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1257 Samalas eruption

Coordinates: 8°24′36″S 116°24′30″E / 8.41000°S 116.40833°E / -8.41000; 116.40833
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Map of Lombok Island with Samalas in the upper part of the island
The volcano-caldera complex in the north of Lombok

The Samalas volcano erupted in 1257 CE, in a major eruption which left behind a large caldera that contains Lake Segara Anak.[1] The eruption had a probable Volcanic Explosivity Index of 7,[a] making it one of the largest eruptions of the current Holocene epoch. Samalas volcano lies next to Mount Rinjani on Lombok Island in Indonesia.

Before the site of the eruption was known, an examination of ice cores around the world had found a large spike in sulfate deposition around 1257, which is strong evidence of a large volcanic eruption having occurred somewhere in the world. In 2013, scientists demonstrated that the eruption occurred at Mount Samalas, thanks to historical records from the area.

This eruption had four distinct phases, alternately creating eruption columns reaching tens of kilometres into the atmosphere and pyroclastic flows burying large parts of Lombok Island. The flows destroyed human habitations, including the city of Pamatan, which was the capital of a kingdom on Lombok. Ash from the eruption fell as far away as Java. The volcano deposited more than 10 cubic kilometres (2.4 cu mi) of rocks and ash. The eruption was witnessed by people who recorded it on the Babad Lombok, which is a document written on palm leaves. Later volcanic activity created additional volcanic centres in the caldera, including the Barujari cone that remains active.

The aerosols injected into the atmosphere reduced the solar radiation reaching the Earth's surface, which cooled the atmosphere for several years and led to famines and crop failures in Europe and elsewhere, although the exact scale of the temperature anomalies and their consequences is still debated. It is possible that the eruption helped trigger the Little Ice Age, a centuries-long cold period during the last thousand years.

Geology

General geology

Samalas (also known as Rinjani Tua[4]) was part of what is now the Rinjani volcanic complex, on Lombok, in Indonesia.[5] The remains of Samalas form the Segara Anak caldera, with Mount Rinjani at its eastern edge.[4] Since the destruction of Samalas, two new volcanoes, Rombongan and Barujari, have formed in the caldera. Mount Rinjani has also been volcanically active, forming its own crater, Segara Muncar.[6] Other volcanoes in the region include Agung, Batur, and Bratan, on the island of Bali to the west.[7]

Lombok is one of the Lesser Sunda Islands[8] in the Sunda Arc[9] of Indonesia,[10] a subduction zone where the Australian plate subducts beneath the Eurasian plate[9] at a rate of 7 centimetres per year (2.8 in/year).[11] The magmas feeding Mount Samalas and Mount Rinjani are likely derived from peridotite rocks beneath Lombok, in the mantle wedge.[9] Before the eruption, Mount Samalas may have been as tall as 4,200 ± 100 metres (13,780 ± 330 ft), based on reconstructions that extrapolate upwards from the surviving lower slopes; its current height is less than that of the neighbouring Mount Rinjani, which reaches 3,726 metres (12,224 ft).[12]

The oldest geological units on Lombok Island are from the Oligocene-Miocene,[5][10] with old volcanic units cropping out in southern Lombok.[4][5] Samalas was built up by volcanic activity before 12,000 BP. Rinjani formed between 11,940 ± 40 and 2,550 ± 50 BP,[10] with an eruption between 5,990 ± 50 and 2,550 ± 50 BP forming the Propok Pumice with a dense rock equivalent volume of 0.1 cubic kilometres (0.024 cu mi).[13] The Rinjani Pumice, with a volume of 0.3 cubic kilometres (0.072 cu mi) dense rock equivalent,[14][b] may have been deposited by an eruption from either Rinjani or Samalas;[16] it is dated to 2,550 ± 50 BP,[14] at the end of the time range during which Rinjani formed.[10] The deposits from this eruption reached thicknesses of 6 centimetres (2.4 in) at 28 kilometres (17 mi) distance.[17] Additional eruptions by either Rinjani or Samalas are dated 11,980 ± 40, 11,940 ± 40, and 6,250 ± 40 BP.[13] Eruptive activity continued until about 500 years before 1257.[18] Most volcanic activity now occurs at the Barujari volcano with eruptions in 1884, 1904, 1906, 1909, 1915, 1966, 1994, 2004, and 2009; Rombongan was active in 1944. Volcanic activity mostly consists of explosive eruptions and ash flows.[19]

The rocks of the Samalas volcano are mostly dacitic, with SiO
2 content of 62–63 percent by weight.[10] Volcanic rocks in the Banda arc are mostly calc-alkaline ranging from basalt over andesite to dacite.[19] The crust beneath the volcano is about 20 kilometres (12 mi) thick, and the lower extremity of the Wadati–Benioff zone is about 164 kilometres (102 mi) deep.[9]

Eruption

A small cone rising above a greenish lake within a large crater on a mountain
The Segara Anak caldera, which was created by the eruption

The events of the 1257 eruption have been reconstructed through geological analysis of the deposits it left.[13] The eruption probably occurred within two or three months of September that year, in light of the time it would have taken for its traces to reach the polar ice sheets and be recorded in ice cores.[20] It began with a phreatic (steam explosion powered) stage that deposited 3 centimetres (1.2 in) of ash over 400 square kilometres (150 sq mi) of northwest Lombok Island. A magmatic stage followed, and lithic-rich pumice rained down, with the fallout reaching a thickness of 8 centimetres (3.1 in) both upwind on East Lombok and on Bali.[13] This was followed by lapilli rock as well as ash fallout, and pyroclastic flows that were partially confined within the valleys on Samalas's western flank. Some ash deposits were eroded by the pyroclastic flows, which created furrow structures in the ash. Pyroclastic flows crossed 10 kilometres (6.2 mi) of the Bali Sea, reaching the Gili Islands to the west of Samalas. The deposits show evidence of interaction of the lava with water, so this eruption phase was probably phreatomagmatic. It was followed by three pumice fallout episodes, with deposits over an area wider than was reached by any of the other eruption phases.[21] These pumices fell as far away as Sumbawa in the east, where they are up to 7 centimetres (2.8 in) thick.[22]

The emplacement of these pumices was followed by another stage of pyroclastic flow activity, probably caused by the collapse of the eruption column that generated the flows. At this time the eruption changed from an eruption-column-generating stage to a fountain-like stage and the caldera began to form. These pyroclastic flows were deflected by the topography of the island, filling valleys and flowing around obstacles such as older volcanoes as they flowed across the island incinerating the island's vegetation. Interaction between these flows and air triggered the formation of additional eruption clouds and secondary pyroclastic flows. Where the flows entered the sea north and east of Lombok Island, steam explosions created pumice cones on the beaches and additional secondary pyroclastic flows.[22] Coral reefs were buried by the pyroclastic flows; some flows crossed the Alas Strait between Sumbawa and Lombok and formed deposits on Sumbawa.[23] These pyroclastic flows reached volumes of 29 cubic kilometres (7.0 cu mi) on Lombok,[24] and thicknesses of 35 metres (115 ft) as far as 25 kilometres (16 mi) from Samalas.[25] The various phases of the eruption are also known as P1 (phreatic and magmatic phase), P2 (phreatomagmatic with pyroclastic flows), P3 (Plinian) and P4 (pyroclastic flows).[26] The duration of the P1 and P3 phases is not known individually, but the two phases combined (not including P2) lasted between 12 and 15 hours.[27] The pyroclastic flows altered the geography of eastern Lombok, burying river valleys and extending the shoreline; a new river network developed on the volcanic deposits after the eruption.[28] The eruption column reached a height of 39–40 kilometres (24–25 mi) during the first stage (P1),[29] and of 38–43 kilometres (24–27 mi) during the third stage (P3);[27] it was high enough that SO
2 in it and its Template:Sulfur isotope ratio was influenced by photolysis at high altitudes.[30]

