Last Glacial Maximum

Short description: Circa 24,000–16,000 BCE; most recent era when ice sheets were at their greatest extent

A map of sea surface temperature changes and glacial extent during the last glacial maximum, according to Earth:Climate: Long range Investigation, Mapping, and Prediction, a mapping project conducted by the National Science Foundation in the 1970s and 1980s

The Last Glacial Maximum (LGM), also referred to as the Last Glacial Coldest Period,[1] 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.[2] 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,[3] along with a large drop in sea levels.[4]

Based on changes in position of ice sheet margins dated via terrestrial cosmogenic nuclides and radiocarbon dating, growth of ice sheets in the southern hemisphere commenced 33,000 years ago and maximum coverage has been estimated to have occurred sometime between 26,500 years ago[1] and 20,000 years ago.[5] After this, deglaciation caused an abrupt rise in sea level. Decline of the West Antarctica ice sheet occurred between 14,000 and 15,000 years ago, consistent with evidence for another abrupt rise in the sea level about 14,500 years ago.[6][7] Glacier fluctuations around the Strait of Magellan suggest the peak in glacial surface area was constrained to between 25,200 and 23,100 years ago.[8]

There are no agreed dates for the beginning and end of the LGM, and researchers select dates depending on their criteria and the data set consulted. Jennifer French, an archeologist specialising in the European Palaeolithic, dates its onset at 27,500 years ago, with ice sheets at their maximum by around 26,000 years ago and deglaciation commencing between 20,000 and 19,000 years ago.[9] The LGM is referred to in Britain as the Dimlington Stadial, dated to between 31,000 and 16,000 years ago.[10][11]

## Contents

* 1 Glacial climate
* 2 World impact
* 2.1 Africa and the Middle East
* 2.2 Asia
* 2.3 Australasia
* 2.4 Europe
* 2.5 North America
* 2.6 South America
* 2.7 Atlantic Ocean
* 2.8 Pacific Ocean
* 2.9 Indian Ocean
* 2.10 Southern Ocean
* 3 Late Glacial Period
* 4 See also
* 5 Notes
* 6 Further reading
* 7 External links

## Glacial climate

A map of vegetation patterns during the last glacial maximum

The average global temperature about 21,000 years ago was about 6 °C (11 °F) colder than today.[12][13][14] According to the United States Geological Survey (USGS), permanent summer ice covered about 8% of Earth's surface and 25% of the land area during the last glacial maximum.[15] The USGS also states that sea level was about 125 meters (410 ft) lower than in present times (2012).[15] When comparing to the present, the average global temperature was 15 °C (59 °F) for the 2013–2017 period.[16] As of 2012 about 3.1% of Earth's surface and 10.7% of the land area is covered in year-round ice.[15]

Carbon sequestration in the highly stratified and productive Southern Ocean was essential in producing the LGM.[17] The formation of an ice sheet or ice cap requires both prolonged cold and precipitation (snow). Hence, despite having temperatures similar to those of glaciated areas in North America and Europe, East Asia remained unglaciated except at higher elevations. This difference was because the ice sheets in Europe produced extensive anticyclones above them. These anticyclones generated air masses that were so dry on reaching Siberia and Manchuria that precipitation sufficient for the formation of glaciers could never occur (except in Kamchatka where these westerly winds lifted moisture from the Sea of Japan). The relative warmth of the Pacific Ocean due to the shutting down of the Oyashio Current and the presence of large east–west mountain ranges were secondary factors that prevented the development of continental glaciation in Asia.[18]

All over the world, climates at the Last Glacial Maximum were cooler and almost everywhere drier. In extreme cases, such as Southern Australia and the Sahel, rainfall could have been diminished by up to 90% compared to the present, with flora diminished to almost the same degree as in glaciated areas of Europe and North America. Even in less affected regions, rainforest cover was greatly diminished, especially in West Africa where a few refugia were surrounded by tropical grasslands. The Amazon rainforest was split into two large blocks by extensive savanna, and the tropical rainforests of Southeast Asia probably were similarly affected, with deciduous forests expanding in their place except on the east and west extremities of the Sundaland shelf. Only in Central America and the Chocó region of Colombia did tropical rainforests remain substantially intact – probably due to the extraordinarily heavy rainfall of these regions. Most of the world's deserts expanded. Exceptions were in what is the present-day Western United States, where changes in the jet stream brought heavy rain to areas that are now desert and large pluvial lakes formed, the best known being Lake Bonneville in Utah. Similar conditions occurred in central Iran, where geomorphological evidence from the Masileh Depression indicates that the Hoz-e-Sultan, Mareh, and Salt Lake basins once merged into a single, integrated pluvial lake covering approximately 6,190 square kilometers during the Quaternary period.[19]

