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Mount Tambora

Coordinates: 8°15′S 118°0′E / 8.250°S 118.000°E / -8.250; 118.000
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Mount Tambora
Tomboro
Caldera of Mount Tambora
Highest point
Elevation2,850 m (9,350 ft)[1]
Prominence2,722 m (8,930 ft)[1][2]
Coordinates8°15′S 118°0′E / 8.250°S 118.000°E / -8.250; 118.000
Geography
Mount Tambora is located in Indonesia
Mount Tambora
Mount Tambora
Location in Indonesia
LocationBima & Dompu Regencies, Sanggar peninsula, Sumbawa, Lesser Sunda Islands, Indonesia
Geology
Rock ageLate Pleistocene-recent
Mountain typeTrachybasaltic-trachyandesitic stratovolcano
Volcanic arcSunda Arc
Last eruption1967[1]
Climbing
Easiest routeSoutheast: Doro Mboha
Northwest: Pancasila

Mount Tambora, or Tomboro, is an active stratovolcano in West Nusa Tenggara, Indonesia. Located on Sumbawa in the Lesser Sunda Islands, it was formed by the active subduction zones beneath it. Before 1815, its elevation reached more than 4,300 metres (14,100 feet) high, making it one of the tallest peaks in the Indonesian archipelago.

Tambora violently erupted in a series of eruptions beginning 5 April 1815, culminating in the largest eruption in recorded human history and the largest of the Holocene (10,000 years ago to present). The magma chamber under Tambora had been drained by previous eruptions and underwent several centuries of dormancy as it refilled. Volcanic activity reached a peak that year, culminating in an explosive eruption. The explosion was heard on Sumatra island, more than 2,600 kilometres (1,600 miles) away and possibly over 3350 km (2060 miles) away in Thailand and Laos.[3] Heavy volcanic ash rains were observed as far away as Borneo, Sulawesi, Java, and Maluku islands, and the maximum elevation of Tambora was reduced from about 4,300 to 2,850 metres (14,110 to 9,350 feet). Although estimates vary, the death toll was at least 71,000 people.[4] The eruption contributed to global climate anomalies in the following years, while 1816 became known as the "year without a summer" because of the impact on North American and European weather. In the Northern Hemisphere, crops failed and livestock died, resulting in the worst famine of the century.

Geographical setting

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Mount Tambora and its surroundings as seen from space.
View of Mount Rinjani from Mount Tambora. Viewing distance is 165 kilometres (103 mi).

Mount Tambora, also known as Tomboro,[5] is situated in the northern part of Sumbawa island, part of the Lesser Sunda Islands.[6] It is a segment of the Sunda Arc, a chain of volcanic islands that make up the southern chain of the Indonesian archipelago.[7] Tambora forms its own peninsula on Sumbawa, known as the Sanggar peninsula. To the north of the peninsula is the Flores Sea[4] and to the south is the 86 kilometres (53 mi) long and 36 kilometres (22 mi) wide Saleh Bay.[8] At the mouth of Saleh Bay there is an islet called Mojo.[9]

Besides the seismologists and vulcanologists who monitor the mountain's activity, Mount Tambora is an area of interest to archaeologists and biologists. The mountain also attracts tourists for hiking and wildlife activities,[10] though in small numbers.[11] The two nearest cities are Dompu and Bima. There are three concentrations of villages around the mountain slope. At the east is Sanggar village, to the northwest are Doro Peti and Pesanggrahan villages, and to the west is Calabai village.[12]

There are two routes of ascent to the caldera. The first begins at Doro Mboha village on the southeast of the mountain and follows a paved road through a cashew plantation to an elevation of 1,150 metres (3,770 ft). The road terminates at the southern part of the caldera, which at 1,950 metres (6,400 ft) is reachable only by hiking.[12] This location is only one hour from the caldera, and usually serves as a base camp from which volcanic activity can be monitored. The second route starts from Pancasila village at the northwest of the mountain and is only accessible on foot.[12] The 16 kilometres (9.9 mi) hike from Pancasila at 740 metres (2,430 ft) elevation to the caldera of the volcano takes approximately 14 hours with several stops (pos) en route to the top. The trail leads through dense jungle with wildlife such as Elaeocarpus, Asian water monitor, reticulated python, hawks, orange-footed scrubfowl, pale-shouldered cicadabird (Coracina dohertyi), brown and scaly-crowned honeyeater, yellow-crested cockatoo, yellow-ringed white-eye, helmeted friarbird, wild boar, Javan rusa and crab-eating macaques.[13]

History of Mount Tambora

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Geological history

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Formation

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Plate boundaries of Indonesia, with the location of Mount Tambora to the lower right of "11"

Tambora is located 340 kilometres (210 mi) north of the Java Trench system and 180 to 190 kilometres (110 to 120 mi) above the upper surface of the active north-dipping subduction zone. Sumbawa Island is flanked to the north and south by oceanic crust.[14] The convergence rate of the Australian Plate beneath the Sunda Plate is 7.8 centimetres (3.1 in) per year.[15] Estimates for the onset of the volcanism at Mount Tambora range from 57[8] to 43 ka. The latter estimate published in 2012 is based on argon dating of the first pre-caldera lava flows.[16] The formation of Tambora drained a large magma chamber pre-existing under the mountain. The Mojo islet was formed as part of this geological process in which Saleh Bay first appeared as a sea basin about 25,000 years BP.[8]