Volcanic rocks ejected by the eruption covered Bali and Lombok and parts of Sumbawa.[11] Tephra in the form of layers of fine ash from the eruption fell as far away as Java, forming part of the Muntilan Tephra, which was found on the slopes of other volcanoes of Java, but could not be linked to eruptions in these volcanic systems. This tephra is now considered to be a product of the 1257 eruption and is thus also known as the Samalas Tephra.[22][31] It reaches thicknesses of 2–3 centimetres (0.79–1.18 in) on Mount Merapi, 15 centimetres (5.9 in) on Mount Bromo, 22 centimetres (8.7 in) at Ijen[32] and 12–17 centimetres (4.7–6.7 in) on Bali's Agung volcano. In Lake Logung on Java it was 3 centimetres (1.2 in) thick. Most of the tephra was deposited west-southwest of Samalas.[33] Considering the thickness of Samalas tephra found at Mount Merapi, the total volume may have reached 32–39 cubic kilometres (7.7–9.4 cu mi).[34] The dispersal index (the surface area covered by an ash or tephra fall) of the eruption reached 7,500 square kilometres (2,900 sq mi) during the first stage and 110,500 square kilometres (42,700 sq mi) during the third stage, implying that these were a Plinian eruption and an Ultraplinian eruption respectively.[35]

Pumice falls with a fine graining and creamy colour from the Samalas eruption have been used as a tephrochronological[c] marker on Bali.[37] Tephra from the volcano was found in ice cores as far as 13,500 kilometres (8,400 mi) away from Samalas,[38] and a tephra layer sampled at Dongdao island in the South China Sea has been tentatively linked to Samalas.[39] Ash and aerosols may have impacted humans and corals at large distances from the eruption.[40]

Estimates of the volumes erupted during the various stages of the Samalas eruption have yielded variable results. The first stage reached a volume of 12.6–13.4 cubic kilometres (3.0–3.2 cu mi). The phreatomagmatic phase has been estimated to have had a volume of 0.9–3.5 cubic kilometres (0.22–0.84 cu mi).[41] The total dense rock equivalent volume of the whole eruption was at least 40 cubic kilometres (9.6 cu mi).[35] The magma erupted was trachydacitic and contained amphibole, apatite, clinopyroxene, iron sulfide, orthopyroxene, plagioclase, and titanomagnetite. It formed out of basaltic magma by fractional crystallization[42] and had a temperature of about 1,000 °C (1,830 °F).[12] Its eruption may have been triggered either by the entry of new magma into the magma chamber or the effects of gas bubble buoyancy.[43]

The eruption had a volcanic explosivity index of 7,[44] making it one of the largest eruptions of the current Holocene epoch.[45] Eruptions of comparable intensity include the Kurile lake eruption (in Kamchatka, Russia) in the 7th millennium BC, the Mount Mazama (United States, Oregon) eruption in the 6th millennium BC, the Minoan eruption (in Santorini, Greece)[45] between 1627 - 1600 BC,[46] and the Tierra Blanca Joven eruption of Lake Ilopango (El Salvador) in the 6th century.[45] Such large volcanic eruptions can result in catastrophic impacts on humans and widespread loss of life both close and far away from the volcano.[47]

The eruption left the 6–7 kilometres (3.7–4.3 mi) wide Segara Anak caldera where the Samalas mountain was before;[6] within its 700–2,800 metres (2,300–9,200 ft) high walls, a 200 metres (660 ft) deep crater lake formed. The Barujari cone rises 320 metres (1,050 ft) above the water of the lake and has erupted 15 times since 1847.[14] A crater lake may have already existed on Samalas before the eruption and supplied its phreatomagmatic phase with 0.1–0.3 cubic kilometres (0.024–0.072 cu mi) of water. Alternatively, the water could have come from aquifers.[48] A collapse structure cuts into Rinjani's slopes facing the Samalas caldera.[12]

The eruption that formed the caldera was first recognized in 2003, and in 2004 a volume of 10 cubic kilometres (2.4 cu mi) was attributed to this eruption.[13] Early research considered that the caldera-forming eruption occurred between 1210 and 1300. In 2013, Lavigne suggested that the eruption occurred in May–October 1257, resulting in the climate changes of 1258.[6] Presently, a number of villages on Lombok are constructed on the pyroclastic flow deposits from the 1257 event.[49]

Research history

The major volcanic event in 1257–1258 was first identified from data in ice cores and from medieval records in the northern hemisphere, which mentioned climate phenomena[50] that are characteristic for volcanic eruptions. Increased sulfate concentrations were first found[51] in 1980 within the Crête ice core[52] (Greenland, drilled in 1974[53]) associated with a deposit of rhyolitic ash;[54] the 1257-1258 layer is the third largest sulfate signal at Crête.[55] These deposits showed that climate disturbances reported at that time were due to a volcanic event, with the global spread indicating a tropical volcano as the cause;[1] at first a source in a volcano near Greenland had been considered[51] but Icelandic records made no mention of eruptions around 1250 and ice cores in Antarctica - at Byrd Station and the South Pole - also contained sulfate signals.[56] Sulfate spikes were also found in ice cores from Ellesmere Island, Canada,[57] and the Samalas sulfate spikes were used as stratigraphic markers for ice cores even before the volcano that caused them was known.[58]

These ice cores indicated a large sulfate spike, accompanied by tephra deposition, around 1259[59] - 1257, the largest[d] in 7,000 years and twice the size of the spike due to the 1815 eruption of Tambora.[61] In 2003, a dense rock equivalent volume of 200–800 cubic kilometres (48–192 cu mi) was estimated for this eruption,[62] but it was also proposed that the eruption might have been somewhat smaller and more enriched in sulfur.[63] The volcano responsible was thought to be located in the Ring of Fire[64] but could not be identified at first;[50] Tofua volcano in Tonga was proposed at first but dismissed, as the Tofua eruption was too small to generate the 1257 sulfate spikes.[65] A volcanic eruption in 1256 at Harrat al-Rahat near Medina was too too small to trigger these events.[66] Other proposals included several simultaneous eruptions.[67] Estimated diameters and positions of the calderas left by the eruption ranged from 10–30 kilometres (6.2–18.6 mi),[68] close to the equator and probably north of it.[69]

The suggestion that Samalas/Rinjani might be the source volcano was first made in 2012, since the other candidate volcanoes – El Chichón and Quilotoa – did not match the chemistry of the sulfur spikes.[70] El Chichon and Quilotoa and Okataina were also inconsistent with the timespan and size of the eruption.[71] The conclusive link between these events and an eruption of Samalas was made in 2013 on the basis of historical records in Indonesia: the Babad Lombok, a series of writings in Old Javanese on palm leaves,[50] written in the 13th century, induced Franck Lavigne,[51] a geoscientist of the Pantheon-Sorbonne University[72] who had already suspected that a volcano on Lombok may be responsible, to conclude that the Samalas volcano was responsible.[51]

All houses were destroyed and swept away, floating on the sea, and many people died

— Babad Lombok, [73]

This event occurred before the end of the 13th century.[12] The role of the Samalas eruption in the global climate events was confirmed by comparing the geochemistry of glass shards found in ice cores to that of the eruption deposits on Lombok.[1] Later, geochemical similarities between tephra found in polar ice cores and eruption products of Samalas reinforced this localization.[74]

