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1815 eruption of Mount Tambora

Coordinates: 8°15′S 118°00′E / 8.25°S 118.00°E / -8.25; 118.00
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1815 eruption of Mount Tambora
Impact range of the 1815 Tambora Explosion
VolcanoMount Tambora
Start date1812[1]
End date15 July 1815[1]
TypeUltra-Plinian
LocationSumbawa, Lesser Sunda Islands, Dutch East Indies (now Indonesia)
8°15′S 118°00′E / 8.25°S 118.00°E / -8.25; 118.00
Volume37–45 km3 (8.9–10.8 cu mi)
VEI7
Impact10,000 to 11,000 deaths from direct volcanic effects; 49,000 to 90,000 deaths from post-eruption famine and epidemic diseases on Sumbawa, Lombok and Bali; reduced global temperatures in the following year which led to famine in numerous regions

Mount Tambora is a volcano on the island of Sumbawa in present-day Indonesia, then part of the Dutch East Indies,[2] and its 1815 eruption was the most powerful volcanic eruption in recorded human history. This volcanic explosivity index (VEI) 7 eruption ejected 37–45 km3 (8.9–10.8 cubic miles) of dense-rock equivalent (DRE) material into the atmosphere,[3] and was the most recent confirmed VEI-7 eruption.[4]

Although the Mount Tambora eruption reached a violent climax on 10 April 1815,[5] increased steaming and small phreatic eruptions occurred during the next six months to three years. The ash from the eruption column dispersed around the world and lowered global temperatures in an event sometimes known as the Year Without a Summer in 1816.[6] This brief period of significant climate change triggered extreme weather and harvest failures in many areas around the world. Several climate forcings coincided and interacted in a systematic manner that has not been observed after any other large volcanic eruption since the early Stone Age.

Chronology of the eruption

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Current topography of Sumbawa, Mt Tambora in the centre, the largest mountain
The estimated volcanic ashfall regions during the 1815 eruption. The red areas show thickness of volcanic ash fall. The outermost region (1 cm (1⁄2 in) thickness) reached Borneo and Sulawesi.

Mount Tambora experienced several centuries of dormancy before 1815, caused by the gradual cooling of hydrous magma in its closed magma chamber.[7] Inside the chamber at depths between 1.5 and 4.5 km (5,000 and 15,000 ft), the exsolution of a high-pressure fluid magma formed during cooling and crystallisation of the magma. An over-pressurization of the chamber of about 4,000–5,000 bar (400–500 MPa; 58,000–73,000 psi) was generated, with the temperature ranging from 700–850 °C (1,290–1,560 °F).[7] In 1812, the volcano began to rumble and generated a dark cloud.[8] On 5 April 1815, a giant eruption occurred, followed by thunderous detonation sounds heard in Makassar on Sulawesi 380 km (240 mi) away, Batavia (now Jakarta) on Java 1,260 km (780 mi) away, and Ternate on the Molucca Islands 1,400 km (870 mi) away. On the morning of 6 April, volcanic ash began to fall in East Java with faint detonation sounds lasting until 10 April. What was first thought to be the sound of firing guns was heard on 10 April in Trumon, Sumatra, more than 2,600 km (1,600 mi) away.[9] New analysis and agreements in dates suggest the rumbles of Tambora were heard even further in Nong Khai at 3352 km (2061 miles) away, Vientiane at 3368 km (2072 miles) away, and perhaps Mukdahan at 3117 km (1919 miles) away.[10]