A high volcanic cone with a single central vent formed before the 1815 eruption, which follows a stratovolcano shape.[17] The diameter at the base is 60 kilometres (37 mi).[7] The volcano frequently erupted lava, which descended over steep slopes.[17] Tambora has produced trachybasalt and trachyandesite rocks which are rich in potassium. The volcanics contain phenocrysts of apatite, biotite, clinopyroxene, leucite, magnetite, olivine and plagioclase, with the exact composition of the phenocrysts varying between different rock types.[7] Orthopyroxene is absent in the trachyandesites of Tambora.[18] Olivine is most present in the rocks with less than 53 percent SiO2, while it is absent in the more silica-rich volcanics, characterised by the presence of biotite phenocrysts.[19] The mafic series also contain titanium magnetite and the trachybasalts are dominated by anorthosite-rich plagioclase.[20] Rubidium, strontium and phosphorus pentoxide are especially rich in the lavas from Tambora, more than the comparable ones from Mount Rinjani.[21] The lavas of Tambora are slightly enriched in zircon compared with those of Rinjani.[22]

The magma involved in the 1815 eruption originated in the mantle and was further modified by melts derived from subducted sediments, fluids derived from the subducted crust and crystallization processes in magma chambers.[16] 87Sr86Sr ratios of Mount Tambora are similar to those of Mount Rinjani, but lower than those measured at Sangeang Api.[14] Potassium levels of Tambora volcanics exceed 3 weight percent, placing them in the shoshonite range for alkaline series.[23]

Since the 1815 eruption, the lowermost portion contains deposits of interlayered sequences of lava and pyroclastic materials. Approximately 40% of the layers are represented in the 1-to-4 m-thick (3.3-to-13.1 ft) lava flows.[17] Thick scoria beds were produced by the fragmentation of lava flows. Within the upper section, the lava is interbedded with scoria, tuffs, pyroclastic flows and pyroclastic falls.[17] Tambora has at least 20 parasitic cones[15] and lava domes, including Doro Afi Toi, Kadiendi Nae, Molo and Tahe.[5] The main product of these parasitic vents is basaltic lava flows.[15]

Eruptive history

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Radiocarbon dating has established that Mount Tambora had erupted three times during the current Holocene epoch before the 1815 eruption, but the magnitudes of these eruptions are unknown. Their estimated dates are 3910 BC ± 200 years, 3050 BC and 740 AD ± 150 years.[24] An earlier caldera was filled with lava flows starting from 43,000 years BC; two pyroclastic eruptions occurred later and formed the Black Sands and Brown Tuff formations, the last of which was emplaced between about 3895 BC and 800 AD.[16]

In 1812, Mount Tambora became highly active, with its maximum eruptive intensity occurring in April 1815.[24] The magnitude was 7 on the Volcanic Explosivity Index (VEI) scale, with a total tephra ejecta volume of up to 1.8 × 1011 cubic metres.[24] Its eruptive characteristics included central vent and explosive eruptions, pyroclastic flows, tsunamis and caldera collapse. This eruption had an effect on global climate. Volcanic activity ceased on 15 July 1815.[24] 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.

Around 1880 ± 30 years, eruptions at Mount Tambora have been registered only inside the caldera.[24] It created small lava flows and lava dome extrusions; this was recorded at two on the VEI scale. This eruption created the Doro Api Toi parasitic cone inside the caldera.[25]

Mount Tambora is still active and minor lava domes and flows have been extruded on the caldera floor during the 19th and 20th centuries.[1] The last eruption was recorded in 1967. However, it was a gentle eruption with a VEI of 0, which means it was non-explosive.[24][26] Another very small eruption was reported in 2011.[27] In August 2011, the alert level for the volcano was raised from level I to level II after increased activity was reported in the caldera, including earthquakes and steam emissions.[28][29]

1815 eruption

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Estimated depth of volcanic ashfall during the 1815 eruption—the outermost region (1 cm) reached Borneo and the Sulawesi islands
Main article: 1815 eruption of Mount Tambora

Chronology of the eruption

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Before 1815, Mount Tambora had been dormant for several centuries, as hydrous magma cooled gradually in a closed magma chamber.[7] Inside the chamber, at depths of 1.5 to 4.5 kilometres (0.93 to 2.80 mi), cooling and partial crystallization of the magma exsolved high-pressure magmatic fluid. Overpressure of the chamber of about 4,000 to 5,000 bars (58,000 to 73,000 psi) was generated as temperatures ranged from 700 to 850 °C (1,292 to 1,562 °F).[7] In 1812, the crater began to rumble and generated a dark cloud.[30]

A moderate-sized eruption on 5 April 1815 was followed by thunderous detonation sounds that could be heard in Ternate on the Molucca Islands, 1,400 kilometres (870 mi) from Mount Tambora. On the morning of 6 April 1815, volcanic ash began to fall in East Java, with faint detonation sounds lasting until 10 April.[30] What was first thought to be the sound of firing guns was heard on 10 and 11 April on Sumatra island (more than 2,600 kilometres (1,600 mi) away),[31] and possibly over 3350 km (2060 miles) away in Thailand and Laos.[3]

The eruptions intensified at about 7:00 p.m. on the 10th.[30] Three plumes rose and merged.[31] Pieces of pumice of up to 20 centimetres (7.9 in) in diameter rained down at approximately 8 p.m., followed by ash at around 9–10 p.m. The eruption column collapsed, producing hot pyroclastic flows that cascaded down the mountain and towards the sea on all sides of the peninsula, wiping out the village of Tambora. Loud explosions were heard until the next evening, 11 April. The veil of ash spread as far as West Java and South Sulawesi, while a "nitrous odor" was noticeable in Batavia. The heavy tephra-tinged rain did not recede until 17 April.[30] Analysis of various sites on Mount Tambora using ground-penetrating radar has revealed alternations of pumice and ash deposits covered by the pyroclastic surge and flow sediments that vary in thickness regionally.[32]