In Australia, shifting sand dunes covered half the continent, while the Chaco and Pampas in South America became similarly dry. Present-day subtropical regions also lost most of their forest cover, notably in eastern Australia, the Atlantic Forest of Brazil, and southern China, where open woodland became dominant due to much drier conditions. In northern China – unglaciated despite its cold climate – a mixture of grassland and tundra prevailed, and even here, the northern limit of tree growth was at least 20° farther south than today. In the period before the LGM, many areas that became completely barren desert were wetter than they are today, notably in southern Australia, where Aboriginal occupation is believed to coincide with a wet period between 40,000 and 60,000 years Before Present (BP). In New Zealand and neighbouring regions of the Pacific, temperatures may have been further depressed during part of the LGM by the world's most recent supervolcanic eruption, the Oruanui eruption, approximately 25,500 years BP.[20]

However, it is estimated that during the LGM, low-to-mid latitude land surfaces at low elevation cooled on average by 5.8 °C relative to their present-day temperatures, based on an analysis of noble gases dissolved in groundwater rather than examinations of species abundances that have been used in the past.[21]

## World impact

During the Last Glacial Maximum, much of the world was cold, dry, and inhospitable, with frequent storms and a dust-laden atmosphere. The dustiness of the atmosphere is a prominent feature in ice cores; dust levels were as much as 20 to 25 times greater than they are in the present. This was probably due to a number of factors: reduced vegetation, stronger global winds, and less precipitation to clear dust from the atmosphere.[22] The massive sheets of ice locked away water, lowering the sea level, exposing continental shelves, joining land masses together, and creating extensive coastal plains.[23] The ice sheets also changed the atmospheric circulation, causing the northern Pacific and Atlantic oceans to cool and produce more clouds, which amplified the global cooling as the clouds reflected even more sunlight.[24] During the LGM, 21,000 years ago, the sea level was about 125 meters (about 410 feet) lower than it is today.[25][26] Across most of the globe, the hydrological cycle slowed down, explaining increased aridity in many regions of the world.[27]

### Africa and the Middle East

In Africa and the Middle East, many smaller mountain glaciers formed, and the Sahara and other sandy deserts were greatly expanded in extent.[23] The Atlantic deep sea sediment core V22-196, extracted off the coast of Senegal, shows a major southward expansion of the Sahara.[28]

The Persian Gulf averages about 35 metres in depth and the seabed between Abu Dhabi and Qatar is even shallower, being mostly less than 15 metres deep. For thousands of years the Ur-Shatt (a confluence of the Tigris-Euphrates Rivers) provided fresh water to the Gulf, as it flowed through the Strait of Hormuz into the Gulf of Oman. Bathymetric data suggests there were two palaeo-basins in the Persian Gulf. The central basin may have approached an area of 20,000 km2, comparable at its fullest extent to lakes such as Lake Malawi in Africa. Between 12,000 and 9,000 years ago much of the Gulf's floor was not covered by water, only being flooded by the sea after 8,000 years BP.[29]

It is estimated that annual average temperatures in Southern Africa were 6 °C lower than at present during the Last Glacial Maximum. This temperature drop alone would however not have been enough to generate widespread glaciation or permafrost in the Drakensberg Mountains or the Lesotho Highlands.[30] Seasonal freezing of the ground in the Lesotho Highlands might have reached depths of 2 meters or more below the surface.[31] A few small glaciers did however develop during the LGM, in particular in south-facing slopes.[30] In the Hex River Mountains, in the Western Cape, block streams and terraces found near the summit of Matroosberg evidences past periglacial activity which likely occurred during the LGM.[32] Palaeoclimatological proxies indicate the region around Boomplaas Cave was wetter, with increased winter precipitation.[33] The region of the Zambezi River catchment was colder relative to present and the local drop in mean temperature was seasonally uniform.[34]

On the island of Mauritius in the Mascarenhas Archipelago, open wet forest vegetation dominated, contrasting with the dominantly closed-stratified-tall-forest state of Holocene Mauritian forests.[35]

### Asia

A map showing the probable extent of land and water at the time of the last glacial maximum, 20,000 years ago and when the sea level was likely more than 110 metres lower than it is today

