1996 eruption of Gjálp

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Coordinates: 64°32′00″N 17°25′00″W / 64.53333°N 17.41667°W / 64.53333; -17.41667
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1996 eruption of Gjálp
Hringvegur partially destroyed
Map
Geological map of subglacial Gjálp ridge (red outline). Shading shows:   subglacial terrain above 1,100 m (3,600 ft),  seismically active areas between 1995 to 2007,   calderas,  central volcanoes and   fissure swarms. Clicking on the image enables fll window and mouse-over with more detail.[4][5]
Vatnajökull: In the western part to be seen are the Grímsvötn caldera (dark half-moon indentation), to the north of it Gjálp, and to the north of Gjálp the completely subglacial caldera of Bárðarbunga
Icelandic rift zones and Vatnajökull: East Volcanic Zone (no. 4) crossing its western part

Gjálp (Icelandic pronunciation: [ˈcaul̥p]) is a hyaloclastite ridge (tindar) in Iceland under the Vatnajökull glacier shield. Its present form resulted from an eruption series in 1996 and it is probably part of the Grímsvötn volcanic system.[6][7] However not all the scientists were of this opinion, as seismic studies are consistent with a 10 km (6.2 mi) lateral dike intrusion at about 5 km (3.1 mi) depth from Bárðarbunga being the trigger event. This does not exclude a shallower secondary intrusion from Grímsvötn being important in the subaerial eruption itself.[8][a]

Importance

The eruption was of importance, because it was for the first time that a subglacial eruption under a thick ice cover as well as the connected jökulhlaup could be observed and analyzed by modern technique.[10][11]

Geography

Eruption location

The

Hamarinn central volcano of the Bárðarbunga volcanic system which has the Loki Ridge extending west-east which has been assigned historically to the Loki-Fögrufjöll volcano.[4]

Vatnajökull ice cap

The

glaciation. Its last advance took place during the so called Little Ice Age from the 13th to the end of the 19th century and since then it is retreating.[13]

Parts of two volcanic zones of Iceland are placed under Vatnajökull, ie. the very active

Öraefi Volcanic Belt, a flank zone mostly under the eastern part of Vatnajökull.[13][17] It is thought that due to climate change, Vatnajökull has lost about 10% of its mass since the end of the 19th century. Measurements showed an accentuated and even accelerating rate of glacio-isostatic uplift.[15] This could lead to increased magma production (so called decompression melt production), because the "pot lid" formed by the glaciers and their weight will be absent in the future, and eruption frequency could increase as a consequence.[18]

The region of the Gjálp fissures is part of this active East Volcanic Zone under Vatnajökull.

Geology

This kind of eruption, but under a glacier shield
Ice cauldrons merging to form an ice canyon at the glacier covered Colombian volcano Nevado del Tolima
Bárðarbunga-Veiðivötn volcanic system not far from Landmannalaugar

The Gjálp eruption formed in about two weeks a subglacial

DRE.[2]

The eruption in 1996

Precursors and possible connection between volcanic systems

Some large

M5+) had taken place in the central volcano Bárðarbunga just before the eruption and proved to be precursors of the eruptive events. In particular a Mw5.6 event took place on the 29th September in the northern part of the Bárðarbunga caldera and its aftershock sequence propagated over the next two days in a linear fashion towards Grímsvötn.[19] It is possible that the first large event was associated with a subglacial eruption within the Bárðarbunga caldera a couple of days before the Gjálp eruption.[8] The seismological study sees a parallel to the 2014–2015 eruptions and to the caldera drop in Bárðarbunga central volcano in that eruption, and postulate a similar magma migration to the eruption site though on a smaller scale. This could mean that the volcano is part of the fissure system of Bárðarbunga, not Grímsvötn.[8] There had been seismic studies that suggested an east west line of seismic activity in the Bárðarbunga volcanic system at the Loki Ridge intersected the eruption location,[5] but the Loki Ridge was not seismically active during the eruption.[8]

Another possibility is that Bárðarbunga magma entered a portion the magmatic system of Grímsvötn and started the eruption by this

intrusion. Bárðarbunga is known for such tendencies, as its magma mingled with Torfajökull magma at least three times in the past which resulted in bimodal eruptions, e.g. of the Veiðivötn and at Landmannalaugar by the end of the 15th century.[20]

Formation of the tindar volcano

The Gjálp

fissure under 550–700 m (1,800–2,300 ft) of glacier ice within Vatnajökull. The eruption in October 1996 could push through this ice in about 30 hours[6] and took place from 30 September to 13 October 1996. The eruption fissure had a length of 6–7 km (3.7–4.3 mi).[1]

The location is some kilometers to the north of Grímsvötn caldera.[6]

