soil from the headland as it flowed over the headland. As it flowed away from its origin it inundated the entire bay, destroyed two fishing boats and damaged a third (by ripping its anchor from the housing within the boat), that were anchored there, killing two people. According to eye-witness accounts (Ulrich and son, reported in Miller 1960), the wave as it approached their fishing boat had an amplitude of about ~30 metres (98 ft). Once the wave reached the open sea, however, it rapidly dissipated.[27][28][29] It was the confining geography of Crillon Inlet and Lituya Bay that created the conditions that caused the initial impact plume to surge onto the headland opposite the impact site and this surge could only dissipate by moving away from the source - down Lituya Bay where it was constrained by the narrow profile of the bay. It remains the highest recorded surge, but was not a tsunami nor a mega-tsunami, despite some workers claiming it is - e.g., McGuire, in: BBC 2 TV. 2000. Transcript "Mega-tsunami; Wave of Destruction". Horizon. First screened 21.30, Thursday, 12 October 2000.

On 9 October 1963, a mass of rock, soil and other debris estimated at 2.6 x 108 m3, slid in a massive landslide off Monte Toc infilling the newly constructed Vajont Dam or Vaiont Dam in north-east Italy. It displaced ~3.0x107 m3 - about 1/5th of the water present in the reservoir, which surged over the dam wall and flooded the Piave Valley below the dam, killing over 2000 people. From the onset of the landslide to impact on the opposite side of the gorge took an estimated 45 seconds - according to seismic records.[30] By the definition of a tsunami the displacement and surge was not a tsunami, but rather a massive displacement of water with a resultant surge, it does serve to indicate how just like at Lituya Bay, massive volumes of debris can displace water. In the case of the disaster, the water behind the dam could only be displaced over the dam.

Both the Lituya Bay and Vaiont Dam incidents are examples of how large volumes of debris may cause a rapid displacement of water when they suddenly enter a body of water in a restricted area. Because the surges were only able to dissipate by moving down the Bay or over the dam they do not serve as examples of mega-tsunami generation.

In 1883 the Indonesian volcano Krakatau exploded in a cataclysmic explosive eruption. Most of the island vanished as the volcano exploded and this generated a tsunami which devastated local areas. It carried a Dutch Naval vessel, the Barouw, inland for over 5 km and left it stranded about 20 m above sea level. The tsunami itself did not propagate over trans-oceanic distances. What was noted on tide gauges around the world are considered to be the effect of the atmospheric pressure wave.[31]

During the second millennium BC, the volcano on Santorini exploded with a VEI estimated at 7. Research suggests that the eruption generated a tsunami which inundated Crete, possibly triggering the downfall of the Minoan civilization.

Lateral collapse events at stratovolcanoes, similar to the current threat posed by the western flank of Cumbre Vieja, could increase due to the physical effects of global warming on the Earth from increases in deviatoric stress from post-glacial rebound, while the size and frequency of eruptions are also likely to increase.[32][33]