Whereas southern Siberia was covered predominantly by the mammoth steppe biome, northern Siberia contained much more mesic and wet habitats, including mires, woodlands, and tundras.[36]

There were ice sheets in modern Tibet (although scientists continue to debate the extent to which the Tibetan Plateau was covered with ice) as well as in Baltistan and Ladakh. In Southeast Asia, many smaller mountain glaciers formed, and permafrost covered Asia as far south as Beijing. Because of lowered sea levels, many of today's islands were joined to the continents: the Indonesian islands as far east as Borneo and Bali were connected to the Asian continent in a landmass called Sundaland. Palawan was also part of Sundaland, while the rest of the Philippine Islands formed one large island separated from the continent only by the Sibutu Passage and the Mindoro Strait.[37]

The environment along the coast of South China was not very different from that of the present day, featuring moist subtropical evergreen forests, despite sea levels in the South China Sea being about 100 metres lower than the present day.[38]

### Australasia

The Australian mainland, New Guinea, Tasmania and many smaller islands comprised a single land mass. This continent is now sometimes referred to as Sahul. In the Bonaparte Gulf of northwestern Australia, sea levels were about 125 metres lower than present.[39] Interior Australia saw widespread aridity, evidenced by extensive dune activity and falling lake levels.[40] Eastern Australia experienced two nadirs in temperature.[41] Lacustrine sediments from North Stradbroke Island in coastal Queensland indicated humid conditions.[42] Data from Little Llangothlin Lagoon likewise indicate the persistence of rainforests in eastern Australia at this time.[43] Rivers maintained their sinuous form in southeastern Australia and there was increased aeolian deposition of sediment in compared to today.[44] The Flinders Ranges likewise experienced humid conditions,[45] as did Kangaroo Island.[46] In southwestern Western Australia, forests disappeared during the LGM.[47]

Between Sahul and Sundaland – a peninsula of South East Asia that comprised present-day Malaysia and western and northern Indonesia – there remained an archipelago of islands known as Wallacea. The water gaps between these islands, Sahul and Sundaland were considerably narrower and fewer in number than in the present day.[citation needed]

The two main islands of New Zealand, along with associated smaller islands, were joined as one landmass. Virtually all of the Southern Alps were under permanent ice cover, with alpine glaciers extending from them into much of the surrounding high country.[48]

### Europe

Main articles: Earth:Weichselian glaciation, Würm glaciation, and Devensian glaciation

The Last Glacial Maximum refugia, c. 20,000 years ago

Solutrean culture

Epigravettian culture[49]

Reconstructions of the LGM climate in the Western Palearctic, based on rodent associations, suggest that cooling was significantly greater in winter than in summer,[50] consistent with findings from other proxies like pollen.[51] The rodent-based model estimated an average mean annual temperature anomaly of −5.3 °C compared with present-day temperatures, with the mean temperature of the coldest month exhibiting a change of almost −7 °C, while the mean temperature of the warmest month anomaly reached only −3.4 °C. Spatial analysis of these reconstructions indicates a pronounced latitudinal gradient, alongside regional differences, suggesting that temperature anomalies were higher in northwestern Europe but smaller in southwestern and eastern Europe compared to results from some general circulation models.[50]

Northern Europe was largely covered by ice, with the southern boundary of the ice sheets passing through Germany and Poland. This ice extended northward to cover Svalbard and Franz Josef Land and northeastward to occupy the Barents Sea, the Kara Sea, and Novaya Zemlya, ending at the Taymyr Peninsula in what is now northwestern Siberia.[52] Warming commenced in northern latitudes around 20,000 years ago, but it was limited and considerable warming did not take place until around 14,600 year ago.[53]

In northwestern Russia, the Fennoscandian ice sheet reached its LGM extent approximately 17,000 years ago, about five thousand years later than in Denmark, Germany and Western Poland. Outside the Baltic Shield, and in Russia in particular, the LGM ice margin of the Fennoscandian Ice Sheet was highly lobate. The main LGM lobes of Russia followed the Dvina, Vologda and Rybinsk basins respectively. Lobes originated as result of ice following shallow topographic depressions filled with a soft sediment substrate.[54] The northern Ural region was covered in periglacial steppes.[55]