The eruption is estimated to have had a Volcanic Explosivity Index of 7.[33] It had 4–10 times the energy of the 1883 Krakatoa eruption.[34] An estimated 100 cubic kilometres (24 cu mi) of pyroclastic trachyandesite was ejected, weighing approximately 1.4×1014 kg.[4] This has left a caldera measuring 6 to 7 kilometres (3.7 to 4.3 mi) across and 600 to 700 metres (2,000 to 2,300 ft) deep.[30] The density of fallen ash in Makassar was 636 kg/m3.[35] Before the explosion, Mount Tambora was approximately 4,300 metres (14,100 ft) high,[30] one of the tallest peaks in the Indonesian archipelago. After the eruption of 1815, the maximum elevation was reduced to 2,851 metres (9,354 ft).[36]

The 1815 Tambora eruption is the largest and most devastating observed eruption in recorded history; a comparison with other major eruptions is listed below.[4][30][37] The explosion was heard 2,600 kilometres (1,600 mi) or 3,350 kilometres (2,080 mi) away, and ash deposits were registered at a distance of at least 1,300 kilometres (810 mi). A pitch of darkness was observed as far away as 600 kilometres (370 mi) from the mountain summit for up to two days.[30] Pyroclastic flows spread to distances of about 20 kilometres (12 mi) from the summit and an estimated 9.3–11.8 × 1013 g of stratospheric sulfate aerosols were generated by the eruption.[38]

Aftermath

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The island's entire vegetation was destroyed as uprooted trees, mixed with pumice ash, washed into the sea and formed rafts of up to 5 kilometres (3.1 mi) across.[30] One pumice raft was found in the Indian Ocean, near Calcutta, on 1 and 3 October 1815.[4] Clouds of thick ash still covered the summit on 23 April. Explosions ceased on 15 July, although smoke emissions were still observed as late as 23 August. Flames and rumbling aftershocks were reported in August 1819, four years after the event.

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[31]

A moderate tsunami struck the shores of various islands in the Indonesian archipelago on 10 April, with waves reaching 4 metres (13 ft) in Sanggar at around 10 p.m. A tsunami causing waves of 1 to 2 metres (3.3 to 6.6 ft) was reported in Besuki, East Java before midnight and another exceeded 2 metres (6.6 ft) in the Molucca Islands.[30] The eruption column reached the stratosphere at an altitude of more than 43 kilometres (141,000 ft).[4] Coarser ash particles fell one to two weeks after the eruptions, while finer particles stayed in the atmosphere for months to years at an altitude of 10 to 30 kilometres (33,000 to 98,000 ft).[30] There are various estimates of the volume of ash emitted: a recent study estimates a dense-rock equivalent volume for the ash of 23 ± 3 cubic kilometres (5.52 ± 0.72 cu mi) and a dense-rock equivalent volume of 18 ± 6 cubic kilometres (4.3 ± 1.4 cu mi) for the pyroclastic flows.[39] Longitudinal winds spread these fine particles around the globe, creating optical phenomena. Between 28 June and 2 July, and between 3 September and 7 October 1815, prolonged and brilliantly coloured sunsets and twilights were frequently seen in London, England. Most commonly, pink or purple colours appeared above the horizon at twilight and orange or red near the horizon.[30]

Fatalities

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The number of fatalities has been estimated by various sources since the nineteenth century. Swiss botanist Heinrich Zollinger traveled to Sumbawa in 1847 and recollected witness accounts about the 1815 eruption of Tambora. In 1855, he published estimates of directly killed people at 10,100, mostly from pyroclastic flows. A further 37,825 were numbered having died from starvation on Sumbawa island.[40] On Lombok, another 10,000 died from disease and hunger.[41] Petroeschevsky (1949) estimated that about 48,000 and 44,000 people were killed on Sumbawa and Lombok, respectively.[42] Several authors have used Petroeschevsky's figures, such as Stothers (1984), who estimated 88,000 deaths in total.[30] However, Tanguy et al. (1998) considered Petroeschevsky's figures based on untraceable sources, so developed an estimate based solely on two primary sources: Zollinger, who spent several months on Sumbawa after the eruption, and the notes of Sir Stamford Raffles,[31] Governor-General of the Dutch East Indies during the event. Tanguy pointed out that there may have been additional victims on Bali and East Java because of famine and disease, and estimated 11,000 deaths from direct volcanic action and 49,000 from post-eruption famine and epidemics.[43] Oppenheimer (2003) estimated at least 71,000 deaths,[4] and numbers as high as 117,000 have been proposed.[37]

Comparison of major volcanic eruptions
Volcano Location Year Column
height (km)		  VEI  N. hemisphere
summer anomaly (°C)		 Fatalities
Taupō Volcano  New Zealand 181 51 7 ? unlikely
Paektu Mountain  Democratic People's Republic of Korea 946 25 7 ? ?
Mount Samalas  Indonesia 1257 38–43[44] 7[45] −1.2[46] ?
1452/1453 mystery eruption Unknown 1452 ? 7 −0.5 ?
Huaynaputina  Peru 1600 46 6 −0.8 ≈1,400
Mount Tambora  Indonesia 1815 44[47] 7 −0.5 >71,000
Krakatoa  Indonesia 1883 80 6 −0.3 36,600
Santa María Volcano  Guatemala 1902 34 6 no anomaly 7,000–13,000
Novarupta  United States 1912 32 6 −0.4 2
Mount St. Helens  United States 1980 24 5 no anomaly 57
El Chichón  Mexico 1982 32 5 ? >2,000
Nevado del Ruiz  Colombia 1985 27 3 no anomaly 23,000
Mount Pinatubo  Philippines 1991 34 6 −0.5 1,202
Hunga Tonga–Hunga Haʻapai  Tonga 2022 58 5–6 ? 6
Sources: Oppenheimer (2003),[4] and Smithsonian Institution's Global Volcanism Program[48]
Global effects
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Sulfate concentration in ice core from Central Greenland, dated by counting oxygen isotope seasonal variations. There is an unknown eruption around the 1810s.[49]
See also: Year Without a Summer