At about 19:00 on 10 April, the eruptions intensified.[8] Three plumes rose up and merged.[9]: 249  The whole mountain was turned into a flowing mass of "liquid fire".[9]: 249  Pumice stones of up to 20 cm (8 in) in diameter started to rain down around 20:00, followed by ash at around 21:00–22:00. Soon after, a violent whirlwind ensued, which hit the village of Saugur (now Sangar), blowing down nearly every house and carrying everything it encountered into the air, including large trees.[11] Pyroclastic flows cascaded down the mountain to the sea on all sides of the peninsula, wiping out the village of Tambora, and affecting a total area on land of about 874 km2 (337 sq mi).[12][13] A moderate-sized tsunami struck the shores of various islands in the Indonesian archipelago on 10 April, with a height of up to 4 m (13 ft) in Sanggar around 22:00.[8] A tsunami of 1–2 m (3–7 ft) in height was reported in Besuki, East Java, before midnight, and one of 2 m (7 ft) in height in the Molucca Islands. The total death toll has been estimated to be around 4,600.[12] Loud explosions were heard until the next evening, 11 April. The ash veil spread as far as West Java and South Sulawesi. A nitrous odor was noticeable in Batavia, and heavy tephra-tinged rain fell, finally receding between 11 and 17 April.[8]

The first explosions were heard on this Island in the evening of 5 April, they were noticed in every quarter, and continued at intervals until the following day. The noise was, in the first instance, almost universally attributed to distant cannon; so much so, that a detachment of troops was marched from Djocjocarta, in the belief that a neighbouring post was being attacked, and along with the coast, boats were in two instances dispatched in quest of a supposed ship in distress.

—Sir Stamford Raffles' memoir.[9]: 241 

The explosion had an estimated VEI of 7.[14] An estimated 41 km3 (10 cu mi) of pyroclastic trachyandesite were ejected, weighing about 10 billion tonnes. This left a caldera measuring 6–7 km (3+1⁄2–4+1⁄2 mi) across and 600–700 m (2,000–2,300 ft) deep.[8] The density of fallen ash in Makassar was 636 kg/m3 (39.7 lb/cu ft).[15] Before the explosion, Mount Tambora's peak elevation was about 4,300 m (14,100 ft),[8] making it one of the tallest peaks in the Indonesian archipelago. After the explosion, its peak elevation had dropped to only 2,851 m (9,354 ft), about two-thirds of its previous height.[16]

The 1815 Tambora eruption is the largest observed eruption in recorded history, as shown in the table below.[8][4] The explosion was heard at least 2,600 km (1,600 mi) away[11] and possibly over 3350 km (2060 mi) away,[10] and ash fell at least 1,300 km (810 mi) away.[8]

Aftermath

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On my trip towards the western part of the island, I passed through nearly the whole of Dompo and a considerable part of Bima. The extreme misery to which the inhabitants have been reduced is shocking to behold. There were still on the road side the remains of several corpses, and the marks of where many others had been interred: the villages almost entirely deserted and the houses fallen down, the surviving inhabitants having dispersed in search of food. ... Since the eruption, a violent diarrhoea has prevailed in Bima, Dompo, and Sang'ir, which has carried off a great number of people. It is supposed by the natives to have been caused by drinking water which has been impregnated with ashes; and horses have also died, in great numbers, from a similar complaint.

—Lt. Philips, ordered by Sir Stamford Raffles to go to Sumbawa.[9]: 248–249 

All vegetation on the island was destroyed. Uprooted trees, mixed with pumice ash, washed into the sea and formed rafts up to five km (three mi) across.[8] Between 1 and 3 October the British ships Fairlie and James Sibbald encountered extensive pumice rafts about 3,600 km (2,200 mi) west of Tambora.[17] Clouds of thick ash still covered the summit on 23 April. Explosions ceased on 15 July, although smoke emissions were observed as late as 23 August. Activity resumed in August 1819—a small eruption with "flames" and rumbling aftershocks, and was considered to be part of the 1815 eruption.[4] This eruption was recorded at 2 on the VEI scale.

The yellow skies typical of summer 1815 had a profound impact on the paintings of J. M. W. Turner

The eruption column reached the stratosphere at an altitude of more than 43 km (141,000 ft).[4] The coarser ash particles settled out one to two weeks after the eruptions, but the finer ash particles stayed in the atmosphere from a few months to a few years at altitudes of 10–30 km (33,000–98,000 ft).[8] Longitudinal winds spread these fine particles around the globe, creating optical phenomena. Prolonged and brilliantly coloured sunsets and twilights were seen frequently in London between 28 June and 2 July 1815 and 3 September and 7 October 1815.[8] The glow of the twilight sky typically appeared orange or red near the horizon and purple or pink above.