Permafrost covered Europe south of the ice sheet down to as far south as present-day Szeged in Southern Hungary. Ice covered the whole of Iceland.[56] In addition, ice covered Ireland along with roughly the northern half of the British Isles with the southern boundary of the ice sheet running approximately from the south of Wales to the north east of England, and then across the now submerged land of Doggerland to Denmark.[57] Central Europe had isolated pockets of relative warmth corresponding to hydrothermally active areas, which served as refugia for taxa not adapted to extremely cold climates.[58]

In the Cantabrian Mountains of the northwestern corner of the Iberian Peninsula, which in the present day have no permanent glaciers, the LGM led to a local glacial recession as a result of increased aridity caused by the growth of other ice sheets farther to the east and north, which drastically limited annual snowfall over the mountains of northwestern Spain. The Cantabrian alpine glaciers had previously expanded between approximately 60,000 and 40,000 years ago during a local glacial maximum in the region.[59] In northeastern Iberia, the LGM was not the coldest part of MIS 2; the interval immediately after from 18 to 14 ka was.[60]

In northeastern Italy, in the region around Lake Fimon, Artemisia-dominated semideserts, steppes, and meadow-steppes replaced open boreal forests at the start of the LGM, specifically during Heinrich Stadial 3. The overall climate of the region became both drier and colder.[61]

In the Sar Mountains, the glacial equilibrium-line altitude was about 450 metres lower than in the Holocene.[62] In Greece, steppe vegetation predominated.[63]

Megafaunal abundance in Europe peaked around 27,000 and 21,000 BP; this bountifulness was attributable to the cold stadial climate.[64]

During the LGM, Europe experienced a significant reduction in human population, with estimates suggesting a decline of up to 60%.[65]

### North America

Main article: Earth:Wisconsin glaciation

See also: Earth:Cordilleran ice sheet

Northern hemisphere glaciation during the last ice ages during which three to four kilometer-thick ice sheets caused a sea level lowering of about 120 m

In Greenland, the difference between LGM temperatures and present temperatures was twice as great during winter as during summer. Greenhouse gas and insolation forcings dominated temperature changes in northern Greenland, whereas Atlantic meridional overturning circulation (AMOC) variability was the dominant influence on southern Greenland's climate.[66] Illorsuit Island was exclusively covered by cold-based glaciers.[67]

Eastern Beringia was extremely cold and dry.[68] July air temperatures in northern Alaska and Yukon were about 2–3 °C lower compared to today.[69] Equilibrium line altitudes in Alaska suggest summer temperatures were 2–5 °C compared to preindustrial.[70] Sediment core analysis from Lone Spruce Pond in southwestern Alaska show it was a pocket of relative warmth.[71]

Following a preceding period of relative retreat from 52,000 to 40,000 years ago,[72] the Laurentide Ice Sheet grew rapidly at the onset of the LGM until it covered essentially all of Canada east of the Rocky Mountains and extended roughly to the Missouri and Ohio Rivers, and eastward to Manhattan,[73][74][75] reaching a total maximum volume of around 26.5 to 37 million cubic kilometres.[76][77][78] At its peak, the Laurentide Ice Sheet reached 3.2 km in height around Keewatin Dome and about 1.7-2.1 km along the Plains divide.[79] In addition to the large Cordilleran Ice Sheet in Canada and Montana, alpine glaciers advanced and (in some locations) ice caps covered much of the Rocky and Sierra Nevada Mountains further south. Latitudinal gradients were so sharp that permafrost did not reach far south of the ice sheets except at high elevations. Glaciers forced the early human populations who had originally migrated from northeast Siberia into refugia, reshaping their genetic variation by mutation and drift. This phenomenon established the older haplogroups found among Native Americans, and later migrations are responsible for northern North American haplogroups.[80]

In southeastern North America, between the southern Appalachian Mountains and the Atlantic Ocean, there was an enclave of unusually warm climate.[81]

### South America

In the Southern Hemisphere, the Patagonian Ice Sheet covered the whole southern third of Chile and adjacent areas of Argentina. On the western side of the Andes the ice sheet reached sea level as far north as in the 41 degrees south at Chacao Channel. The western coast of Patagonia was largely glaciated, but some authors have pointed out the possible existence of ice-free refugia for some plant species. On the eastern side of the Andes, glacier lobes occupied the depressions of Seno Skyring, Seno Otway, Inútil Bay, and Beagle Channel. On the Straits of Magellan, ice reached as far as Segunda Angostura.[82]