The 1815 eruption released 10 to 120 million tons of sulphur[4] into the stratosphere, causing a global climate anomaly. Different methods have been used to estimate the ejected sulfur mass: the petrological method, an optical depth measurement based on anatomical observations, and the polar ice core sulfate concentration method, which calibrated against cores from Greenland and Antarctica.

In the spring and summer of 1816, a persistent stratospheric sulfate aerosol veil, described then as a "dry fog", was observed in the northeastern United States. It was not dispersed by wind or rainfall, and it reddened and dimmed sunlight to an extent that sunspots were visible to the naked eye.[4] Areas of the northern hemisphere suffered extreme weather conditions and 1816 became known as the "year without a summer". Average global temperatures decreased about 0.4 to 0.7 °C (0.7 to 1.3 °F),[30] enough to cause significant agricultural problems around the globe. After 4 June 1816, when there were frosts in Connecticut, cold weather expanded over most of New England. On 6 June 1816, it snowed in Albany, New York and Dennysville, Maine. Similar conditions persisted for at least three months, ruining most crops across North America while Canada experienced extreme cold. Snow fell until 10 June near Quebec City, accumulating to 30 centimetres (12 in).[4]

That year became the second-coldest year in the northern hemisphere since 1400,[33] while the 1810s were the coldest decade on record, a result of Tambora's eruption and other suspected volcanic events between 1809 and 1810.[50] (See sulfate concentration chart.) Surface-temperature anomalies during the summers of 1816, 1817 and 1818 were −0.51, −0.44 and −0.29 °C, respectively.[33] Along with a cooler summer, parts of Europe experienced a stormier winter,[4] and the Elbe and Ohře Rivers froze over a period of twelve days in February 1816. As a result, prices of wheat, rye, barley and oats rose dramatically by 1817.[51]

This climate anomaly has been cited as a reason for the severity of the 1816–19 typhus epidemic in southeast Europe and the eastern Mediterranean.[4] In addition, large numbers of livestock died in New England during the winter of 1816–1817, while cool temperatures and heavy rains led to 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. Demonstrations at 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]

Culture

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Size comparison of Mount Tambora ("Pompeii of the East") and Mount Vesuvius ("Pompeii")
Main article: Tambora culture

A human settlement obliterated by the Tambora eruption was discovered in 2004. That summer, a team led by Haraldur Sigurðsson with scientists from the University of Rhode Island, the University of North Carolina at Wilmington and the Indonesian Directorate of Volcanology began an archaeological dig in Tambora. Over six weeks, they unearthed evidence of habitation about 25 kilometres (16 mi) west of the caldera, deep in jungle, 5 kilometres (3.1 mi) from shore. The team excavated 3 metres (9.8 ft) of deposits of pumice and ash.[52] The scientists used ground-penetrating radar to locate a small buried house which contained the remains of two adults, bronze bowls, ceramic pots, iron tools and other artifacts.[52] Tests revealed that objects had been carbonized by the heat of the magma. Sigurdsson dubbed the find the "Pompeii of the East",[53][54] and media reports referred to the "Lost Kingdom of Tambora".[55][56] Sigurdsson intended to return to Tambora in 2007 to search for the rest of the villages, and hopefully to find a palace.[52] Many villages in the area had converted to Islam in the 17th century, but the structures uncovered so far do not show Islamic influence.[55]

Based on the artifacts found, such as bronzeware and finely decorated china possibly of Vietnamese or Cambodian origin, the team concluded that the people were well-off traders.[55] The Sumbawa people were known in the East Indies for their horses, honey, sappan wood (for producing red dye), and sandalwood (for incense and medications). The area was thought to be highly productive agriculturally.[52]

The language of the Tambora people was lost with the eruption. Linguists have examined remnant lexical material, such as records by Zollinger and Raffles, and established that Tambora was not an Austronesian language, as would be expected in the area, but possibly a language isolate, or perhaps a member of one of the families of Papuan languages found 500 kilometres (310 mi) or more to the east.[57]

The eruption is captured in latter-day folklore, which explains the cataclysm as divine retribution. A local ruler is said to have incurred the wrath of Allah by feeding dog meat to a hajji and killing him.[11] This is expressed in a poem written around 1830:

Ecosystem

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The floor of the caldera of Mount Tambora, looking north
Tephra layers near the caldera (left) and summit (background) of Mount Tambora

A team led by the Swiss botanist Heinrich Zollinger arrived on Sumbawa in 1847. Zollinger sought to study the area of eruption and its effects on the local ecosystem. He was the first person after the eruption to ascend the summit, which was still covered by smoke. As Zollinger climbed, his feet sank several times through a thin surface crust into a warm layer of powder-like sulfur. Some vegetation had regrown, including trees on the lower slope. A Casuarina forest was noted at 2,200 to 2,550 metres (7,220 to 8,370 ft), while several Imperata cylindrica grasslands were also found.[58] In August 2015 a team of Georesearch Volcanedo Germany followed the way used by Zollinger and explored this way for the first time since 1847. Because of the length of the distance to be travelled on foot, the partly very high temperatures and the lack of water it was a particular challenge for the team of Georesearch Volcanedo.[59]