The estimated number of deaths varies depending on the source. Zollinger (1855) puts the number of direct deaths at 10,000, probably caused by pyroclastic flows. On Sumbawa, 18,000 starved to death or died of disease. About 10,000 people on Lombok died from disease and hunger.[18] Petroeschevsky (1949) estimated that about 48,000 people were killed on Sumbawa and 44,000 on Lombok.[19] Stothers in 1984 and several other authors have accepted Petroeschevsky's claim of 88,000 deaths in total.[8] However, a 1998 journal article authored by J. Tanguy and others claimed that Petroeschevsky's figures were unfounded and based on untraceable references.[20] Tanguy's revision of the death toll was based on Zollinger's work on Sumbawa for several months after the eruption and on Thomas Raffles's notes.[9] Tanguy pointed out that there may have been additional victims on Bali and East Java because of famine and disease. Their estimate was 11,000 deaths from direct volcanic effects and 49,000 by post-eruption famine and epidemic diseases.[20] Oppenheimer wrote that there were at least 71,000 deaths in total.[4] Reid has estimated that 100,000 people on Sumbawa, Bali, and other locations died from the direct and indirect effects of the eruption.[21]

Disruption of global temperatures

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The eruption caused a volcanic winter. During the Northern Hemisphere summer of 1816, global temperatures cooled by 0.53 °C (0.95 °F). This cooling directly or indirectly caused 90,000 deaths. The eruption of Mount Tambora was the largest cause of this climate anomaly.[22] While there were other eruptions in 1815, Tambora is classified as a VEI-7 eruption with a column 45 km (148,000 ft) tall, eclipsing all others by at least one order of magnitude.

The VEI is used to quantify the amount of ejected material, with a VEI-7 being 100 km3 (24 cu mi). Every index value below that is one order of magnitude (meaning ten times) less. Furthermore, the 1815 eruption occurred during a Dalton Minimum, a period of unusually low solar radiation.[23] Volcanism plays a large role in climate shifts, both locally and globally. This was not always understood and did not enter scientific circles as fact until the 1883 eruption of Krakatoa tinted the skies orange.[22]

The scale of the volcanic eruption will determine the significance of the impact on climate and other chemical processes, but a change will be measured even in the most local of environments. When volcanoes erupt, they eject carbon dioxide (CO2), water, hydrogen, sulfur dioxide (SO2), hydrogen chloride, hydrogen fluoride, and many other gases (Meronen et al. 2012). CO2 and water are greenhouse gases, which comprise 0.0415 percent and 0.4 percent of the atmosphere, respectively. Their small proportion disguises their significant role in trapping solar radiation and reradiating it back to Earth.

Global effects

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See also: Year Without a Summer
Sulfate concentration in ice core from Central Greenland, dated by counting oxygen isotope seasonal variations: An unknown eruption occurred around the 1810s.[24]

The 1815 eruption released SO2 into the stratosphere, causing a global climate anomaly. Different methods have estimated the ejected sulfur mass during the eruption: the petrological method; an optical depth measurement based on anatomical observations; and the polar ice core sulfate concentration method, using cores from Greenland and Antarctica. The figures vary depending on the method, ranging from 10 to 120 million tonnes.[4]

In the northern spring and summer of 1815, a persistent "dry fog" was observed in the northeastern United States. The fog reddened and dimmed the sunlight, such that sunspots were visible to the naked eye. Neither wind nor rainfall dispersed the "fog". It was identified as a stratospheric sulfate aerosol veil.[4] In summer 1816, countries in the Northern Hemisphere suffered extreme weather conditions, dubbed the "Year Without a Summer". Average global temperatures decreased by about 0.4 to 0.7 °C (0.7 to 1.3 °F),[8] enough to cause significant agricultural problems around the globe. On 4 June 1816, frosts were reported in the upper elevations of New Hampshire, Maine (then part of Massachusetts), Vermont, and northern New York. On 6 June 1816, snow fell in Albany, New York and Dennysville, Maine.[4] On 8 June 1816, the snow cover in Cabot, Vermont was reported still to be 46 cm (18 in) deep.[25] Such conditions occurred for at least three months and ruined most agricultural crops in North America. Canada experienced extreme cold during that summer. Snow 30 cm (12 in) deep accumulated near Quebec City from 6 to 10 June 1816.