References

  1. ↑ "La Palma: Synonyms and Subfeatures". Global Volcanism Program. Smithsonian Institution.
  2. ↑ "La Palma: Eruptive History". Global Volcanism Program. Smithsonian Institution.
  3. ↑ Carracedo, J.C. 1996. A simple model for the genesis of large gravitational landslide hazards in the Canary Islands. In McGuire, W: Jones, & Neuberg, J. P. (eds). Volcano Instability on the Earth and Other Planets. Geological Society, London. Special Publication, 110, 125-135.
  4. ↑ Carracedo, J. C; 1994. The Canary Islands: an example of structural control on the growth of large oceanic-island volcanoes. J. Volcanol. Geotherm Res. 60, 225-241.
  5. ↑ Carracedo, J. C; 1999. Growth, Structure, Instability and Collapse of Canarian Volcanoes and Comparisons with Hawaiian Volcanoes. J. Volcanol. Geotherm. Res. 94, 1-19.
  6. 1 2 3 4 5 6 7 Day, S. J; Carracedo, J. C; Guillou, H. & Gravestock, P; 1999. Recent structural evolution of the Cumbre Vieja volcano, La Palma, Canary Islands: volcanic rift zone re-configuration as a precursor to flank instability. J. Volcanol. Geotherm Res. 94, 135-167.,
  7. 1 2 3 4 5 Ward, S. N; & Day, S. J; 2001. Cumbre Vieja Volcano; potential collapse and tsunami at La Palma, Canary Islands. Geophys. Res. Lett. 28-17, 3397-3400. http://www.es.ucsc.edu/~ward/papers/La_Palma_grl.pdf
  8. ↑ Siebert, L; 1984. Large volcanic debris avalanches: characteristics of source areas, deposits and associated eruptions. J. Volcanol. Geotherm Res. 22, 163-197.
  9. 1 2 3 4 5 6 Bonelli-Rubio, J. M; 1950. Contribucion al estudio de la erupcion del Nambroque o San Juan. Madrid: Inst. Geografico y Catastral, 25 pp.
  10. ↑ Ortiz, J. R., & Bonelli Rubio, J. M; 1951. La erupción del Nambroque (Junio-Agosto de 1949). Madrid: Talleres del Instituto Geográfico y Catastral, 100 pp.
  11. ↑ Klügel, A; Schmincke, H –U; White, J. D. L; and Hoernle, K. A; 1999. Chronology and volcanology of the 1949 multi-vent rift-zone eruption on La Palma (Canary Islands). J. Volcanol. Geotherm. Res. 94, 267-282.
  12. ↑ Newhall, C. G.; Self, S; 1982. The Volcanic Explosivity Index (VEI): An Estimate of Explosive Magnitude for Historical Volcanism. Journal of Geophysical Research 87 (C2): 1231–1238. Bibcode:1982JGR....87.1231N. doi:10.1029/JC087iC02p01231.
  13. ↑ BBC 2 TV. 2000. Transcript "Mega-tsunami; Wave of Destruction". Horizon. First screened 21.30, Thursday, 12 October 2000.
  14. ↑ BBC 2 TV "Could we survive a Mega-Tsunami?" First screened 21:00, Thursday 18 April 2013.
  15. 1 2 3 Ward, S. N. & Day, S. J; 2005. Tsunami Thoughts. Recorder - Canadian Soc. Explor. Geophysics. 30, 38-44.
  16. ↑ Pararas-Carayannis, G; 2002. Evaluation of the Threat of Mega Tsunami Generation from Postulated Massive Slope Failure of Island Stratovolcanoes on La Palma, Canary Islands, and on The Island of Hawaii. Science of Tsunami Hazards, Vol 20, No.5, pp 251-277.
  17. ↑ Rihm, R; Krastel, S., CD109 Shipboard Scientific Party. 1998. Volcanoes and landslides in the Canaries. National Environment Research Council News. Summer, 16-17.
  18. ↑ Moore, J. G. 1964. Giant Submarine Landslides on the Hawaiian Ridge. US Geologic Survey Professional Paper 501-D, D95-D98.
  19. ↑ Moss, J. L; McGuire, W. J; and Page, D; 1999. Ground deformation monitoring of a potential landslide at La Palma, Canary Islands. J. Volcanol. Geotherm. Res. 94, 251-265.
  20. ↑ Carracedo, J. C; Badiola, E. R; Guillou, H; de la Nuez, J; and Pérez Torrado, F. J; 2001. Geology and Volcanology of La Palma and El Hierro, Western Canaries. Estudios Geol. 57, (5-6) 175-273.
  21. ↑ Pararas-Carayannis, G. 2002. Evaluation of the Threat of Mega Tsunami Generation From Postulated Massive Slope Failure Of Island StratoVolcanoes On La Palma, Canary Islands and on the Island of Hawaii. Sci. Tsunami Haz. 20-5, 251-277.
  22. ↑ Ward, S. N. & Day, S; 2003. Ritter Island Volcano - lateral collapse and the tsunami of 1888. Geophys. J. Int. 154, 891 - 902
  23. ↑ Cooke, R. J. S; 1981. Eruptive history of the volcano at Ritter Island, in Cooke-Ravian Volume of Volcanological Papers, pp. 115-123, ed. Johnson, R. W; Geological Survey Papua New Guinea, Memoir 10.
  24. ↑ Murty, T. S; Nirupama, N; Nistor, I; and Rao, A. D; 2005. Why the Atlantic Generally cannot generate trans-oceanic tsunamis? ISET J. of Earthquake Tech. Tech. Note., 42, No. 4, pp 227-236.
  25. ↑ Pérez-Torrado, F. J; Paris, R; Cabrera, M. C; Schneider, J-L; Wassmer, P; Carracedo, J. C; Rodríguez-Santana, A; & Santana, F; 2006. Tsunami deposits related to flank collapse in oceanic volcanoes: The Agaete Valley evidence, Gran Canaria, Canary Islands. Marine Geol. 227, 135-149.
  26. ↑ http://www.tudelft.nl/fileadmin/UD/MenC/Support/Internet/TU_Website/TU_Delft_portal/Actueel/Magazines/Delft_Integraal/archief/2006_DI/2006-3/achtergrond/doc/LaPalma.pdf
  27. ↑ Miller, D. J; 1960a. The Alaska earthquake of July 10, 1958: giant wave in Lituya Bay. Bull. Seismol. Soc. Amer., 50(2), 253–266.
  28. ↑ Miller, D. J; 1960b. Giant Waves in Lituya Bay Alaska - Shorter Contributions to General Geology. Geol. Surv. Prof. Pap. 354-C. USGS.
  29. ↑ Pararas-Carayannis, G; 1999. "The mega-tsunami of July 9, 1958 in Lituya Bay, Alaska. Analyis of mechanism. Excerpts from Presentation at the Tsunami Symposium of Tsunami Society of May 25–27, 1999, in Honolulu, Hawaii. USA." Website http://www.drgeorgepc.com/Tsunami1958LituyaB.html accessed 29 August 2015.
  30. ↑ Ward, S. N; & Day, S; 2011. The 1963 Landslide and Flood at Vaiont Reservoir, Italy. A tsunami ball simulation. Ital. J. Geosci. (Boll. Soc. Geol. It.), 130, 1. 16-26. doi:10.3301/IJG.2010.21
  31. ↑ Symons, G.J. (ed) "The Eruption of Krakatoa and Subsequent Phenomena - Report of the Krakatoa Committee of the Royal Society". London, 1888
  32. ↑ Tuffen, H. (May 2010). "How will melting of ice affect volcanic hazards in the twenty-first century?". Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences. 368 (1919): 2535–58. Bibcode:2010RSPTA.368.2535T. doi:10.1098/rsta.2010.0063. PMID 20403841.
  33. ↑ Deeming, K. R.; McGuire, B.; Harrop, P. (May 2010). "Climate forcing of volcano lateral collapse: evidence from Mount Etna, Sicily". Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences. 368 (1919): 2559–77. Bibcode:2010RSPTA.368.2559D. doi:10.1098/rsta.2010.0054. PMID 20403842.

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