Resettlement of the area began in 1907, and a coffee plantation was established in the 1930s in the Pekat village on the northwestern slope.[11] A dense rain forest of Duabanga moluccana trees had grown at an altitude of 1,000 to 2,800 metres (3,300 to 9,200 ft).[11] It covers an area up to 80,000 hectares (200,000 acres). The rain forest was discovered by a Dutch team, led by Koster and de Voogd in 1933. From their accounts, they started their journey in a "fairly barren, dry and hot country", and then they entered "a mighty jungle" with "huge, majestic forest giants".[11] At 1,100 metres (3,600 ft), the trees became thinner in shape. Above 1,800 metres (5,900 ft), they found Dodonaea viscosa flowering plants dominated by Casuarina trees. On the summit was sparse Edelweiss and Wahlenbergia.[11]

An 1896 survey records 56 species of birds including the crested white-eye.[60] Several other zoological surveys followed and found other bird species, with over 90 bird species discoveries in this period, including yellow-crested cockatoos, Zoothera thrushes, Hill mynas, green junglefowl and rainbow lorikeets are hunted for the cagebird trade by the local people. Orange-footed scrubfowl are hunted for food. This bird exploitation has resulted in population declines, and the yellow-crested cockatoo is nearing extinction on Sumbawa island.[60]

A commercial logging company began to operate in the area in 1972, posing a threat to the rain forest.[11] The company holds a timber-cutting concession for an area of 20,000 hectares (49,000 acres), or 25% of the total area.[11] Another part of the rain forest is used as a hunting ground. In between the hunting ground and the logging area, there is a designated wildlife reserve where deer, water buffalos, wild pigs, bats, flying foxes and species of reptiles and birds can be found.[11] In 2015, the conservation area protecting the mountain's ecosystem was upgraded to a national park.[61][62]

Exploration of the caldera floor

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Zollinger (1847), van Rheden (1913) and W. A. Petroeschevsky (1947) could only observe the caldera floor from the crater rim. In 2013, a German research team (Georesearch Volcanedo Germany) for the first time carried out a longer expedition into this caldera, about 1300 m deep, and with the help of a native team climbed down the southern caldera wall, reaching the caldera floor while experiencing extreme conditions. The team stayed in the caldera for nine days. People had reached the caldera floor only in a few cases as the descent down the steep wall is difficult and dangerous, subject to earthquakes, landslides and rockfalls. Moreover, only relatively short stays on the caldera floor had been possible because of logistical problems, so that extensive studies had been impossible. The investigation program of Georesearch Volcanedo on the caldera floor included researching the visible effects of smaller eruptions which had taken place since 1815, gas measurements, studies of flora and fauna and measurement of weather data. Especially striking was the relatively high activity of Doro Api Toi ("Gunung Api Kecil" means "small volcano") in the southern part of the caldera and the gases escaping under high pressure on the lower north-east wall. Besides the team discovered near the Doro Api Toi a lavadome which had not yet been mentioned in scientific studies. The team called this new discovery "Adik Api Toi (Indonesian "adik": younger brother). Later this lavadome was called by the Indonesians "Doro Api Bou" ("new volcano"). This lavadome probably appeared in 2011/2012 when there was an increased seismic activity and probably volcanic activity on the caldera floor (there is no exact information about the caldera floor at that time). In 2014 the same research team carried out a further expedition into the caldera and set a new record: over 12 days the investigations of 2013 were continued.[59]

An infrared image of Mount Tambora (north is on the left)

Monitoring

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Indonesia's population has been increasing rapidly since the 1815 eruption. In 2020, the population of the country reached 270 million people, of which 56% concentrated on the island of Java.[63] An event as significant as the 1815 eruption would impact about eight million people.[64]

Seismic activity in Indonesia is monitored by the Directorate of Volcanology and Geological Hazard Mitigation with the monitoring post for Mount Tambora located at Doro Peti village.[65] They focus on seismic and tectonic activity by using a seismograph. There has been no significant increase in seismic activity since the 1880 eruption. Monitoring is continuously performed inside the caldera, with a focus on the parasitic cone Doro Api Toi.[66]

The directorate created a disaster mitigation map for Mount Tambora, which designates two zones for an eruption: a dangerous zone and a cautious zone.[65] The dangerous zone identifies areas that would be directly affected by pyroclastic flows, lava flows or pyroclastic falls. It includes areas such as the caldera and its surroundings, a span of up to 58.7 square kilometres (14,500 acres) where habitation is prohibited. The cautious zone consists of land that might be indirectly affected, either by lahar flows and other pumice stones. The size of the cautious area is 185 square kilometres (46,000 acres), and includes Pasanggrahan, Doro Peti, Rao, Labuan Kenanga, Gubu Ponda, Kawindana Toi and Hoddo villages. A river, called Guwu, at the southern and northwest part of the mountain is also included in the cautious zone.[65]

Panorama

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Panorama of the caldera of Mount Tambora, July 2017