The second-coldest year in the Northern Hemisphere since around 1400 was 1816, and the 1810s are the coldest decade on record. That was the consequence of Tambora's 1815 eruption and possibly another VEI-6 eruption in late 1808. The surface temperature anomalies during the summer of 1816, 1817, and 1818 were −0.51 °C (−0.92 °F), −0.44 °C (−0.79 °F), and −0.29 °C (−0.52 °F), respectively.[14] Parts of Europe also experienced a stormier winter.[citation needed]

This climate anomaly has been blamed for the severity of typhus epidemics in southeast Europe and along the eastern Mediterranean Sea between 1816 and 1819.[4] The climate changes disrupted the Indian monsoons, caused three failed harvests and famine, and contributed to the spread of a new strain of cholera that originated in Bengal in 1816.[26] Many livestock died in New England during the winter of 1816–1817. Cool temperatures and heavy rains resulted in failed harvests in the British Isles. Families in Wales travelled long distances as refugees, begging for food. Famine was prevalent in north and southwest Ireland, following the failure of wheat, oat, and potato harvests. The crisis was severe in Germany, where food prices rose sharply, and demonstrations in front of grain markets and bakeries, followed by riots, arson, and looting, took place in many European cities. It was the worst famine of the 19th century.[4]

Effects of volcanism

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Volcanism affects the atmosphere in two distinct ways: short-term cooling caused by reflected insolation and long-term warming from increased CO2 levels. Most of the water vapor and CO2 is collected in clouds within a few weeks to months because both are already present in large quantities, so the effects are limited.[27] It has been suggested that a volcanic eruption in 1809 may also have contributed to a reduction in global temperatures.[24]

Impact of the eruption

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By most calculations, the eruption of Tambora was at least a full order of magnitude (10 times) larger than that of Mount Pinatubo in 1991.(Graft et al. 1993)[citation needed] Its energy release was equivalent to about 33 gigatons of TNT (1.4×1020 J).[28] An estimated 1,220 m (4,000 ft) of the top of the mountain collapsed to form a caldera, reducing the height of the summit by a third. Around 100 km3 (24 cu mi) of rock was blasted into the air.(Williams 2012)[citation needed] Toxic gases also were pumped into the atmosphere, including sulfur that caused lung infections.(Cole-Dai et al. 2009)[citation needed] Volcanic ash was over 100 cm (40 in) deep within 75 km (45 mi) of the eruption, while areas within a 500 km (300 mi) radius saw a 5 cm (2 in) ash fall, and ash could be found as far away as 1,300 km (810 mi).[4] The ash burned and smothered crops, creating an immediate shortage of food in Indonesia.(Cole-Dai et al. 2009)[citation needed] The ejection of these gases, especially hydrogen chloride, caused the precipitation to be extremely acidic, killing much of the crops that survived or were rebudding during the spring. The food shortages were compounded by the Napoleonic wars, floods, and cholera.[4]