A map of the world during the Last Glacial Maximum

During the LGM, valley glaciers in the southern Andes (38–43° S) merged and descended from the Andes occupying lacustrine and marine basins where they spread out forming large piedmont glacier lobes. Glaciers extended about 7 km west of the modern Llanquihue Lake, but not more than 2 to 3 km south of it. Nahuel Huapi Lake in Argentina was also glaciated by the same time.[83] Over most of the Chiloé Archipelago, glacier advance peaked 26,000 years ago, forming a long north–south moraine system along the eastern coast of Chiloé Island (41.5–43° S). By that time the glaciation at the latitude of Chiloé was of ice sheet type contrasting to the valley glaciation found further north in Chile.[84]

Despite glacier advances much of the area west of Llanquihue Lake was still ice-free during the Last Glacial Maximum. During the coldest period of the Last Glacial Maximum vegetation at this location was dominated by Alpine herbs in wide open surfaces. The global warming that followed caused a slow change in vegetation towards a sparsely distributed vegetation dominated by Nothofagus species.[85] Within this parkland vegetation Magellanic moorland alternated with Nothofagus forest, and as warming progressed even warm-climate trees began to grow in the area. It is estimated that the tree line was depressed about 1,000 m relative to present day elevations during the coldest period, but it rose gradually until 19,300 years ago. At that time a cold reversal caused a replacement of much of the arboreal vegetation with Magellanic moorland and Alpine species.[86] On Isla Grande de Chiloé, Magellanic moorland and closed-canopy Nothofagus forests were both present during the LGM, but the former disappeared by the late LGM.[87]

Little is known about the extent of glaciers during Last Glacial Maximum north of the Chilean Lake District. To the north, in the dry Andes of Central and the Last Glacial Maximum is associated with increased humidity and the verified advance of at least some mountain glaciers.[88] Montane glaciers in the northern Andes reached their peak extent approximately 27,000 years ago.[89] In northwestern Argentina, pollen deposits record the altitudinal descent of the treeline during the LGM.[90]

Amazonia was much drier than in the present.[91] δD values from plant waxes from the LGM are significantly more enriched than those in the present and those dating back to MIS 3, evidencing this increased aridity.[92] Eastern Brazil was also affected; the site of Guanambi in Bahia was much drier than today.[93]

### Atlantic Ocean

AMOC was weaker and more shallow during the LGM.[94] Sea surface temperatures in the western subtropical gyre of the North Atlantic were around 5 °C colder compared to today. Intermediate depth waters of the North Atlantic were better ventilated during the LGM by Glacial North Atlantic Intermediate Water (GNAIW) relative to its present-day ventilation by upper North Atlantic Deep Water (NADW). GNAIW was nutrient poor compared to present day upper NADW. Below GNAIW, southern source bottom water that was very rich in nutrients filled the deep North Atlantic.[95]

Due to the presence of immense ice sheets in Europe and North America, continental weathering flux into the North Atlantic was reduced, as measured by the increased proportion of radiogenic isotopes in neodymium isotope ratios.[96]

There is controversy whether upwelling off the Moroccan coast was stronger during the LGM compared to today. Though coccolith size increases in Calcidiscus leptoporus suggest stronger trade winds during the LGM caused there to be increased coastal upwelling of the northwestern coast of Africa,[97] planktonic foraminiferal δ13C records show upwelling and primary productivity were not enhanced during the LGM except in transient intervals around 23,200 and 22,300 BP.[98]

In the western South Atlantic, where Antarctic Intermediate Water forms, sinking particle flux was heightened as a result of increased dust flux during the LGM and sustained export productivity. The increased sinking particle flux removed neodymium from shallow waters, producing an isotopic ratio change.[99]

### Pacific Ocean

On the Island of Hawaii, geologists have long recognized deposits formed by glaciers on Mauna Kea during recent ice ages. The latest work indicates that deposits of three glacial episodes since 150,000 to 200,000 years ago are preserved on the volcano. Glacial moraines on the volcano formed about 70,000 years ago and from about 40,000 to 13,000 years ago. If glacial deposits were formed on Mauna Loa, they have long since been buried by younger lava flows.[100]

Low sea surface temperature (SST) and sea surface salinity (SSS) in the East China Sea during the LGM suggests the Kuroshio Current was reduced in strength relative to the present.[101] Abyssal Pacific overturning was weaker during the LGM than in the present day, although it was temporarily stronger during some intervals of ice sheet retreat.[102] The El Niño–Southern Oscillation (ENSO) was strong during the LGM.[103] Evidence suggests that the Peruvian Oxygen Minimum Zone in the eastern Pacific was weaker than it is in the present day, likely as a result of increased oxygen concentrations in seawater permitted by cooler ocean water temperatures, though it was similar in spatial extent.[104]