References

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Notes

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  1. ^ a b c d "Tambora". Global Volcanism Program. Smithsonian Institution. Retrieved 24 June 2021.
  2. ^ "Gunung Tambora". Peakbagger. Archived from the original on 19 March 2007. Retrieved 2 August 2018.
  3. ^ a b Goldrick, Richard. "Tambora's Rumblings in The Annals of Lang Xang". {{cite journal}}: Cite journal requires |journal= (help)
  4. ^ a b c d e f g h i j k l m n o 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. ^ a b "Tambora: Synonyms & Subfeatures". Global Volcanism Program. Smithsonian Institution. Retrieved 24 June 2021.
  6. ^ "Mount Tambora". Mount Tambora. Archived from the original on 30 September 2021. Retrieved 4 March 2021.
  7. ^ a b c d e Foden, J. (1986). "The petrology of Tambora volcano, Indonesia: A model for the 1815 eruption". Journal of Volcanology and Geothermal Research. 27 (1–2): 1–41. Bibcode:1986JVGR...27....1F. doi:10.1016/0377-0273(86)90079-X.
  8. ^ a b c Degens, E.T.; Buch, B. (1989). "Sedimentological events in Saleh Bay, off Mount Tambora". Netherlands Journal of Sea Research. 24 (4): 399–404. Bibcode:1989NJSR...24..399D. doi:10.1016/0077-7579(89)90117-8.
  9. ^ Dekov, V.M.; Van Put, A.; Eisma, D.; Van Grieken, R. (March 1999). "Single particle analysis of suspended matter in the Makassar Strait and Flores Sea with particular reference to tin-bearing particles". Journal of Sea Research. 41 (1–2): 45. Bibcode:1999JSR....41...35D. doi:10.1016/S1385-1101(98)00035-5.
  10. ^ "Hobi Mendaki Gunung – Menyambangi Kawah Raksasa Gunung Tambora" (in Indonesian). Sinar Harapan. 2003. Archived from the original on 7 January 2007. Retrieved 2 August 2018.
  11. ^ a b c d e f g h i j de Jong Boers, B. (1995). "Mount Tambora in 1815: A Volcanic Eruption in Indonesia and its Aftermath". Indonesia. 60 (60): 37–59. doi:10.2307/3351140. hdl:1813/54071. JSTOR 3351140. Retrieved 2 August 2018.
  12. ^ a b c Nasution, Aswanir. "Tambora, Nusa Tenggara Barat" (in Indonesian). Directorate of Volcanology and Geological Hazard Mitigation, Indonesia. Archived from the original on 29 September 2007. Retrieved 2 August 2018.
  13. ^ Febriyanto, Erwin (18 October 2015). "Potensi Gunung Tambora" (in Indonesian). Archived from the original on 4 June 2019. Retrieved 2 August 2018.
  14. ^ a b Foden, J.; Varne, R. (1980). "The petrology and tectonic setting of Quaternary—Recent volcanic centres of Lombok and Sumbawa, Sunda arc". Chemical Geology. 30 (3): 201–206. Bibcode:1980ChGeo..30..201F. doi:10.1016/0009-2541(80)90106-0.
  15. ^ a b c Sigurdsson, H.; Carey, S. (1989). "Plinian and co-ignimbrite tephra fall from the 1815 eruption of Tambora volcano". Bulletin of Volcanology. 51 (4): 243–270. Bibcode:1989BVol...51..243S. doi:10.1007/BF01073515. S2CID 132160294.
  16. ^ a b c Gertisser, R.; Self, S.; Thomas, L.E.; Handley, H.K.; Van Calsteren, P.; Wolff, J.A. (1 February 2012). "Processes and Timescales of Magma Genesis and Differentiation Leading to the Great Tambora Eruption in 1815". Journal of Petrology. 53 (2): 271–297. Bibcode:2012JPet...53..271G. doi:10.1093/petrology/egr062.
  17. ^ a b c d "Geology of Tambora Volcano". Vulcanological Survey of Indonesia. Archived from the original on 24 October 2007. Retrieved 2 August 2018.
  18. ^ Foden, 1979, p. 49
  19. ^ Foden, 1979, p. 50
  20. ^ Foden, 1979, p. 51
  21. ^ Foden, 1979, p. 56
  22. ^ Foden, 1979, p.60
  23. ^ Fiorentini, Marco L.; Garwin, Steve L. (2010). "Evidence of a mantle contribution in the genesis of magmatic rocks from the Neogene Batu Hijau district in the Sunda Arc, South Western Sumbawa, Indonesia". Contributions to Mineralogy and Petrology. 159 (6): 826. Bibcode:2010CoMP..159..819F. doi:10.1007/s00410-009-0457-7. S2CID 129804058.
  24. ^ a b c d e f "Tambora: Eruptive History". Global Volcanism Program. Smithsonian Institution. Retrieved 24 June 2021.
  25. ^ "Tambora Historic Eruptions and Recent Activities". Vulcanological Survey of Indonesia. Archived from the original on 27 September 2007. Retrieved 2 August 2018.
  26. ^ "Volcanic Explosivity Index (VEI)". Global Volcanism Program. Smithsonian National Museum of Natural History. Archived from the original on 10 November 2011. Retrieved 2 August 2018.
  27. ^ Wood, Gillen D'Arcy (2014). Tambora: The Eruption That Changed the World. Princeton University Press. pp. 1–312. ISBN 9780691168623.
  28. ^ "Peningkatan Status G. Tambora dari Normal ke Waspada" (in Indonesian). Directorate of Volcanology and Geological Hazard Mitigation, Indonesia. 30 August 2011. Archived from the original on 8 September 2011. Retrieved 2 August 2018.