The ash in the atmosphere for several months after the eruption reflected significant amounts of solar radiation, causing unseasonably cool summers that contributed to food shortages.[4] China, Europe, and North America had well-documented below normal temperatures, which devastated their harvests. The monsoon season in China and India was altered, causing flooding in the Yangtze Valley and forcing thousands of Chinese to flee coastal areas. (Granados et al. 2012)[citation needed] The gases also reflected some of the already-decreased incoming solar radiation, causing a 0.4 to 0.7 °C (0.7 to 1.3 °F) decrease in global temperatures throughout the decade. An ice dam formed in Switzerland during the summers of 1816 and 1817, earning 1816 the title "Year without a Summer".[27] The winter months of 1816 were not much different from previous years, but the spring and summer maintained the cool-to-freezing temperatures. The winter of 1817, however, was radically different, with temperatures below −34 °C (−30 °F) in central and northern New York, which were cold enough to freeze lakes and rivers that were normally used to transport supplies. Both Europe and North America suffered from freezes lasting well into June, with snow accumulating to 32 cm (13 in) in August, which killed recently planted crops and crippled the food industry. The length of the growing seasons in parts of Massachusetts and New Hampshire were less than 80 days in 1816, resulting in harvest failures (Oppenheimer 2003). Visually unique sunsets were observed in western Europe, and red fog was observed along the eastern coast of the U.S. These unique atmospheric conditions persisted for the better part of 2.5 years.(Robock 2000)[citation needed]

Scientists have used ice cores to monitor atmospheric gases during the cold decade (1810–1819), and the results have been puzzling. The sulfate concentrations found in both Siple Station, Antarctica and central Greenland bounced from 5.0[clarification needed] in January 1816 to 1.1[clarification needed] in August 1818.[24] This means that 25–30 teragrams of sulfur were ejected into the atmosphere, most of which came from Tambora, followed by a rapid decrease through natural processes. Tambora caused the largest shift in sulfur concentrations in ice cores for the past 5,000 years. Estimates of the sulfur yield vary from 10 teragrams (Black et al. 2012)[citation needed] to 120 teragrams,(Stothers 2000)[citation needed] with the average of the estimates being 25–30 teragrams. The high concentrations of sulfur could have caused a four-year stratospheric warming of around 15 °C (27 °F), resulting in a delayed cooling of surface temperatures that lasted for nine years.(Cole-Dai et al. 2009)[citation needed] This has been dubbed a "volcanic winter", similar to a nuclear winter because of the overall decrease in temperatures and abysmal farming conditions.[4]

Climate data have shown that the variance between daily lows and highs may have played a role in the lower average temperature because the fluctuations were much more subdued. Generally, the mornings were warmer because of nightly cloud cover and the evenings were cooler because the clouds had dissipated. There were documented fluctuations of cloud cover for various locations that suggested it was a nightly occurrence and the sun killed them off, much like a fog.[4] The class boundaries between 1810 and 1830 without volcanically perturbed years was around 7.9 °C (14.2 °F). In contrast, the volcanically perturbed years (1815–1817) had a change of only around 2.3 °C (4.1 °F). This meant that the mean annual cycle in 1816 was more linear than bell shaped and 1817 endured cooling across the board. Southeastern England, northern France, and the Netherlands experienced the greatest amount of cooling in Europe, accompanied by New York, New Hampshire, Delaware, and Rhode Island in North America.[27] The documented rainfall was as much as 80 percent more than the calculated normal with regards to 1816, with unusually high amounts of snow in Switzerland, France, Germany, and Poland. This is again contrasted by the unusually low precipitations in 1818, which caused droughts throughout most of Europe and Asia.(Auchmann et al. 2012)[29] Russia had already experienced unseasonably warm and dry summers since 1815 and this continued for the next three years. There are also documented reductions in ocean temperature near the Baltic Sea, the North Sea, and the Mediterranean Sea. This seems to have been an indicator of shifted oceanic circulation patterns and possibly changed wind direction and speed.(Meronen et al. 2012)[citation needed]

Taking into account the Dalton Minimum and the presence of famine and droughts predating the eruption, the Tambora eruption accelerated or exacerbated the extreme climate conditions of 1815. While other eruptions and other climatological events would have led to a global cooling of about 0.2 °C (0.4 °F), Tambora increased on that benchmark substantially.[24]