Climate effects

Aerosol and paleoclimate data

Ice cores in the northern and southern hemisphere display sulfate spikes associated with Samalas. The signal is the strongest in the southern hemisphere for the last 1000 years;[75] one reconstruction even considers it the strongest of the last 2500 years.[76] In the northern hemisphere it is only exceeded by the signal of the destructive 1783/1784 Laki eruption;[75] The ice core sulfate spikes have been used as a time marker in chronostratigraphic studies.[77] Ice cores from Illimani in Bolivia contain thallium[78] and sulfate spikes from the eruption.[79] For comparison, the 1991 eruption of Pinatubo ejected only about a tenth of the amount of sulfur erupted by Samalas.[80] Sulfate deposition from the Samalas eruption has been noted at Svalbard,[81] and the fallout of sulfuric acid from the volcano may have directly affected peatlands in northern Sweden.[82] The amount of sulfur dioxide released by the eruption has been estimated to be 158 ± 12 million tonnes.[42] The mass release was greater than for the Tambora eruption; Samalas may have been more effective at injecting tephra into the stratosphere, and the Samalas magma may have had higher sulfur content.[83] After the eruption, it probably took weeks to months for the fallout to reach large distances from the volcano.[64] When large scale volcanic eruptions inject aerosols into the atmosphere, they can form stratospheric veils. These reduce the amount of light reaching the surface and cause colder temperatures, which can lead to poor crop yields.[84]

Other records of the eruption's impact include decreased tree growth in Mongolia between 1258–1262 based on tree ring data,[85] frost rings (tree rings damaged by frost during the growth season[86]), light tree rings in Canada and northwestern Siberia from 1258 and 1259 respectively,[87] thin tree rings in the Sierra Nevada, California, U.S.[88] lake sediments recording a cooling episode in northeastern China,[89] a very wet monsoon in Vietnam,[90] droughts in many places of the Northern Hemisphere,[91] and a decade-long thinning of tree rings in Norway and Sweden.[92] Another effect of the eruption-induced climate change may have been a brief decrease of atmospheric carbon dioxide[67] Cooling may have lasted for 4–5 years based on simulations and tree ring data.[93]

The Samalas signal, however, is only inconsistently reported from tree ring climate information,[94][95] and the temperature effects were likewise limited, probably because the large sulfate output altered the average size of particles and thus their radiation forcing.[96] Climate modelling indicated that the Samalas eruption may have reduced global temperatures by approximately 2 °C (3.6 °F), a value largely not replicated by proxy data.[97] Better modelling with a general circulation model that includes a detailed description of the aerosol indicated that the principal temperature anomaly occurred in 1258 and continued until 1261.[97] Climate models tend to overestimate the climate impact of a volcanic eruption;[98] one explanation is that climate models tend to assume that aerosol optical depth increases linearly with the quantity of erupted sulfur.[99] The possible occurrence of an El Niño before the eruption may have further reduced the cooling.[100]

The Samalas eruption, together with another eruption in the 14th century, set off a growth of ice caps and sea ice,[101] and glaciers in Norway advanced.[102] The advances of ice after the Samalas eruption may have strengthened and prolonged the climate effects.[82] Later volcanic activity in 1269, 1278, and 1286 and the effects of sea ice on the North Atlantic would have further contributed to ice expansion.[103] The glacier advances triggered by the Samalas eruption are documented on Baffin Island, where the advancing ice killed and then incorporated vegetation, conserving it.[104] Likewise, a change in Arctic Canada from a warm climate phase to a colder one coincides with the Samalas eruption.[105]

Simulated effects

According to 2003 reconstructions, summer cooling reached 0.69 °C (1.24 °F) in the southern hemisphere and 0.46 °C (0.83 °F) in the northern hemisphere.[106] More recent proxy data indicate that a temperature drop of 0.7 °C (1.3 °F) occurred in 1258 and of 1.2 °C (2.2 °F) in 1259, but with differences between various geographical areas.[107] For comparison, the radiation forcing of Pinatubo's 1991 eruption was about a seventh of that of the Samalas eruption.[108] Sea surface temperatures too decreased by 0.3–2.2 °C (0.54–3.96 °F),[109] triggering changes in the ocean circulations. Ocean temperature and salinity changes may have lasted for a decade.[110] Precipitation and evaporation both decreased, with evaporation reduced more than precipitation.[111]

Volcanic eruptions can also deliver bromine and chlorine into the stratosphere, where they contribute to the breakdown of ozone through their oxides chlorine monoxide and bromine monoxide. While most bromine and chlorine erupted would have been scavenged by the eruption column and thus would not have entered the stratosphere, the quantities that have been modelled for the Samalas halogen release (227 ± 18 million tonnes of chlorine and up to 1.3 ± 0.3 million tonnes of bromine) would have reduced stratospheric ozone.[42]

Climate effects

Samalas, along with the Kuwae eruption in the 1450s and Tambora in 1815, was one of the strongest cooling events in the last millennium, even more so than at the peak of the Little Ice Age.[112] After an early warm winter 1257–1258[e][113] resulting in the early flowering of violets according to reports from France,[114] European summers were colder after the eruption,[115] and winters were long and cold.[116]

The Samalas eruption came after the Medieval Climate Anomaly,[117] a period early in the last millennium with unusually warm temperatures,[118] and at a time where a period of climate stability was ending, with prior eruptions in 1108, 1171, and 1230 already having upset global climate. Subsequent time periods displayed increased volcanic activity until the early 20th century.[119] The time period 1250–1300 was heavily disturbed by volcanic activity,[103] and is recorded by a moraine from a glacial advance on Disko Island,[120] although the moraine may indicate a pre-Samalas cold spell.[121] These volcanic disturbances along with positive feedback effects from increased ice may have started the Little Ice Age even without the need for changes in solar radiation,[122][123] this theory is not without disagreement.[124] The Little Ice Age is a time in the last thousand years during which for several centuries temperatures were depressed;[118] the cooling was associated with volcanic eruptions.[125]

Other inferred effects of the eruption are:

Other regions such as Alaska were mostly unaffected,[134] with little evidence that tree growth was affected in the Western United States,[135] where the eruption may have interrupted a prolonged drought period.[136] The climate effect in Alaska may have been moderated by the nearby ocean.[137] In 1259, on the other hand, western Europe and the west coastal North America had mild weather.[107]

Social and historical consequences

This eruption led to global disaster in 1257–1258.[1] Very large volcanic eruptions can cause destruction close to the volcano[138] and, through their effects on climate, significant human hardship, including famine, away from the volcano although the social effects are often reduced by the resilience of humans.[84] The consequences can affect the whole globe.[2]

Lombok Kingdom and Bali (Indonesia)

Western and central Indonesia at the time were divided into kingdoms in competition with each other, which often built temple complexes with inscriptions documenting historical events,[47] but little direct historical evidence of the consequences of the Samalas eruption exists.[139] The Babad Lombok describe how villages on Lombok were destroyed during the middle 13th century by ash and high-speed sweeps of gas and rocks.[50] They are also - together with other texts - the source of the name "Samalas".[4]

Mount Rinjani avalanched and Mount Salamas collapsed, followed by large flows of debris accompanied by the noise coming from boulders. These flows destroyed Pamatan. All houses were destroyed and swept away, floating on the sea, and many people died. During seven days, big earthquakes shook the Earth, stranded in Leneng, dragged by the boulder flows, People escaped and some of them climbed the hills.