The outflow of North Pacific Intermediate Water through the Tasman Sea was stronger during the LGM.[105]

In the Great Barrier Reef along the coast of Queensland, reef development shifted seaward due to the precipitous drop in sea levels, reaching a maximum distance from the present coastline as sea levels approached their lowest levels around 20,700–20,500 years ago.[106] Microbial carbonate deposition in the Great Barrier Reef was enhanced due to low atmospheric CO2 levels.[107]

### Indian Ocean

The deep waters of the Indian Ocean were significantly less oxygenated during the LGM compared to the Middle Holocene.[108] The deep South Indian Ocean in particular was an enormous carbon sink, partially explaining the very low pCO2 of the LGM.[109] The intermediate waters of the southeastern Arabian Sea were poorly ventilated relative to today because of the weakened thermohaline circulation.[110]

### Southern Ocean

Evidence from sediment cores in the Scotia Sea suggests the Antarctic Circumpolar Current was weaker during the LGM than during the Holocene.[111] The Antarctic Polar Front (APF) was located much farther to the north compared to its present-day location. Studies suggest it could have been placed as far north as 43°S, reaching into the southern Indian Ocean.[112]

## Late Glacial Period

The Late Glacial Period followed the LGM and preceded the Holocene, which started around 11,700 years ago.[113]

## See also

* Earth:Climate: Long range Investigation, Mapping, and Prediction - Research project
* Earth:Penultimate Glacial Period - Glacial age that occurred before the Last Glacial Period
* Earth:Mousterian Pluvial - Obsolete term for a prehistoric wet and rainy period in North Africa
* Earth:Holocene glacial retreat - Global deglaciation starting about 19,000 years ago and accelerating about 15,000 years ago
* Earth:Oldest Dryas - Abrupt climatic cooling event during the last glacial retreat
* Earth:Older Dryas - Geological period of the Earth
* Earth:Bølling–Allerød warming - 2000 year warm period about 14,000 years ago
* Bølling oscillation
* Allerød oscillation
* Earth:Younger Dryas - Time period c. 12,900–11,700 years ago
* Earth:African humid period - Holocene climate period during which northern Africa was wetter than today
* History:8.2-kiloyear event - Rapid global cooling about 8,200 years ago
* Earth:5.9 kiloyear event
* Earth:Older Peron
* Earth:Piora Oscillation - Abrupt cold and wet period in the Holocene Epoch
* Earth:Little Ice Age - Climatic cooling after the Medieval Warm Period (16th–19th centuries)
* Earth:Sea level rise - Rise in sea levels due to climate change
* Unsolved:Black Sea deluge hypothesis - Hypothetical flood scenario
* Earth:Timeline of glaciation - Chronology of the major ice ages of the Earth