In the beginning, a 2–4 km (1.2–2.5 mi) long N–S trending depression was formed above the fissure, with time three ice cauldrons were built at each end and in the middle,[1] but the eruption concentrated later on one of them where a 200–300 m (660–980 ft) wide crater came to light. After some time, an open ice canyon was built above the fissure. It had a length of about 3.5 km (2.2 mi) and was up to 500 m (1,600 ft) in width.[6]

The meltwater drained first through the ice canyon and then disappeared into subglacial channels and run from there to the subglacial caldera lake of Grímsvötn.[6] The subglacial channels were easily recognized, because continuous melting caused by the hot water from the eruption site initiated the formation of depressions on the ice surface. And so the scientists followed the melting path down to Grímsvötn caldera.[1]

Though the eruption was mostly

ice flow into the crater.[6]

During the two weeks of eruption, volcanic activity thawed no less than 3 km3 (0.72 cu mi) of ice, and this continued to a lesser extent for some time after the end of the eruption.[6]

The newly formed tindar disappeared again completely under the glacier ice about 1 year later,[6] but an identifiable ice cauldron remained until at least 2007.[2] The tindar was a 6 km (3.7 mi) long ridge newly deposited to a height of 500 m (1,600 ft) above the pre-existing bedrock with a volume of 0.7 km3 (0.17 cu mi).[2] It is postulated that the original unconsolidated hyaloclastitic volcanic glass and tephra of the ridge could have by now undergone a process called palagonitization due to hydrothermal alteration, to palagonite, a consolidated rock more resistant to erosion, but it is unknown if this has happened.[2]

Eruption products

The eruptive products consisted of predominantly basaltic andesite which surprised the scientists as these more evolved rocks are neither typical for Bárðarbunga nor for Grímsvötn, both more connected to basaltic volcanism. Some scientists thought therefore that Gjálp could be an independent volcano.[12] The bulk samples obtained shortly after the eruption ranged from basaltic andesite to basalt and were of distinctive Grímsvötn composition.[9]: 33  Basaltic andesite from a 1887 eruption had been previously attributed to the Grímsvötn volcanic system and had very similar composition.[9] Tephra assigned to the eruption has been analysed by several researchers and has composition that is Grímsvötn basaltic andesite with rarely Grímsvötn basalt. A total of three samples out of the several hundred in the literature had some tephra with Bárðarbunga basalt composition. It is unknown if this was due to contamination from pre-existing tephra layers in the ice that was overlying Gjálp or if the Bárðarbunga basalt was erupted together with the Grímsvötn basaltic andesite.[9]: 62 

Jökulhlaup in 1996

outlet glacier Svínafellsjökull
in the background
Parts of the destroyed bridge over Gígjukvísl river on Skeiðarársandur

In the beginning, scientists presumed that the eruption would be followed immediately by a big jökulhlaup (sort of a meltwater tsunami including large blocks of ice and a high quantity of sediment). But it took some time to fill the subglacial lake of Grímsvötn in such a manner that the ice wall holding it back would break.[6]

Not before some weeks had passed after the eruption was terminated, the expected jökulhlaup took place from 4 to 7 November 1996.

outlet glacier Skeiðarárjökull. There, to everybody's surprise, the water masses streamed in such a quantity that the whole glacier was lifted up.[21][22]

In the end, the water sprang up from under the glacier edge and the flood covered most of

Hringvegur
including two bridges and some communication installations. Luckily, the road had been closed before so that nobody was injured.

The volume of meltwater produced by this eruption was around 4 km3.

sandur streamed up to 50–60.000 m3/sec.[6] The first estimates had been somewhat lower.[12]

Former eruption in 1938

At more or less the same place another eruption had taken place in the 1930s. It had also caused a jökulhlaup, but at the time, science could not yet analyse the events. That eruption stayed subglacial.[6]

See also

Wikimedia Commons has media related to Grímsvötn-Gjálp eruption 1996.

