8.2-kiloyear event

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The 8.2 kiloyear event appears as a dent in the warm Holocene period. Evolution of temperatures in the Post-Glacial period following the Last Glacial Maximum (LGM), according to Greenland ice cores. Evolution of temperature in the Post-Glacial period according to Greenland ice cores.jpg
The 8.2 kiloyear event appears as a dent in the warm Holocene period. Evolution of temperatures in the Post-Glacial period following the Last Glacial Maximum (LGM), according to Greenland ice cores.
The warm Holocene period with the 8.2 kiloyear event. Central Greenland ice core reconstructed temperature up to mid-19th century. Greenland Gisp2 Temperature.svg
The warm Holocene period with the 8.2 kiloyear event. Central Greenland ice core reconstructed temperature up to mid-19th century.

In climatology, the 8.2 kiloyear event was a rapid drop in global temperatures that occurred around 8,200 years ago, lasting between two and four centuries. This event marks the beginning of the Northgrippian Age within the Holocene epoch. While this cooling phase was not as intense as the earlier Younger Dryas period that occurred just before the Holocene began, it was still significant. During the 8.2-kiloyear event, atmospheric methane levels dropped by 80 parts per billion, a 15% reduction, suggesting a broad cooling and drying trend across the Northern Hemisphere.

Contents

Identification

A rapid cooling around 8,200 years ago was first identified by Swiss botanist Heinrich Zoller in 1960, who named the event the Misox oscillation for the Val Mesolcina [2] . It is also known as the Finse event in Norway. [3] Evidence for the 8.2 kiloyear event has been found in speleothem records across Eurasia, the Mediterranean, South America, and southern Africa, indicating the event was globally synchronous. [4] The strongest evidence for the event comes from the North Atlantic region; the disruption in climate shows clearly in Greenland ice cores, sedimentary records, and other records of the temperate and tropical North Atlantic. [5] [6] [7] There is less evidence in ice cores from Antarctica and South American records. [8] [9] The effects of the sudden temperature decrease were global, most notably sea level change.

Cooling event

The event may have been caused by a large meltwater pulse, [10] which probably resulted from the final collapse of the Laurentide Ice Sheet of northeastern North America, [11] [12] [13] most likely when the glacial lakes Ojibway and Agassiz suddenly drained into the North Atlantic Ocean. [14] The same type of action produced the Missoula floods which formed the Channeled Scablands of the Columbia River basin. The meltwater pulse may have affected the North Atlantic thermohaline circulation, [15] [16] [17] reducing northward heat transport in the Atlantic and causing significant North Atlantic cooling. [18] The Atlantic meridional overturning circulation (AMOC) weakened by 55% [12] or 62%. [18] Estimates of the cooling vary and depend somewhat on the interpretation of the proxy data, but decreases of around 1 to 5 °C (1.8 to 9.0 °F) have been reported. In Greenland, the event started at 8175 BP, and the cooling was 3.3°C below the decadal average in less than 20 years. The coldest period lasted for about 60 years, and its total duration was about 150 years. [19] [20] The meltwater causation hypothesis is, however, considered to be speculation[ by whom? ] because of inconsistencies with its onset and an unknown region of impact.[ citation needed ]

Researchers suggest that the discharge was probably superimposed upon a longer episode of cooler climate lasting up to 600 years, and it was merely one contributing factor to the event as a whole. [21]

Further afield from the Laurentide Ice Sheet, some tropical records report a 3 °C (5.4 °F) cooling, based on cores drilled into an ancient coral reef in Indonesia. [22] The event also caused a global CO2 decline of about 25 ppm over about 300 years. [23] However, dating and interpretation of other tropical sites are more ambiguous than the North Atlantic sites. In addition, climate modeling shows that the amount of meltwater and the pathway of meltwater are both important in perturbing the North Atlantic thermohaline circulation. [24]

The initial meltwater pulse caused between 0.5 and 4 m (1 ft 8 in and 13 ft 1 in) of sea-level rise. Based on estimates of lake volume and decaying ice cap size, values of 0.4–1.2 m (1 ft 4 in – 3 ft 11 in) circulate. Based on sea-level data from the Mississippi Delta, the end of the Lake Agassiz–Ojibway (LAO) drainage occurred at 8.31 to 8.18 ka and ranges from 0.8 to 2.2 m. [25] The sea-level data from the Rhine–Meuse Delta indicate a 2–4 m (6 ft 7 in – 13 ft 1 in) of near-instantaneous rise at 8.54 to 8.2 ka, in addition to 'normal' post-glacial sea-level rise. [26] Meltwater pulse sea-level rise was experienced fully at a great distance from the release area. Gravity and rebound effects associated with the shifting of water masses meant that the sea-level rise was smaller in areas closer to the Hudson Bay. The Mississippi Delta records around 20%, Northwestern Europe 70%, and Asia 105% of the globally averaged amount. [27] The cooling of the 8.2-kiloyear event was a temporary feature, but the sea-level rise of the meltwater pulse was permanent.