  29. ^ Wunderman, Richard (2011). "Report on Tambora (Indonesia)". Bulletin of the Global Volcanism Network. 36 (8). doi:10.5479/si.GVP.BGVN201108-264040.
  30. ^ a b c d e f g h i j k l m n Stothers, Richard B. (1984). "The Great Tambora Eruption in 1815 and Its Aftermath". Science. 224 (4654): 1191–1198. Bibcode:1984Sci...224.1191S. doi:10.1126/science.224.4654.1191. PMID 17819476. S2CID 23649251.
  31. ^ a b c d Raffles, S. (1830). Memoir of the life and public services of Sir Thomas Stamford Raffles, F.R.S. &c., particularly in the government of Java 1811–1816, and of Bencoolen and its dependencies 1817–1824: with details of the commerce and resources of the eastern archipelago, and selections from his correspondence (PDF). London: John Murray. Archived (PDF) from the original on 2 August 2018. Retrieved 2 August 2018. Cited by Oppenheimer (2003)
  32. ^ Abrams, Lewis J.; Sigurdsson, Haraldur (2007). "Characterization of pyroclastic fall and flow deposits from the 1815 eruption of Tambora volcano, Indonesia using ground-penetrating radar" (PDF). Journal of Volcanology and Geothermal Research. 161 (4): 352–361. Bibcode:2007JVGR..161..352A. doi:10.1016/j.jvolgeores.2006.11.008. Archived (PDF) from the original on 4 August 2020. Retrieved 2 August 2018.
  33. ^ a b c Briffa, K.R.; Jones, P.D.; Schweingruber, F.H.; Osborn, T.J. (1998). "Influence of volcanic eruptions on Northern Hemisphere summer temperature over the past 600 years". Nature. 393 (6684): 450–455. Bibcode:1998Natur.393..450B. doi:10.1038/30943. S2CID 4392636.
  34. ^ Blast from the Past Archived 15 March 2022 at the Wayback Machine; article; [July, 2002]; By Robert Evans; Smithsonian Magazine, online; accessed September 10, 2020
  35. ^ Stothers, Richard B. (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.
  36. ^ Monk, K.A.; Fretes, Y.; Reksodiharjo-Lilley, G. (1996). The Ecology of Nusa Tenggara and Maluku. Hong Kong: Periplus Editions Ltd. p. 60. ISBN 978-962-593-076-3.
  37. ^ a b Cao, S.; Li, Y.; Yang, B. (2012). "Mt. Tambora, Climatic Changes, and China's Decline in the Nineteenth Century". Journal of World History. 23 (3): 587–607. doi:10.1353/jwh.2012.0066. S2CID 145137831.
  38. ^ Self, S.; Gertisser, R.; Thordarson, T.; Rampino, M.R.; Wolff, J.A. (1 October 2004). "Magma volume, volatile emissions, and stratospheric aerosols from the 1815 eruption of Tambora" (PDF). Geophysical Research Letters. 31 (20): L20608. Bibcode:2004GeoRL..3120608S. doi:10.1029/2004GL020925. hdl:20.500.11820/6925218f-d09e-4f9d-9f2e-3ab8419b223f. S2CID 56290102. Archived (PDF) from the original on 26 April 2019. Retrieved 30 June 2019.
  39. ^ Kandlbauer, J.; Sparks, R.S.J. (October 2014). "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.
  40. ^ Haeseler, Susanne (2016). "Der Ausbruch des Vulkans Tambora in Indonesien im Jahr 1815 und seine weltweiten Folgen, insbesondere das "Jahr ohne Sommer" 1816" (PDF) (in German). Deutscher Wetterdienst. pp. 1–18. Archived (PDF) from the original on 16 February 2020. Retrieved 2 August 2018.
  41. ^ Zollinger (1855): Besteigung des Vulkans Tamboro auf der Insel Sumbawa und Schiderung der Eruption desselben im Jahren 1815, Winterthur: Zurcher and Fürber, Wurster and Co., cited by Oppenheimer (2003).
  42. ^ Petroeschevsky, W.A. (1949). "A contribution to the knowledge of the Gunung Tambora (Sumbawa)". Tijdschrift van het Koninklijk Nederlandsch Aardrijkskundig Genootschap. 2 (66): 688–703., cited by Oppenheimer (2003).
  43. ^ 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.
  44. ^ Vidal, CélineM.; Komorowski, Jean-Christophe; Métrich, Nicole; Pratomo, Indyo; Kartadinata, Nugraha; Prambada, Oktory; Michel, Agnès; Carazzo, Guillaume; Lavigne, Franck; Rodysill, Jessica; Fontijn, Karen (8 August 2015). "Dynamics of the major plinian eruption of Samalas in 1257 A.D. (Lombok, Indonesia)". Bulletin of Volcanology. 77 (9): 73. Bibcode:2015BVol...77...73V. doi:10.1007/s00445-015-0960-9. S2CID 127929333.
  45. ^ Whelley, Patrick L.; Newhall, Christopher G.; Bradley, Kyle E. (22 January 2015). "The frequency of explosive volcanic eruptions in Southeast Asia". Bulletin of Volcanology. 77 (1): 1–11. Bibcode:2015BVol...77....1W. doi:10.1007/s00445-014-0893-8. PMC 4470363. PMID 26097277.