## Notes

1. ↑ 1.0 1.1 Barrell, David J. A.; Almond, Peter C.; Vandergoes, Marcus J.; Lowe, David J.; Newnham, Rewi M. (15 August 2013). "A composite pollen-based stratotype for inter-regional evaluation of climatic events in New Zealand over the past 30,000 years (NZ-Intimate project)". Quaternary Science Reviews 74: 4–20. doi:10.1016/j.quascirev.2013.04.002. Bibcode: 2013QSRv...74....4B. https://www.sciencedirect.com/science/article/abs/pii/S0277379113001339. Retrieved 9 May 2023.
2. ↑ Armstrong, Edward; Hopcroft, Peter O.; Valdes, Paul J. (7 November 2019). "A simulated Northern Hemisphere terrestrial climate dataset for the past 60,000 years". Scientific Data 6 (1): 265. doi:10.1038/s41597-019-0277-1. PMID 31700065. Bibcode: 2019NatSD...6..265A.
3. ↑ Beyer, Robert M.; Krapp, Mario; Manica, Andrea (14 July 2020). "High-resolution terrestrial climate, bioclimate and vegetation for the last 120,000 years". Scientific Data 7 (1): 236. doi:10.1038/s41597-020-0552-1. PMID 32665576. Bibcode: 2020NatSD...7..236B.
4. ↑ Mithen, Steven (2004). After the Ice: a global human history, 20.000–5.000 BC. Cambridge MA: Harvard University Press. p. 3. ISBN 978-0-674-01570-8.
5. ↑ Anonymous (22 February 1994). "Reconstructing the last glacial and deglacial ice sheets". Eos, Transactions American Geophysical Union 75 (8): 82–84. doi:10.1029/94EO00492. Bibcode: 1994EOSTr..75...82.. https://agupubs.onlinelibrary.wiley.com/doi/abs/10.1029/94EO00492. Retrieved 10 May 2023.
6. ↑ Clark, Peter U.; Dyke, Arthur S.; Shakun, Jeremy D.; Carlson, Anders E.; Clark, Jorie; Wohlfarth, Barbara; Mitrovica, Jerry X.; Hostetler, Steven W. et al. (2009). "The Last Glacial Maximum". Science 325 (5941): 710–4. doi:10.1126/science.1172873. PMID 19661421. Bibcode: 2009Sci...325..710C.
7. ↑ Evans, Amanda M.; Flatman, Joseph C.; Flemming, Nicholas C. (5 May 2014). Prehistoric Archaeology on the Continental Shelf: A Global Review. Springer. ISBN 978-1-46149635-9. https://books.google.com/books?id=s4YpBAAAQBAJ&pg=PA75.
8. ↑ Fernández, Marilén; Ponce, Juan Federico; Mercau, Josefina Ramón; Coronato, Andrea; Laprida, Cecilia; Maidana, Nora; Quiroga, Diego; Magneres, Ignacio (15 July 2020). "Paleolimnological response to climate variability during Late Glacial and Holocene times: A record from Lake Arturo, located in the Fuegian steppe, southern Argentina". Palaeogeography, Palaeoclimatology, Palaeoecology 550. doi:10.1016/j.palaeo.2020.109737. Bibcode: 2020PPP...55009737F. https://www.sciencedirect.com/science/article/abs/pii/S0031018220301826#!. Retrieved 5 November 2022.
9. ↑ French, Jennifer (2021). Palaeolithic Europe: A Demographic and Social Prehistory. Cambridge, UK: Cambridge University Press. p. 226. ISBN 978-1-108-49206-5.
10. ↑ Ashton, Nick (2017). Early Humans. William Collins. p. 241. ISBN 978-0-00-815035-8.
11. ↑ Pettitt, Paul; White, Mark (2012). The British Palaeolithic: hominin societies at the edge of the Pleistocene world. London: Routledge. pp. 424–426. ISBN 978-0-415-67454-6.
12. ↑ "How cold was the ice age? Researchers now know" (in en). phys.org. https://phys.org/news/2020-08-cold-ice-age.html.
13. ↑ Tierney, Jessica E.; Zhu, Jiang; King, Jonathan; Malevich, Steven B.; Hakim, Gregory J.; Poulsen, Christopher J. (August 2020). "Glacial cooling and climate sensitivity revisited" (in en). Nature 584 (7822): 569–573. doi:10.1038/s41586-020-2617-x. ISSN 1476-4687. PMID 32848226. Bibcode: 2020Natur.584..569T. https://www.nature.com/articles/s41586-020-2617-x. Retrieved 7 September 2020.
14. ↑ Seltzer, Alan M.; Ng, Jessica; Aeschbach, Werner; Kipfer, Rolf; Kulongoski, Justin T.; Severinghaus, Jeffrey P.; Stute, Martin (12 May 2021). "Widespread six degrees Celsius cooling on land during the Last Glacial Maximum" (in en). Nature 593 (7858): 228–232. doi:10.1038/s41586-021-03467-6. ISSN 1476-4687. PMID 33981051. Bibcode: 2021Natur.593..228S. https://www.nature.com/articles/s41586-021-03467-6.
15. ↑ 15.0 15.1 15.2 Richard Z. Poore, Richard S. Williams, Jr., and Christopher Tracey. "Sea Level and Climate". United States Geological Survey.
16. ↑ "Land and Ocean Summary". Berkeley Earth.