— Babad Lombok, [140]

The city of Pamatan, capital of a kingdom on Lombok, was destroyed, and both disappeared from the historical record. The royal family survived the disaster according to the Javanese text,[141] and there is no clear cut evidence that the kingdom itself was destroyed by the eruption although the history there is poorly known in general.[139] Thousands of people died during the eruption.[12] In Bali the number of inscriptions dropped off after the eruption,[142] and Bali and Lombok may have been depopulated by it,[143] possibly for generations, allowing King Kertanegara of Singhasari on Java to conquer Bali in 1284 with little resistance.[114][142]

Oceania and New Zealand

Historical events in Oceania are usually poorly dated, making it difficult to assess the timing and role of specific events, but there is evidence that between 1250 and 1300 there were crises in Oceania, for example at Easter Island, which may be linked with the beginning of the Little Ice Age and the Samalas eruption.[40] Around 1300, settlements in many places of the Pacific relocated, perhaps because of a sea level drop that occurred after 1250, and the 1991 eruption of Pinatubo has been linked to small drops in sea level.[132]

Climate change triggered by the Samalas eruption and the beginning Little Ice Age may have led to people in Polynesia migrating southwestward in the 13th century. The first settlement of New Zealand most likely occurred 1230–1280 AD and the arrival of people there and on other islands in the region may reflect such a climate-induced migration.[144]

Europe and the Near East

Contemporary chronicles in Europe mention unusual weather conditions in 1258.[145] Reports in 1258 in France and England indicate a dry fog, giving the impression of a persistent cloud cover to contemporary observers.[146] Medieval chronicles say that in 1258, the summer was cold and rainy, causing floods and bad harvests,[71] with cold from February to June.[147] Frost occurred in the summer 1259 according to Russian chronicles.[87] In Europe and the Middle East, changes in atmospheric colours, storms, cold, and severe weather were reported in 1258–1259,[148] with agricultural problems extending to Northern Africa.[149] In Europe, excess rain and cold and high cloudiness damaged crops and caused famines followed by epidemics,[150][90] although 1258–1259 did not lead to famines as bad as some other famines like the Great Famine of 1315–17.[151] In northwest Europe, the effects included crop failure, famine, and weather changes.[101] A famine in London has been linked to this event;[44] while this food crisis was not extraordinary[152] and there were issues with harvests already before the eruption,[153] it is the first well documented food crisis in England.[152] The famine occurred at a time of political crisis between King Henry III of England and the English magnates.[154] Witnesses reported a death toll of 15,000 to 20,000 in London. A mass burial of famine victims was found in the 1990s in the centre of London.[90] Matthew Paris of St. Albans described how until mid-August in 1258, the weather alternated between cold and strong rain, causing high mortality.[155]

Swollen and rotting in groups of five or six, the dead lay abandoned in pigsties, on dunghills, and in the muddy streets.

— Matthew Paris, chronicler of St. Albans, [155]

The resulting famine was severe enough that grain was imported from Germany and Holland.[156] The price for cereal increased in Britain,[148] France, and Italy. Outbreaks of disease occurred during this time in the Middle East and England.[157] With and after the winter of 1258–9, exceptional weathers were reported less commonly, but the winter of 1260–1 was very severe in Iceland, Italy, and elsewhere.[158] The disruption caused by the eruption may have influenced the onset of the Mudéjar revolt of 1264–1266 in Iberia.[159] The Flagellant movement, which is first recorded in Italy in 1260, may have originated in the social distress caused by the effects of the eruption, though warfare and other causes probably played a more important role than natural events.[160]

Long term consequences in Europe and the Near East

Over the long term, the cooling of and sea ice expansion in the North Atlantic may have impacted the societies of Greenland and Iceland[161] by restraining navigation and agriculture, perhaps allowing further climate shocks around 1425 to end the existence of the Norse settlement in Greenland.[162]

Another possible longer term consequence of the eruption was the Byzantine Empire's loss of control over western Anatolia, because of a shift in political power from Byzantine farmers to mostly Turkoman pastoralists in the area. Colder winters caused by the eruption would have impacted agriculture more severely than pastoralism.[163]

Four Corners region, North America

The 1257 Samalas eruption took place during the Pueblo III Period in southwestern North America, during which the Mesa Verde region on the San Juan River was the site of the so-called cliff dwellings. Several sites were abandoned after the eruption, which had cooled the local climate.[164] The Samalas eruption[165] was one among several eruptions during this period which may have triggered climate stresses, which in turn caused strife within the society of the Ancestral Puebloans; possibly they left the northern Colorado Plateau as a consequence.[166]

Altiplano, South America

In the Altiplano of South America, a cold and dry interval between 1200 and 1450 has been associated with the Samalas eruption and the 1280 eruption of Quilotoa volcano in Ecuador. The use of rain-fed agriculture increased in the area between the Salar de Uyuni and the Salar de Coipasa despite the climatic change, implying that the local population effectively coped with the effects of the eruption.[167]

Northeast Asia

Problems were also recorded in China, Japan, and Korea.[90] In Japan, the Azuma Kagami chronicle mentions that rice paddies and gardens were destroyed by the cold and wet weather,[168] and the so-called Shôga famine may have been aggravated by bad weather in 1258 and 1259.[151] Other effects of the eruption include a total darkening of the Moon in May 1258 during a lunar eclipse,[169] a phenomenon also recorded from Europe; volcanic aerosols reduce the amount of sunlight scattered into Earth's shadow and thus the brightness of the eclipsed Moon.[170] The effects of the eruption may also have hastened the decline of the Mongol Empire, although the volcanic event is unlikely to have been the sole cause.[132]

See also

Notes

  1. ^ The Volcanic Explosivity Index is a scale that measures the intensity of an explosive eruption;[2] a magnitude of 7 implies a very large eruption that produces at least 100 cubic kilometres (24 cu mi) of volcanic deposits. Such large eruptions occur once or twice per millennium, although their frequency might be underestimated due to incomplete geological and historical records.[3]
  2. ^ The dense rock equivalent is a measure of how voluminous the magma that the pyroclastic material originated from was.[15]
  3. ^ Tephrochronology is a technique that uses dated layers of tephra to correlate and synchronize events.[36]
  4. ^ Sulfate spikes around 44 BC and 426 BC, discovered later, rival its size.[60]
  5. ^ Winter warming is frequently observed after tropical volcanic eruptions,[113] due to dynamic effects triggered by the sulfate aerosols.[114]