Further reading

Notes

  1. ^ Despite the extensive study the precise sequence of events during the eruption has not been conclusively determined as well as assignment to volcanic system. Several authorities have speculated on the following sequence of events given evolving volcanology theory in the last decade:[9]: 62 
    1. Deep basaltic primary intrusion from Bárðarbunga system on 29th September 1996
    2. This intercepted a maturing Grímsvötn magma pocket (that may have had some active Grímsvötn basalt magma input at the time)
    3. Which was triggered into eruption 30th September 1996 onwards
    Another alternative explanation for the observations could be:
    1. Tectonic interaction along a fault that propagated from Bárðarbunga towards Grímsvötn
    2. This intercepted an almost primed maturing Grímsvötn magma pocket (that may have had some active Grímsvötn basalt magma input at the time)
    3. Which was triggered into eruption 30th September 1996 onwards
    Less consistent with the compositional studies evidence:[8]
    1. Subglacial eruption at north western part of Bárðarbunga Caldera on 29th September 1996
    2. Deep basaltic Bárðarbunga intrusion on far side of Bárðarbunga system into maturing shallower magma pocket shared with Grímsvötn system
    3. Which was triggered into eruption 30th September 1996 onwards
    Inconsistent with current compositional and seismic evidence base:
    1. Maturing shallow magma pocket in either Bárðarbunga volcanic system or its Loki-Fögrufjöll subsystem (best location data on 192 peri-eruption seismic events with good location solutions only assigned two to Loki Ridge, but perhaps there is a magma pocket under the Loki Ridge)
    2. Bárðarbunga Caldera priming event 29th September 1996
    3. Bárðarbunga volcanic system triggered into subaerial eruption 30th September 1996 onwards

References

  1. ^
    doi:10.3189/172756501781832520
    . Retrieved 8 August 2020.
  2. ^
    doi:10.1016/j.jvolgeores.2007.10.012
    .
  3. ^ "Grímsvötn". Global Volcanism Program. Smithsonian Institution.
  4. ^ a b Björnsson, H.; Einarsson, P. (1990). "Volcanoes beneath Vatnajökull, Iceland: Evidence from radio echo-sounding, earthquakes and jökulhlaups" (PDF). Jökull. 40: 147–168. Archived (PDF) from the original on 20 March 2023. Retrieved 25 March 2024.: 155 
  5. ^ a b Jakobsdóttir, S.S. (2008). "Seismicity in Iceland: 1994–2007" (PDF). Jökull. 58 (1): 75–100.: 87 
  6. ^ a b c d e f g h i j k Snæbjörn Guðmundsson: Vegavísir um jarðfræði Íslands. Reykjavík 2015, p. 280-281
  7. ^ See also "Grímsvötn:Eruptive history". Global Volcanism Program. Smithsonian Institution. Retrieved 29 August 2020.
  8. ^
    doi:10.1007/s00024-019-02387-x
    .
  9. ^ a b c d Jóngeirsdóttir, Irma Gná (2022). The tephra layer formed in the 1996 eruption of Gjálp: Dispersal and volume. Magister Scientiarum thesis (Thesis). Faculty of Earth Science School of Engineering and Natural Sciences, University of Iceland.
  10. doi:10.1007/s00445-003-0295-9
    .
  11. doi:10.3189/172756407782282534
    . Retrieved 30 August 2020.
  12. ^
    doi:10.1029/97EO00237
    . Retrieved 29 August 2020.
  13. ^
    hdl:11568/500513
    . Retrieved 8 August 2020.
  14. ^ Thordarson, Thorvaldur; Höskuldsson, Ármann (2008). "Postglacial volcanism in Iceland" (PDF). Jökull. 58. Retrieved 24 March 2024.
  15. ^ a b Friðriksdóttir, Hildur María (2017). Landris á Vatnajökulssvæðinu metið með GPS landmælingum. BS ritgerð (PDF) (Thesis) (in Icelandic). Jarðvísindadeild Háskóli Íslands. Leiðbeinendur Sigrún Hreinsdóttir, Erik Sturkell. Retrieved 24 March 2024.
  16. doi:10.1016/S0921-8181(02)00130-3
    . Retrieved 31 August 2020.
  17. ^ See also: Björnsson, Helgi; Einarsson, Páll (1990). "Volcanoes beneath Vatnajökull, Iceland. Evidence from radio echo sounding, earthquakes and jökulhlaups". Jökull. 40. Retrieved 8 August 2020.
  18. hdl:11568/500303
    . Retrieved 4 September 2020.
  19. ^ Utami, I.W. (2018). A reappraisal of seismicity recorded during the 1996 Gjalp eruption in Iceland using modern seismological methods. PhD dissertation (PDF) (Thesis) (in Chinese). National Central University, Taiwan (國立中央大學). Retrieved 24 March 2024.
  20. doi:10.1016/j.epsl.2008.02.026
    .
  21. ^ Jóhannesson, Tomas (2002). "Propagation of a subglacial flood wave during the initiation of a jôkulhlaup". Hydrological Sciences-Journal-des Sciences Hydrologiques. 47 (3). Retrieved 8 August 2020.
  22. ^ See also: Björnsson, Helgi (2010). "Understanding jökulhlaups: from tale to theory" (PDF). Journal of Glaciology. 56 (200). Retrieved 8 August 2020.
  23. ^ M.T. Gudmundsson, G. Larsen, Á. Höskuldsson and Á.G. Gylfason: Volcanic hazards in Iceland. Jökull no. 58 (2008) (PDF) Retrieved 8 August 2020.
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