  46. ^ Guillet, Sébastien; Corona, Christophe; Stoffel, Markus; Khodri, Myriam; Lavigne, Franck; Ortega, Pablo; Eckert, Nicolas; Sielenou, Pascal Dkengne; Daux, Valérie; (Sidorova), Olga V. Churakova; Davi, Nicole; Edouard, Jean-Louis; Zhang, Yong; Luckman, Brian H.; Myglan, Vladimir S.; Guiot, Joël; Beniston, Martin; Masson-Delmotte, Valérie; Oppenheimer, Clive (2017). "Climate response to the Samalas volcanic eruption in 1257 revealed by proxy records" (PDF). Nature Geoscience. 10 (2): 123–128. Bibcode:2017NatGe..10..123G. doi:10.1038/ngeo2875. S2CID 133586732. Archived (PDF) from the original on 28 April 2019. Retrieved 30 June 2019.
  47. ^ "Tambora, Sumbawa, Indonesia". volcano.oregonstate.edu. Archived from the original on 17 June 2017. Retrieved 26 February 2019.
  48. ^ "Large Holocene Eruptions". Global Volcanism Program. Smithsonian Institution. Archived from the original on 7 May 2013. Retrieved 7 November 2006.
  49. ^ Dai, J.; Mosley-Thompson, E.; Thompson, L.G. (1991). "Ice core evidence for an explosive tropical volcanic eruption six years preceding Tambora" (PDF). Journal of Geophysical Research: Atmospheres. 96 (D9): 17361–17366. Bibcode:1991JGR....9617361D. doi:10.1029/91JD01634. S2CID 8384563. Archived from the original (PDF) on 2 August 2018. Retrieved 2 August 2018.
  50. ^ Cole-Dai, Jihong; Ferris, David; Lanciki, Alyson; Savarino, Joël; Baroni, Mélanie; Thiemens, Mark H. (1 November 2009). "Cold decade (AD 1810–1819) caused by Tambora (1815) and another (1809) stratospheric volcanic eruption" (PDF). Geophysical Research Letters. 36 (22): L22703. Bibcode:2009GeoRL..3622703C. doi:10.1029/2009GL040882. S2CID 10579910. Archived (PDF) from the original on 6 December 2019. Retrieved 30 June 2019.
  51. ^ Brázdil, Rudolf; Řezníčková, Ladislava; Valášek, Hubert; Dolák, Lukáš; Kotyza, Oldřich (2016). "Climatic effects and impacts of the 1815 eruption of Mount Tambora in the Czech Lands". Climate of the Past. 12 (6): 1361–1374. Bibcode:2016CliPa..12.1361B. doi:10.5194/cp-12-1361-2016.
  52. ^ a b c d "URI volcanologist discovers lost kingdom of Tambora" (Press release). University of Rhode Island. 27 February 2006. Archived from the original on 21 July 2006. Retrieved 2 August 2018.
  53. ^ "'Pompeii of the East' discovered". BBC News. 28 February 2006. Archived from the original on 19 December 2006. Retrieved 2 August 2018.
  54. ^ "Indonesian Volcano Site Reveals 'Pompeii of the East' (Update1)". Bloomberg Asia. 28 February 2006. Archived from the original on 30 September 2007. Retrieved 2 August 2018.
  55. ^ a b c Roach, John (27 February 2006). ""Lost Kingdom" Discovered on Volcanic Island in Indonesia". National Geographic. Archived from the original on 14 November 2006. Retrieved 9 October 2006.
  56. ^ "'Lost kingdom' springs from the ashes". International Herald Tribune. 1 March 2006. Archived from the original on 13 March 2006. Retrieved 2 August 2018.
  57. ^ Donohue, Mark (2007). "The Papuan Language of Tambora" (PDF). Oceanic Linguistics. 46 (2): 520–537. doi:10.1353/ol.2008.0014. JSTOR 20172326. S2CID 26310439. Archived from the original (PDF) on 2 August 2018. Retrieved 2 August 2018.
  58. ^ Zollinger (1855) cited by Trainor (2002).
  59. ^ a b "Volcanedo". Archived from the original on 24 December 2018. Retrieved 30 March 2019.
  60. ^ a b Trainor, C.R. (2002). "Birds of Gunung Tambora, Sumbawa, Indonesia: effects of altitude, the 1815 catalysmic volcanic eruption and trade" (PDF). Forktail. 18: 49–61. Archived from the original (PDF) on 26 February 2012. Retrieved 2 August 2018.
  61. ^ Fardah (15 April 2015). "Mount Tambora National Park Transformed Into New Ecotourism Destination". Antara News. Archived from the original on 30 September 2017. Retrieved 2 August 2018.
  62. ^ Rahmad, Rahmadi (14 May 2015). "Geckos, moths and spider-scorpions: Six new species on Mount Tambora, say Indonesian researchers". Mongabay. Archived from the original on 30 September 2017. Retrieved 2 August 2018.
  63. ^ "Penduduk Migran Seumur Hidup" (in Indonesian). Indonesian Central Statistics Bureau. Archived from the original on 5 November 2010. Retrieved 2 August 2018.
  64. ^ Simpson, Alanna; Johnson, R. Wally; Cummins, Phil (1 May 2011). "Volcanic threat in developing countries of the Asia–Pacific region: probabilistic hazard assessment, population risks, and information gaps". Natural Hazards. 57 (2): 162. Bibcode:2011NatHa..57..151S. doi:10.1007/s11069-010-9601-y. S2CID 129040686.
  65. ^ a b c "Tambora Hazard Mitigation" (in Indonesian). Directorate of Volcanology and Geological Hazard Mitigation. Archived from the original on 29 September 2007. Retrieved 2 August 2018.
  66. ^ "Tambora Geophysics" (in Indonesian). Directorate of Volcanology and Geological Hazard Mitigation, Indonesia. Archived from the original on 29 September 2007. Retrieved 2 August 2018.

Bibliography

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