References

  1. ^ a b c d Reid, Anthony (10 July 2016). "Revisiting Southeast Asian History with Geology: Some Demographic Consequences of a Dangerous Environment". In Bankoff, Greg; Christensen, Joseph (eds.). Natural Hazards and Peoples in the Indian Ocean World. Palgrave Macmillan US. p. 33. doi:10.1057/978-1-349-94857-4_2. ISBN 978-1-349-94857-4.
  2. ^ a b Newhall, Self & Robock 2018, p. 572.
  3. ^ Newhall, Self & Robock 2018, p. 573.
  4. ^ a b c d "Rinjani Dari Evolusi Kaldera hingga Geopark". Geomagz (in Indonesian). 4 April 2016. Archived from the original on 2018-02-22. Retrieved 3 March 2018. {{cite web}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  5. ^ a b c Métrich et al. 2018, p. 2258.
  6. ^ a b c Rachmat et al. 2016, p. 109.
  7. ^ Fontijn et al. 2015, p. 2.
  8. ^ Mutaqin et al. 2019, pp. 338–339.
  9. ^ a b c d Rachmat et al. 2016, p. 107.
  10. ^ a b c d e Rachmat et al. 2016, p. 108.
  11. ^ a b Mutaqin et al. 2019, p. 339.
  12. ^ a b c d e Lavigne et al. 2013, p. 16743.
  13. ^ a b c d e Vidal et al. 2015, p. 3.
  14. ^ a b c Vidal et al. 2015, p. 2.
  15. ^ Pyle, David M. (2015-01-01). Sizes of Volcanic Eruptions. pp. 257–264. doi:10.1016/B978-0-12-385938-9.00013-4. ISBN 9780123859389. {{cite book}}: |journal= ignored (help)
  16. ^ Métrich et al. 2018, p. 2260.
  17. ^ Métrich et al. 2018, p. 2264.
  18. ^ Métrich et al. 2018, p. 2263.
  19. ^ a b Rachmat et al. 2016, p. 110.
  20. ^ Crowley, T. J.; Unterman, M. B. (23 May 2013). "Technical details concerning development of a 1200 yr proxy index for global volcanism". Earth System Science Data. 5 (1): 193. Bibcode:2013ESSD....5..187C. doi:10.5194/essd-5-187-2013.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  21. ^ Vidal et al. 2015, p. 5.
  22. ^ a b c Vidal et al. 2015, p. 7.
  23. ^ Mutaqin et al. 2019, p. 344.
  24. ^ Vidal et al. 2015, p. 17.
  25. ^ Lavigne et al. 2013, p. 16744.
  26. ^ Vidal et al. 2015, pp. 21–22.
  27. ^ a b Vidal et al. 2015, p. 18.
  28. ^ Mutaqin et al. 2019, p. 348.
  29. ^ Vidal et al. 2015, pp. 17–18.
  30. ^ Whitehill, A. R.; Jiang, B.; Guo, H.; Ono, S. (20 February 2015). "SO2 photolysis as a source for sulfur mass-independent isotope signatures in stratospehric aerosols". Atmospheric Chemistry and Physics. 15 (4): 1861. Bibcode:2015ACP....15.1843W. doi:10.5194/acp-15-1843-2015.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  31. ^ Alloway et al. 2017, p. 87.
  32. ^ Alloway et al. 2017, p. 90.
  33. ^ Vidal et al. 2015, p. 12.
  34. ^ Vidal et al. 2015, p. 16.
  35. ^ a b Vidal et al. 2015, p. 19.
  36. ^ Lowe, David J. (April 2011). "Tephrochronology and its application: A review". Quaternary Geochronology. 6 (2): 107. doi:10.1016/j.quageo.2010.08.003. hdl:10289/4616. ISSN 1871-1014.
  37. ^ Fontijn et al. 2015, p. 8.
  38. ^ Stevenson, J. A.; Millington, S. C.; Beckett, F. M.; Swindles, G. T.; Thordarson, T. (19 May 2015). "Big grains go far: understanding the discrepancy between tephrochronology and satellite infrared measurements of volcanic ash". Atmospheric Measurement Techniques. 8 (5): 2075. Bibcode:2015AMT.....8.2069S. doi:10.5194/amt-8-2069-2015.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  39. ^ Yang, Zhongkang; Long, Nanye; Wang, Yuhong; Zhou, Xin; Liu, Yi; Sun, Liguang (1 February 2017). "A great volcanic eruption around AD 1300 recorded in lacustrine sediment from Dongdao Island, South China Sea". Journal of Earth System Science. 126 (1): 5. doi:10.1007/s12040-016-0790-y. ISSN 0253-4126.
  40. ^ a b Margalef et al. 2018, p. 5.
  41. ^ Vidal et al. 2015, p. 14.
  42. ^ a b c Vidal, Céline M.; Métrich, Nicole; Komorowski, Jean-Christophe; Pratomo, Indyo; Michel, Agnès; Kartadinata, Nugraha; Robert, Vincent; Lavigne, Franck (10 October 2016). "The 1257 Samalas eruption (Lombok, Indonesia): the single greatest stratospheric gas release of the Common Era". Scientific Reports. 6: 34868. Bibcode:2016NatSR...634868V. doi:10.1038/srep34868. PMC 5056521. PMID 27721477.
  43. ^ Métrich et al. 2018, p. 2278.
  44. ^ a b 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): 3. Bibcode:2015BVol...77....1W. doi:10.1007/s00445-014-0893-8. PMC 4470363. PMID 26097277.
  45. ^ a b c Lavigne et al. 2013, p. 16745.
  46. ^ Lavigne et al. 2013, Table S1.
  47. ^ a b Alloway et al. 2017, p. 86.
  48. ^ Vidal et al. 2015, pp. 14–15.
  49. ^ Lavigne, Franck; Morin, Julie; Mei, Estuning Tyas Wulan; Calder, Eliza S.; Usamah, Muhi; Nugroho, Ute (2017). Mapping Hazard Zones, Rapid Warning Communication and Understanding Communities: Primary Ways to Mitigate Pyroclastic Flow Hazard. Advances in Volcanology. p. 4. doi:10.1007/11157_2016_34. ISBN 978-3-319-44095-8. {{cite book}}: |journal= ignored (help)
  50. ^ a b c d "Culprit Behind Medieval Eruption". Science. 342 (6154): 21.2–21. 3 October 2013. doi:10.1126/science.342.6154.21-b.
  51. ^ a b c d Hamilton 2013, p. 39.
  52. ^ Oppenheimer 2003, p. 417.
  53. ^ Langway, Chester C. (2008). "The history of early polar ice cores" (PDF). Cold Regions Science and Technology. 52 (2): 28. doi:10.1016/j.coldregions.2008.01.001. Archived from the original (PDF) on 2016-11-18. Retrieved 29 January 2019. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  54. ^ Oppenheimer 2003, p. 418.
  55. ^ Hammer, Clausen & Langway 1988, p. 103.
  56. ^ Hammer, Clausen & Langway 1988, p. 104.
  57. ^ Hammer, Clausen & Langway 1988, p. 106.
  58. ^ Osipova, O. P.; Shibaev, Y. A.; Ekaykin, A. A.; Lipenkov, V. Y.; Onischuk, N. A.; Golobokova, L. P.; Khodzher, T. V.; Osipov, E. Y. (7 May 2014). "High-resolution 900 year volcanic and climatic record from the Vostok area, East Antarctica". The Cryosphere. 8 (3): 7. doi:10.5194/tc-8-843-2014. ISSN 1994-0416.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  59. ^ Narcisi et al. 2019, p. 165.
  60. ^ Sigl, M.; Winstrup, M.; McConnell, J. R.; Welten, K. C.; Plunkett, G.; Ludlow, F.; Büntgen, U.; Caffee, M.; Chellman, N.; Dahl-Jensen, D.; Fischer, H.; Kipfstuhl, S.; Kostick, C.; Maselli, O. J.; Mekhaldi, F.; Mulvaney, R.; Muscheler, R.; Pasteris, D. R.; Pilcher, J. R.; Salzer, M.; Schüpbach, S.; Steffensen, J. P.; Vinther, B. M.; Woodruff, T. E. (8 July 2015). "Timing and climate forcing of volcanic eruptions for the past 2,500 years". Nature. 523 (7562): 543–9. Bibcode:2015Natur.523..543S. doi:10.1038/nature14565. PMID 26153860.