In 2003, the Office of Net Assessment (ONA) at the United States Department of Defense was commissioned to produce a study on the likely and potential effects of modern climate change. [28] The study, conducted under ONA head Andrew Marshall, modeled its prospective climate change on the 8.2 kiloyear event, precisely because it was the middle alternative between the Younger Dryas and the milder Little Ice Age. [29]

Effects

This is the most prominent temperature fallback (regression) of the Holocene immediately preceding the Atlantic temperature peak. Hans J.J.G. Holm , Climate Relapse around 6250 BC.png
This is the most prominent temperature fallback (regression) of the Holocene immediately preceding the Atlantic temperature peak.

Across much of the world, the 8.2 kiloyear event engendered drier environmental conditions. [30] Northern Hemisphere monsoon precipitation declined by 12.4% for every °C of global mean temperature change, while Southern Hemisphere monsoon precipitation rose by 4.2%/°C. [31] The 8.2 kiloyear event was also associated with an increase in ocean salinity and terrestrial dust flux. [32]

North Africa and Mesopotamia

Drier conditions were notable in North Africa; the area around the Charef River in eastern Morocco records an episode of extreme aridity around 8,200 BP. [33] East Africa was significantly affected by five centuries of general drought. In West Asia, especially Mesopotamia, the 8.2-kiloyear event was a 300-year aridification and cooling episode which may have provided the natural force for Mesopotamian irrigation agriculture and surplus production, which were essential for the earliest formation of classes and urban life.[ citation needed ] However, changes taking place over centuries around the period are difficult to link specifically to the approximately 100-year abrupt event, as recorded most clearly in the Greenland ice cores.

In particular, in Tell Sabi Abyad, Syria, significant cultural changes were observed at c. 6200 BC; the settlement was not abandoned at the time. [34]

Madagascar

In northwestern Madagascar, the 8.2 kiloyear event is associated with a negative δ18O excursion and calcite deposition, indicating wet, humid conditions caused by the southward migration of the ITCZ. [35] Summer monsoons in the Southern Hemisphere likely became stronger, contributing to precipitation increases. [36] Humidification was two-phased, with an 8.3 kiloyear sub-event preceding the 8.2 kiloyear sub-event by about 20 years. [37]

Europe

The sediment core records of the Fram Strait show a short-lived cooling during the 8.2 kiloyear event superimposed on a broader interval of warm climate. [38] In western Scotland, the 8.2 kiloyear event coincided with a dramatic reduction in the Mesolithic population. [39] In the Iberian Peninsula, the 8.2 kiloyear event is linked to greater summer aridity that caused an increase in the frequency of fires and a consequent expansion of fire-resistant evergreen oak trees. [40]

North Asia

Lacustrine sediment records show that Western Siberia underwent humidification during the 8.2 kiloyear event. [41]

South Asia

Carbonates from the Riwasa Palaeolake show a weakening of the Indian Summer Monsoon (ISM) synchronous with the 8.2 kiloyear event. [42] Stalagmites from Kotumsar Cave [43] and from Socotra and Oman further confirm the ISM precipitously diminished in strength. [44]

East Asia

A sediment core from Lop Nur in the Tarim Basin shows a major dry spell occurred during the 8.2 kiloyear event. [45] The impact of the 8.2 kiloyear event on forests in the Korean Peninsula was severe, shown by a sizeable reduction in pollen production. It took approximately 400 years for forest ecosystems to recover from the event to their state before the climatic perturbation. [46]

Southeast Asia

Evidence from the Gulf of Thailand reveals that a sea level drop occurred concordantly with the 8.2 kiloyear event. Also detectable from palynological and sedimentological records is an increase in runoff. [47]