Comparison of selected volcanic eruptions

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Comparison of selected volcanic eruptions within the last 2000 years
Eruptions Country Location Year Column
height (km)		  Volcanic
Explosivity Index 		 N. Hemisphere
summer anomaly (°C)		 Fatalities
Eruption of Mount Vesuvius in 79 AD Italy Mediterranean Sea 79 30 5 Unlikely 02001>2,000
Hatepe (Taupo) New Zealand Ring of Fire 232 51 7 ? 000000
946 eruption of Paektu Mountain China / North Korea Ring of Fire 946 36 6 ? 00000?
1257 Samalas eruption Indonesia Ring of Fire 1257 40 7 −2.0 ??
1600 eruption of Huaynaputina Peru Ring of Fire 1600 46 6 −0.8 01400≈1,400
1815 eruption of Mount Tambora Indonesia / Dutch East-Indies Ring of Fire 1815 43 7 −0.5 >71,000-121,000
1883 eruption of Krakatoa Indonesia / Dutch East-Indies Ring of Fire 1883 27 6 −0.3 3600036,600
1902 eruption of Santa María Guatemala Ring of Fire 1902 34 6 no anomaly 070017,000–13,000
1912 eruption of Novarupta United States, Alaska Ring of Fire 1912 32 6 −0.4 000022
1980 eruption of Mount St. Helens United States, Washington Ring of Fire 1980 19 5 no anomaly 0005757
1982 eruption of El Chichón Mexico Ring of Fire 1982 32 4–5 ? 02001>2,000
1985 eruption of Nevado del Ruiz Colombia Ring of Fire 1985 27 3 no anomaly 2300023,000
1991 eruption of Mount Pinatubo Philippines Ring of Fire 1991 34 6 −0.5 847847
2022 Hunga Tonga–Hunga Haʻapai eruption and tsunami Tonga Ring of Fire 2022 55 5 +0.035[30] 020015

Source: Oppenheimer (2003),[4] and Smithsonian Global Volcanism Program for VEI.[31]

See also

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References

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Public Domain This article incorporates public domain material from websites or documents of the United States Geological Survey.