  61. ^ Auchmann, Renate; Brönnimann, Stefan; Arfeuille, Florian (March 2015). "Tambora: das Jahr ohne Sommer". Physik in Unserer Zeit (in German). 46 (2): 67. Bibcode:2015PhuZ...46...64A. doi:10.1002/piuz.201401390.
  62. ^ Oppenheimer 2003, p. 419.
  63. ^ Oppenheimer 2003, p. 420.
  64. ^ a b Campbell 2017, p. 113.
  65. ^ Caulfield, J. T.; Cronin, S. J.; Turner, S. P.; Cooper, L. B. (27 April 2011). "Mafic Plinian volcanism and ignimbrite emplacement at Tofua volcano, Tonga". Bulletin of Volcanology. 73 (9): 1274. Bibcode:2011BVol...73.1259C. doi:10.1007/s00445-011-0477-9.
  66. ^ Stothers 2000, p. 361.
  67. ^ a b Brovkin et al. 2010, p. 675.
  68. ^ Oppenheimer 2003, p. 424.
  69. ^ Hammer, Clausen & Langway 1988, p. 107.
  70. ^ Witze, Alexandra (14 July 2012). "Earth: Volcanic bromine destroyed ozone: Blasts emitted gas that erodes protective atmospheric layer". Science News. 182 (1): 12. doi:10.1002/scin.5591820114.
  71. ^ a b Lavigne et al. 2013, p. 16742.
  72. ^ "Centuries-old volcano mystery solved?". Science News. UPI. 18 June 2012. Retrieved 11 March 2019.
  73. ^ Hamilton 2013, pp. 39–40.
  74. ^ Narcisi et al. 2019, p. 168.
  75. ^ a b Kokfelt et al. 2016, p. 2.
  76. ^ Swingedouw et al. 2017, p. 28.
  77. ^ Boudon, Georges; Balcone-Boissard, Hélène; Solaro, Clara; Martel, Caroline (September 2017). "Revised chronostratigraphy of recurrent ignimbritic eruptions in Dominica (Lesser Antilles arc): Implications on the behavior of the magma plumbing system". Journal of Volcanology and Geothermal Research. 343: 135. doi:10.1016/j.jvolgeores.2017.06.022. ISSN 0377-0273.
  78. ^ Kellerhals, Thomas; Tobler, Leonhard; Brütsch, Sabina; Sigl, Michael; Wacker, Lukas; Gäggeler, Heinz W.; Schwikowski, Margit (1 February 2010). "Thallium as a Tracer for Preindustrial Volcanic Eruptions in an Ice Core Record from Illimani, Bolivia". Environmental Science & Technology. 44 (3): 888–93. doi:10.1021/es902492n. ISSN 0013-936X. PMID 20050662.
  79. ^ Knüsel, S. (2003). "Dating of two nearby ice cores from the Illimani, Bolivia". Journal of Geophysical Research. 108 (D6): 4181. Bibcode:2003JGRD..108.4181K. doi:10.1029/2001JD002028.
  80. ^ Fu et al. 2016, p. 2862.
  81. ^ Wendl, I. A.; Eichler, A.; Isaksson, E.; Martma, T.; Schwikowski, M. (7 July 2015). "800-year ice-core record of nitrogen deposition in Svalbard linked to ocean productivity and biogenic emissions". Atmospheric Chemistry and Physics. 15 (13): 7290. Bibcode:2015ACP....15.7287W. doi:10.5194/acp-15-7287-2015.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  82. ^ a b Kokfelt et al. 2016, p. 6.
  83. ^ Vidal et al. 2015, p. 21.
  84. ^ a b Stothers 2000, p. 362.
  85. ^ Davi, N.K.; D'Arrigo, R.; Jacoby, G.C.; Cook, E.R.; Anchukaitis, K.J.; Nachin, B.; Rao, M.P.; Leland, C. (August 2015). "A long-term context (931–2005 C.E.) for rapid warming over Central Asia". Quaternary Science Reviews. 121: 95. Bibcode:2015QSRv..121...89D. doi:10.1016/j.quascirev.2015.05.020.
  86. ^ Baillie, M. G. L.; McAneney, J. (16 January 2015). "Tree ring effects and ice core acidities clarify the volcanic record of the first millennium". Climate of the Past. 11 (1): 105. doi:10.5194/cp-11-105-2015. ISSN 1814-9324. Archived from the original on 2018-10-20. Retrieved 19 October 2018. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)CS1 maint: unflagged free DOI (link)
  87. ^ a b Hantemirov, Rashit M; Gorlanova, Ludmila A; Shiyatov, Stepan G (July 2004). "Extreme temperature events in summer in northwest Siberia since AD 742 inferred from tree rings". Palaeogeography, Palaeoclimatology, Palaeoecology. 209 (1–4): 161. doi:10.1016/j.palaeo.2003.12.023. ISSN 0031-0182.
  88. ^ Scuderi, Louis A. (1990). "Tree-Ring Evidence for Climatically Effective Volcanic Eruptions". Quaternary Research. 34 (1): 73. doi:10.1016/0033-5894(90)90073-T. ISSN 1096-0287. Archived from the original on 2019-01-11. Retrieved 11 January 2019. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  89. ^ Chu, Guoqiang; Sun, Qing; Wang, Xiaohua; Liu, Meimei; Lin, Yuan; Xie, Manman; Shang, Wenyu; Liu, Jiaqi (1 July 2012). "Seasonal temperature variability during the past 1600 years recorded in historical documents and varved lake sediment profiles from northeastern China". The Holocene. 22 (7): 787. doi:10.1177/0959683611430413. ISSN 0959-6836.
  90. ^ a b c d Hamilton 2013, p. 40.
  91. ^ Fei, Jie; Zhou, Jie (February 2016). "The drought and locust plague of 942–944 AD in the Yellow River Basin, China". Quaternary International. 394: 120. doi:10.1016/j.quaint.2014.11.053. ISSN 1040-6182.
  92. ^ Thun, Terje; Svarva, Helene (February 2018). "Tree-ring growth shows that the significant population decline in Norway began decades before the Black Death". Dendrochronologia. 47: 28. doi:10.1016/j.dendro.2017.12.002. ISSN 1125-7865.
  93. ^ Stoffel et al. 2015, p. 787.
  94. ^ Guillet et al. 2017, p. 123.
  95. ^ Baillie, M. G. L.; McAneney, J. (16 January 2015). "Tree ring effects and ice core acidities clarify the volcanic record of the first millennium". Climate of the Past. 11 (1): 106. Bibcode:2015CliPa..11..105B. doi:10.5194/cp-11-105-2015.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  96. ^ Boucher, Olivier (19 May 2015). "Stratospheric Aerosols". Atmospheric Aerosols. Springer Netherlands. p. 279. doi:10.1007/978-94-017-9649-1_12. ISBN 978-94-017-9649-1.
  97. ^ a b Guillet, Sebastien; Corona, Christophe; Stoffel, Markus; Khodri, Myriam; Poulain, Virginie; Guiot, Joel; Luckman, Brian; Churakova, Olga; Beniston, Martin; Franck, Lavigne; Masson-Delmotte, Valerie; Oppenheimer, Clive (2015). "Toward a more realistic assessment of the climatic impacts of the 1257 eruption". EGU General Assembly 2015. 17: 1268. Bibcode:2015EGUGA..17.1268G.
  98. ^ Swingedouw et al. 2017, p. 30.
  99. ^ Stoffel et al. 2015, p. 785.
  100. ^ Timmreck et al. 2009, p. 3.
  101. ^ a b Brewington, Seth D. (May 2016). "The Social Costs of Resilience: An Example from the Faroe Islands". Archeological Papers of the American Anthropological Association. 27 (1): 99. doi:10.1111/apaa.12076.
  102. ^ a b Faust, Johan C.; Fabian, Karl; Milzer, Gesa; Giraudeau, Jacques; Knies, Jochen (February 2016). "Norwegian fjord sediments reveal NAO related winter temperature and precipitation changes of the past 2800 years". Earth and Planetary Science Letters. 435: 91. Bibcode:2016E&PSL.435...84F. doi:10.1016/j.epsl.2015.12.003.