North America

In Greenland, the 8.2 kiloyear event is associated with a large negative spike in ice core δ18O values. [48] [49] The waters off Cape Hatteras experienced a major increase in salinity. [50] Bat guano δ13C and δD values in the Grand Canyon declined. [51] Southwestern Mexico became significantly drier, evidenced by the interruption of stalagmite growth. [52] In the Gulf of Mexico, bay-head deltas back stepped as sea levels rose. [53] Mustang Island was breached and ceased to be an effective salinity barrier. [54] Gulf of Mexico δ18Oseawater values dropped by 0.8%. [55]

South America

The South American Summer Monsoon (SASM) drastically intensified during the 8.2 kiloyear event as revealed by sediment records from Juréia Paleolagoon. [56]

See also

Related Research Articles

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The Holocene is the current geological epoch, beginning approximately 11,700 years ago. It follows the Last Glacial Period, which concluded with the Holocene glacial retreat. The Holocene and the preceding Pleistocene together form the Quaternary period. The Holocene is an interglacial period within the ongoing glacial cycles of the Quaternary, and is equivalent to Marine Isotope Stage 1.

<span class="mw-page-title-main">Younger Dryas</span> Time period c. 12,900–11,700 years ago with Northern Hemisphere glacial cooling and SH warming

The Younger Dryas was a period in Earth's geologic history that occurred circa 12,900 to 11,700 years Before Present (BP). It is primarily known for the sudden or "abrupt" cooling in the Northern Hemisphere, when the North Atlantic Ocean cooled and annual air temperatures decreased by ~3 °C (5.4 °F) over North America, 2–6 °C (3.6–10.8 °F) in Europe and up to 10 °C (18 °F) in Greenland, in a few decades. Cooling in Greenland was particularly rapid, taking place over just 3 years or less. At the same time, the Southern Hemisphere experienced warming. This period ended as rapidly as it began, with dramatic warming over ~50 years, which transitioned the Earth from the glacial Pleistocene epoch into the current Holocene.

<span class="mw-page-title-main">Last Interglacial</span> Interglacial period which began 130,000 years ago

The Last Interglacial, also known as the Eemian, was the interglacial period which began about 130,000 years ago at the end of the Penultimate Glacial Period and ended about 115,000 years ago at the beginning of the Last Glacial Period. It corresponds to Marine Isotope Stage 5e. It was the second-to-latest interglacial period of the current Ice Age, the most recent being the Holocene which extends to the present day. During the Last Interglacial, the proportion of CO2 in the atmosphere was about 280 parts per million. The Last Interglacial was one of the warmest periods of the last 800,000 years, with temperatures comparable to and at times warmer than the contemporary Holocene interglacial, with the maximum sea level being up to 6 to 9 metres higher than at present, with global ice volume likely also being smaller than the Holocene interglacial.

<span class="mw-page-title-main">Dansgaard–Oeschger event</span> Rapid climate fluctuation in the last glacial period

A Dansgaard–Oeschger event, is a rapid climate fluctuation; such events occurred 25 times during the last glacial period. Some scientists say that the events occur quasi-periodically with a recurrence time being a multiple of 1,470 years, but this is debated. The comparable climate cyclicity during the Holocene is referred to as Bond events. Dansgaard–Oeschger refers to palaeoclimatologists Willi Dansgaard and Hans Oeschger.

<span class="mw-page-title-main">Last Glacial Maximum</span> Circa 24,000–16,000 BCE; most recent era when ice sheets were at their greatest extent

The Last Glacial Maximum (LGM), also referred to as the Last Glacial Coldest Period, was the most recent time during the Last Glacial Period where ice sheets were at their greatest extent between 26,000 and 20,000 years ago. Ice sheets covered much of Northern North America, Northern Europe, and Asia and profoundly affected Earth's climate by causing a major expansion of deserts, along with a large drop in sea levels.

<span class="mw-page-title-main">Black Sea deluge hypothesis</span> Hypothetical flood scenario

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<span class="mw-page-title-main">Heinrich event</span> Large groups of icebergs traverse the North Atlantic.

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<span class="mw-page-title-main">Abrupt climate change</span> Form of climate change

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<span class="mw-page-title-main">Marine Isotope Stage 11</span> Marine isotope stage between 424,000 and 374,000 years ago

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Siwan Davies FLSW is a Welsh professor of Physical Geography in the department of science at Swansea University.

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<span class="mw-page-title-main">African humid period</span> Holocene climate period during which northern Africa was wetter than today

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The preboreal oscillation (PBO) was a short cooling period within the preboreal stage of the Holocene epoch.

References

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