  1. ^ a b "Tambora". Global Volcanism Program. Smithsonian Institution. Retrieved 2022-02-08.
  2. ^ * Hägerdal, Hans (2017), Held's History of Sumbawa. Amsterdam: Amsterdam University Press, p. 19-20, 141-2.[1]
  3. ^ Kandlbauer, J.; Sparks, R. S. J. (2014-10-01). "New estimates of the 1815 Tambora eruption volume". Journal of Volcanology and Geothermal Research. 286: 93–100. Bibcode:2014JVGR..286...93K. doi:10.1016/j.jvolgeores.2014.08.020. ISSN 0377-0273.
  4. ^ a b c d e f g h i j k l m n o p Oppenheimer, Clive (2003). "Climatic, environmental and human consequences of the largest known historic eruption: Tambora volcano (Indonesia) 1815". Progress in Physical Geography. 27 (2): 230–259. Bibcode:2003PrPG...27..230O. doi:10.1191/0309133303pp379ra. S2CID 131663534.
  5. ^ Earth Observatory
  6. ^ "Tambora Volcano, Indonesia". United States Geological Survey. 3 June 2002. Archived from the original on 2 June 2010. Retrieved 8 September 2010.
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  13. ^ Sutawidjaja, Igan Supriatman; Sigurdsson, Haraldur; Abrams, Lewis (2006). "Characterization of volcanic deposits and geoarchaeological studies from the 1815 eruption of Tambora volcano".
  14. ^ a b Briffa, K. R.; Jones, P. D.; Schweingruber, F. H.; Osborn, T. J. (1998). "Influence of volcanic eruptions on Northern Hemisphere summer temperature over 600 years". Nature. 393 (6684): 450–455. Bibcode:1998Natur.393..450B. doi:10.1038/30943. S2CID 4392636.
  15. ^ Richard B. Stothers (2004). "Density of fallen ash after the eruption of Tambora in 1815". Journal of Volcanology and Geothermal Research. 134 (4): 343–345. Bibcode:2004JVGR..134..343S. doi:10.1016/j.jvolgeores.2004.03.010.
  16. ^ Monk, K. A.; Fretes, Y.; Reksodiharjo-Lilley, G. (1996). The Ecology of Nusa Tenggara and Maluku. Hong Kong: Periplus Editions Ltd. p. 60. ISBN 962-593-076-0.
  17. ^ (Anon.) (August 1816). "Volcanic phenomenon". The Asiatic Journal. 2: 161.
  18. ^ Zollinger, Heinrich (1855). Besteigung des Vulkans Tamboro auf der Insel Sumbawa und Schilderung der Eruption desselben im Jahre 1815 [Ascent of the Tambora Volcano on the Island of Sumbawa and Account of its Eruption in the Year 1815] (in German). Winterthur, Switzerland: Joh. Wurster & Co. p. 20., cited by Oppenheimer (2003).
  19. ^ Petroeschevsky (1949): A contribution to the knowledge of the Gunung Tambora (Sumbawa). Tijdschrift van het K. Nederlandsch Aardrijkskundig Genootschap, Amsterdam Series 2 66, 688–703, cited by Oppenheimer (2003).
  20. ^ a b Tanguy, J. C.; Scarth, A.; Ribière, C.; Tjetjep, W. S. (1998). "Victims from volcanic eruptions: a revised database". Bulletin of Volcanology. 60 (2): 137–144. Bibcode:1998BVol...60..137T. doi:10.1007/s004450050222. S2CID 129683922.
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  22. ^ a b Alan Robock. "Volcanic eruptions and climate" (PDF). Retrieved 11 March 2016.
  23. ^ Spadin, Reto; Stickler, Alexander; Breda, L.; Bühler, M.; Spadin, R.; Stickler, A. (2012). "Extreme climate, not extreme weather: the summer of 1816 in Geneva, Switzerland". Climate of the Past. 8 (1): 325. Bibcode:2012CliPa...8..325A. doi:10.5194/cp-8-325-2012. hdl:20.500.11850/47338. Retrieved 11 March 2016.
  24. ^ a b c d Dai, Jihong; Mosley-Thompson, Ellen; Thompson, Lonnie G. (1991). "Ice core evidence for an explosive tropical volcanic eruption six years preceding Tambora". Journal of Geophysical Research: Atmospheres. 96 (D9): 17, 361–17, 366. Bibcode:1991JGR....9617361D. doi:10.1029/91jd01634.
  25. ^ "1816: The Year Without a Summer". The New England Historical Society. 6 June 2014. Retrieved 30 March 2021.
  26. ^ Peterson, Doug LAS News (Spring 2010) University of Illinois at Urbana-Champaign p. 11.
  27. ^ a b c Bodenmann, Tom; et al. (2011). "Perceiving, explaining, and observing climatic changes: An historical case study of the "year without a summer" 1816" (PDF). Meteorologische Zeitschrift. 20 (6): 577–587. Bibcode:2011MetZe..20..577B. doi:10.1127/0941-2948/2011/0288.
  28. ^ "Tambora 1815: Just How Big Was the Eruption?". Wired. Archived from the original on 2019-04-29.
  29. ^ Auchmann, R.; Brönnimann, S.; Breda, L.; Bühler, M.; Spadin, R.; Stickler, A. (24 February 2012). "Extreme climate, not extreme weather: The summer of 1816 in Geneva, Switzerland". Climate of the Past. 8 (1): 325–335. Bibcode:2012CliPa...8..325A. doi:10.5194/cp-8-325-2012. hdl:20.500.11850/47338.
  30. ^ Jenkins, S., Smith, C., Allen, M. et al. Tonga eruption increases chance of temporary surface temperature anomaly above 1.5 °C. Nat. Clim. Chang. 13, 127–129 (2023). https://doi.org/10.1038/s41558-022-01568-2
  31. ^ "Large Holocene Eruptions". Global Volcanism Program. Smithsonian Institution. Archived from the original on 17 January 2012. Retrieved 7 November 2006.
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