  103. ^ a b Zhong, Y.; Miller, G. H.; Otto-Bliesner, B. L.; Holland, M. M.; Bailey, D. A.; Schneider, D. P.; Geirsdottir, A. (31 December 2010). "Centennial-scale climate change from decadally-paced explosive volcanism: a coupled sea ice-ocean mechanism". Climate Dynamics. 37 (11–12): 2374–2375. Bibcode:2011ClDy...37.2373Z. doi:10.1007/s00382-010-0967-z.
  104. ^ Robock, Alan (27 August 2013). "The Latest on Volcanic Eruptions and Climate". Eos, Transactions American Geophysical Union. 94 (35): 305–306. Bibcode:2013EOSTr..94..305R. doi:10.1002/2013EO350001.
  105. ^ Gennaretti, F.; Arseneault, D.; Nicault, A.; Perreault, L.; Begin, Y. (30 June 2014). "Volcano-induced regime shifts in millennial tree-ring chronologies from northeastern North America". Proceedings of the National Academy of Sciences. 111 (28): 10077–10082. Bibcode:2014PNAS..11110077G. doi:10.1073/pnas.1324220111. PMC 4104845. PMID 24982132.
  106. ^ Oppenheimer 2003, p. 422.
  107. ^ a b Guillet et al. 2017, p. 126.
  108. ^ Lim, Hyung-Gyu; Yeh, Sang-Wook; Kug, Jong-Seong; Park, Young-Gyu; Park, Jae-Hun; Park, Rokjin; Song, Chang-Keun (29 August 2015). "Threshold of the volcanic forcing that leads the El Niño-like warming in the last millennium: results from the ERIK simulation". Climate Dynamics. 46 (11–12): 3727. Bibcode:2016ClDy...46.3725L. doi:10.1007/s00382-015-2799-3.
  109. ^ Chikamoto, Megumi O.; Timmermann, Axel; Yoshimori, Masakazu; Lehner, Flavio; Laurian, Audine; Abe-Ouchi, Ayako; Mouchet, Anne; Joos, Fortunat; Raible, Christoph C.; Cobb, Kim M. (16 February 2016). "Intensification of tropical Pacific biological productivity due to volcanic eruptions" (PDF). Geophysical Research Letters. 43 (3): 1185. Bibcode:2016GeoRL..43.1184C. doi:10.1002/2015GL067359. Archived from the original (PDF) on 2018-07-22. Retrieved 16 December 2018. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  110. ^ Kim, Seong-Joong; Kim, Baek-Min (30 September 2012). "Ocean Response to the Pinatubo and 1259 Volcanic Eruptions". Ocean and Polar Research. 34 (3): 321. doi:10.4217/OPR.2012.34.3.305.
  111. ^ Fu et al. 2016, p. 2859.
  112. ^ Neukom, Raphael; Gergis, Joëlle; Karoly, David J.; Wanner, Heinz; Curran, Mark; Elbert, Julie; González-Rouco, Fidel; Linsley, Braddock K.; Moy, Andrew D.; Mundo, Ignacio; Raible, Christoph C.; Steig, Eric J.; van Ommen, Tas; Vance, Tessa; Villalba, Ricardo; Zinke, Jens; Frank, David (30 March 2014). "Inter-hemispheric temperature variability over the past millennium". Nature Climate Change. 4 (5): 364. Bibcode:2014NatCC...4..362N. doi:10.1038/nclimate2174.
  113. ^ a b Newhall, Self & Robock 2018, p. 575.
  114. ^ a b c Lavigne et al. 2013, p. 16746.
  115. ^ Luterbacher, J; Werner, J P; Smerdon, J E; Fernández-Donado, L; González-Rouco, F J; Barriopedro, D; Ljungqvist, F C; Büntgen, U; Zorita, E; Wagner, S; Esper, J; McCarroll, D; Toreti, A; Frank, D; Jungclaus, J H; Barriendos, M; Bertolin, C; Bothe, O; Brázdil, R; Camuffo, D; Dobrovolný, P; Gagen, M; García-Bustamante, E; Ge, Q; Gómez-Navarro, J J; Guiot, J; Hao, Z; Hegerl, G C; Holmgren, K; Klimenko, V V; Martín-Chivelet, J; Pfister, C; Roberts, N; Schindler, A; Schurer, A; Solomina, O; von Gunten, L; Wahl, E; Wanner, H; Wetter, O; Xoplaki, E; Yuan, N; Zanchettin, D; Zhang, H; Zerefos, C (1 February 2016). "European summer temperatures since Roman times". Environmental Research Letters. 11 (2): 8. doi:10.1088/1748-9326/11/2/024001.
  116. ^ Hernández-Almeida, I.; Grosjean, M.; Przybylak, R.; Tylmann, W. (August 2015). "A chrysophyte-based quantitative reconstruction of winter severity from varved lake sediments in NE Poland during the past millennium and its relationship to natural climate variability". Quaternary Science Reviews. 122: 74–88. Bibcode:2015QSRv..122...74H. doi:10.1016/j.quascirev.2015.05.029.
  117. ^ Andres & Peltier 2016, p. 5783.
  118. ^ a b Andres & Peltier 2016, p. 5779.
  119. ^ Bradley, R. S.; Wanner, H.; Diaz, H. F. (22 January 2016). "The Medieval Quiet Period". The Holocene. 26 (6): 992. doi:10.1177/0959683615622552.
  120. ^ Jomelli et al. 2016, p. 3.
  121. ^ Jomelli et al. 2016, p. 5.
  122. ^ a b Margalef et al. 2018, p. 4.
  123. ^ Miller, Gifford H.; Geirsdóttir, Áslaug; Zhong, Yafang; Larsen, Darren J.; Otto-Bliesner, Bette L.; Holland, Marika M.; Bailey, David A.; Refsnider, Kurt A.; Lehman, Scott J.; Southon, John R.; Anderson, Chance; Björnsson, Helgi; Thordarson, Thorvaldur (January 2012). "Abrupt onset of the Little Ice Age triggered by volcanism and sustained by sea-ice/ocean feedbacks". Geophysical Research Letters. 39 (2): n/a. Bibcode:2012GeoRL..39.2708M. doi:10.1029/2011GL050168.
  124. ^ Naulier, M.; Savard, M. M.; Bégin, C.; Gennaretti, F.; Arseneault, D.; Marion, J.; Nicault, A.; Bégin, Y. (17 September 2015). "A millennial summer temperature reconstruction for northeastern Canada using oxygen isotopes in subfossil trees". Climate of the Past. 11 (9): 1160. Bibcode:2015CliPa..11.1153N. doi:10.5194/cp-11-1153-2015.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  125. ^ Wang, Zhiyuan; Wang, Jianglin; Zhang, Shijia (25 January 2019). "Variations of the global annual mean surface temperature during the past 2000 years: results from the CESM1". Theoretical and Applied Climatology: 8. doi:10.1007/s00704-019-02775-2.
  126. ^ a b Dätwyler et al. 2017, p. 2336.
  127. ^ Dätwyler et al. 2017, pp. 2321–2322.
  128. ^ Emile-Geay et al. 2008, p. 3141.
  129. ^ Emile-Geay et al. 2008, p. 3144.
  130. ^ Yan, Qing; Korty, Robert; Zhang, Zhongshi (September 2015). "Tropical Cyclone Genesis Factors in a Simulation of the Last Two Millennia: Results from the Community Earth System Model". Journal of Climate. 28 (18): 7185. doi:10.1175/jcli-d-15-0054.1. ISSN 0894-8755.
  131. ^ Swingedouw et al. 2017, p. 41.
  132. ^ a b c Newhall, Self & Robock 2018, p. 576.
  133. ^ Knudsen, Karen Luise; Sha, Longbin; Zhao, Meixun; Seidenkrantz, Marit-Solveig; Björck, Svante; Jiang, Hui; Li, Tiegang; Li, Dongling (1 January 2018). "East Asian Winter Monsoon Variations and Their Links to Arctic Sea Ice During the Last Millennium, Inferred From Sea Surface Temperatures in the Okinawa Trough". Paleoceanography and Paleoclimatology. 33 (1): 68. doi:10.1002/2016PA003082. ISSN 2572-4525.
  134. ^ Guillet, Sebastien; Corona, Christophe; Stoffel, Markus; Khodri, Myriam; Poulain, Virginie; Lavigne, Franck; Churakova, Olga; Ortega, Pablo; Daux, Valerie; Luckman, Brian; Guiot, Joel; Oppenheimer, Clive; Masson-Delmotte, Valérie; Edouard, Jean-Louis (2016). "Reassessing the climatic impacts of the AD 1257 Samalas eruption in Europe and in the Northern Hemisphere using historical archives and tree-rings". EGU General Assembly 2016 – SAO/NASA ADS Physics Abstract Service. 18: EPSC2016–15250. Bibcode:2016EGUGA..1815250G.
  135. ^ D'Arrigo, Rosanne; Frank, David; Jacoby, Gordon; Pederson, Neil (2001). "Spatial Response to Major Volcanic Events in or about AD 536, 934 and 1258: Frost Rings and Other Dendrochronological Evidence from Mongolia and Northern Siberia: Comment on R. B. Stothers, 'Volcanic Dry Fogs, Climate Cooling, and Plague Pandemics in Europe and the Middle East' (Climatic Change, 42, 1999)". Climatic Change. 49 (1/2): 243. doi:10.1023/A:1010727122905.
  136. ^ Herweijer, Celine; Seager, Richard; Cook, Edward R.; Emile-Geay, Julien (April 2007). "North American Droughts of the Last Millennium from a Gridded Network of Tree-Ring Data". Journal of Climate. 20 (7): 1355. CiteSeerX 10.1.1.466.4049. doi:10.1175/jcli4042.1. ISSN 0894-8755.
  137. ^ Schneider, David P.; Ammann, Caspar M.; Otto-Bliesner, Bette L.; Kaufman, Darrell S. (1 August 2009). "Climate response to large, high-latitude and low-latitude volcanic eruptions in the Community Climate System Model". Journal of Geophysical Research. 114 (D15): 19. Bibcode:2009JGRD..11415101S. doi:10.1029/2008JD011222.
  138. ^ Newhall, Self & Robock 2018, p. 578.
  139. ^ a b Alloway et al. 2017, p. 98.
  140. ^ Lavigne et al. 2013, Supporting Information.
  141. ^ Hamilton 2013, p. 41.
  142. ^ a b Reid, Anthony (2017-01-16). "Population history in a dangerous environment: How important may natural disasters have been?". Masyarakat Indonesia. 39 (2): 520. ISSN 2502-5694. Archived from the original on 2018-10-19. Retrieved 18 October 2018. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  143. ^ Reid, Anthony (2016). "Building Cities in a Subduction Zone: Some Indonesian Dangers". In Miller, Michelle Ann; Douglass, Mike (eds.). Disaster Governance in Urbanising Asia. Springer Singapore. p. 51. doi:10.1007/978-981-287-649-2_3. ISBN 978-981-287-649-2.
  144. ^ Anderson, Atholl (2016). The First Migration: Māori Origins 3000BC – AD1450. Bridget Williams Books. p. 18. ISBN 9780947492809.
  145. ^ Ludlow, Francis (2017). "Volcanology: Chronicling a medieval eruption". Nature Geoscience. 10 (2): 78–79. doi:10.1038/ngeo2881. ISSN 1752-0908.
  146. ^ Stothers 2000, p. 363.
  147. ^ D'Arrigo, Rosanne; Jacoby, Gordon; Frank, David (2003). "Dendroclimatological evidence for major volcanic events of the past two millennia". Volcanism and the Earth's Atmosphere: Dendroclimatological evidence for major volcanic events of the past two millennia. Geophysical Monograph Series. Vol. 139. p. 259. Bibcode:2003GMS...139..255D. doi:10.1029/139GM16. ISBN 978-0-87590-998-1. {{cite book}}: |journal= ignored (help)
  148. ^ a b Dodds & Liddy 2011, p. 54.
  149. ^ Sánchez, Antonio Vicente Frey (2017). "¿Qué puede aportar el clima a la historia? El ejemplo del periodo cálido medieval en el Magreb almorávide y almohade". El Futuro del Pasado: Revista Electrónica de Historia (in Spanish). 6 (8): 221–266. ISSN 1989-9289. Archived from the original on 2018-10-20. Retrieved 20 October 2018. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  150. ^ Guillet et al. 2017, p. 124.
  151. ^ a b Guillet et al. 2017, p. 127.
  152. ^ a b Campbell 2017, p. 91.
  153. ^ Campbell 2017, p. 108.
  154. ^ Campbell 2017, p. 119.
  155. ^ a b John Gillingham (30 October 2014). Conquests, Catastrophe and Recovery: Britain and Ireland 1066–1485. Random House. p. 26. ISBN 978-1-4735-2233-6.
  156. ^ Speed, Robert; Tickner, David; Lei, Gang; Sayers, Paul; Wei, Yu; Li, Yuanyuan; Moncrieff, Catherine; Pegram, Guy (19 September 2016). Drought risk management: a strategic approach. UNESCO Publishing. p. 44. ISBN 978-92-3-100094-2.
  157. ^ Stothers 2000, p. 366.
  158. ^ Stothers 2000, p. 364.
  159. ^ Sánchez, Antonio Vicente Frey (31 December 2014). "Ciudades y poder político en al-Andalus. Una hipótesis sobre el origen de las revueltas urbanas en Murcia en el siglo XIII". Anuario de Estudios Medievales (in Spanish). 44 (2): 854. doi:10.3989/aem.2014.44.2.06. ISSN 1988-4230. Archived from the original on 2018-12-26. Retrieved 16 December 2018. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  160. ^ Stothers 2000, pp. 367–368.
  161. ^ Harrison & Maher 2014, pp. 156–157.
  162. ^ Harrison & Maher 2014, p. 180.
  163. ^ Xoplaki, Elena; Fleitmann, Dominik; Luterbacher, Juerg; Wagner, Sebastian; Haldon, John F.; Zorita, Eduardo; Telelis, Ioannis; Toreti, Andrea; Izdebski, Adam (March 2016). "The Medieval Climate Anomaly and Byzantium: A review of the evidence on climatic fluctuations, economic performance and societal change". Quaternary Science Reviews. 136: 229–252. Bibcode:2016QSRv..136..229X. doi:10.1016/j.quascirev.2015.10.004.
  164. ^ Matson, R.G. (February 2016). "The nutritional context of the Pueblo III depopulation of the northern San Juan: Too much maize?". Journal of Archaeological Science: Reports. 5: 622–624. doi:10.1016/j.jasrep.2015.08.032. ISSN 2352-409X.
  165. ^ Salzer 2000, p. 308.
  166. ^ Salzer 2000, pp. 312–314.
  167. ^ Cruz, Pablo; Winkel, Thierry; Ledru, Marie-Pierre; Bernard, Cyril; Egan, Nancy; Swingedouw, Didier; Joffre, Richard (1 December 2017). "Rain-fed agriculture thrived despite climate degradation in the pre-Hispanic arid Andes". Science Advances. 3 (12): 5. doi:10.1126/sciadv.1701740. ISSN 2375-2548. PMC 5738230. PMID 29279865. Archived from the original on 2018-10-21. Retrieved 20 October 2018. {{cite journal}}: Unknown parameter |dead-url= ignored (|url-status= suggested) (help)
  168. ^ Guillet et al. 2017, p. 125.
  169. ^ Timmreck et al. 2009, p. 1.
  170. ^ Alloway et al. 2017, p. 96.

Sources

8°24′36″S 116°24′30″E / 8.41000°S 116.40833°E / -8.41000; 116.40833

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