17. ↑ Sikes, Elisabeth L.; Umling, Natalie E.; Allen, Katherine A.; Ninnemann, Ulysses S.; Robinson, Rebecca S.; Russell, Joellen L.; Williams, Thomas J. (9 June 2023). "Southern Ocean glacial conditions and their influence on deglacial events" (in en). Nature Reviews Earth & Environment 4 (7): 454–470. doi:10.1038/s43017-023-00436-7. ISSN 2662-138X. Bibcode: 2023NRvEE...4..454S. https://www.nature.com/articles/s43017-023-00436-7. Retrieved 21 September 2023.
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86. ↑ Moreno, Patricio I.; Denton, George H.; Moreno, Hugo; Lowell, Thomas V.; Putnam, Aaron E.; Kaplan, Michael R. (2015). "Radiocarbon chronology of the last glacial maximum and its termination in northwestern Patagonia". Quaternary Science Reviews 122: 233–249. doi:10.1016/j.quascirev.2015.05.027. Bibcode: 2015QSRv..122..233M. http://repositorio.uchile.cl/bitstream/2250/134818/1/Radiocarbon-chronology-of-the-last-glacial-maximum.pdf.
87. ↑ Briones, Dalila; Guerra, Lucía; Soteres, Rodrigo L.; Moreno, Patricio I. (15 November 2024). "Vegetation and environmental responses from extreme glacial to extreme interglacial conditions in central Isla Grande de Chiloé (∼42°S), northwestern Patagonia" (in en). Quaternary Science Reviews 344. doi:10.1016/j.quascirev.2024.108927. Bibcode: 2024QSRv..34408927B. https://www.sciencedirect.com/science/article/pii/S0277379124004281. Retrieved 18 October 2024.
88. ↑ Harrison, Stephan (2004). "The Pleistocene glaciations of Chile". in Ehlers, J.. Quaternary Glaciations – Extent and Chronology: Part III: South America, Asia, Africa, Australasia, Antarctica. pp. 91–97.
89. ↑ Clapperton, Chalmers M. (1 April 1993). "Nature of environmental changes in South America at the Last Glacial Maximum". Palaeogeography, Palaeoclimatology, Palaeoecology. Quaternary Palaeoclimates of the Southern Hemisphere 101 (3): 189–208. doi:10.1016/0031-0182(93)90012-8. ISSN 0031-0182. Bibcode: 1993PPP...101..189C. https://www.sciencedirect.com/science/article/abs/pii/0031018293900128. Retrieved 9 September 2024.
90. ↑ Torres, Gonzalo R.; Pérez, Claudio F.; Lupo, Liliana C. (15 April 2019). "Altitudinal patterns of wind transport and deposition of Yungas tree pollen in northwestern Argentina: Implications for interpreting the Quaternary fossil record". Palaeogeography, Palaeoclimatology, Palaeoecology 520: 66–77. doi:10.1016/j.palaeo.2019.01.013. Bibcode: 2019PPP...520...66T. https://www.sciencedirect.com/science/article/abs/pii/S003101821830720X. Retrieved 10 January 2023.
91. ↑ Reis, Luiza Santos; Guimarães, José Tasso Felix; Souza-Filho, Pedro Walfir Martins; Sahoo, Prafulla Kumar; de Figueiredo, Mariana Maha Jana Costa; de Souza, Everaldo Barreiros; Giannini, Tereza Cristina (25 August 2017). "Environmental and vegetation changes in southeastern Amazonia during the late Pleistocene and Holocene". Quaternary International 449: 83–105. doi:10.1016/j.quaint.2017.04.031. ISSN 1040-6182. Bibcode: 2017QuInt.449...83R. https://www.sciencedirect.com/science/article/pii/S1040618216312678. Retrieved 19 December 2023.
92. ↑ Häggi, Christoph; Chiessi, Cristiano M.; Merkel, Ute; Mulitza, Stefan; Prange, Matthias; Schulz, Michael; Schefuß, Enno (1 December 2017). "Response of the Amazon rainforest to late Pleistocene climate variability". Earth and Planetary Science Letters 479: 50–59. doi:10.1016/j.epsl.2017.09.013. ISSN 0012-821X. Bibcode: 2017E&PSL.479...50H. https://www.sciencedirect.com/science/article/pii/S0012821X17305095. Retrieved 19 December 2023.
93. ↑ Scherer, Carolina Saldanha; Pales, Letícia Francielle Moreira; Rosa, Mariane; Silva, Samara de Almeida da (1 November 2017). "Chronological, taphonomical, and paleoenvironmental aspects of a Late Pleistocene mammalian fauna from Guanambi, Bahia, Brazil". Journal of South American Earth Sciences 79: 95–110. doi:10.1016/j.jsames.2017.07.016. ISSN 0895-9811. Bibcode: 2017JSAES..79...95S. https://www.sciencedirect.com/science/article/pii/S0895981117302043. Retrieved 5 January 2024.
94. ↑ Pöppelmeier, Frerk; Jeltsch-Thömmes, Aurich; Lippold, Jörg; Joos, Fortunat; Stocker, Thomas F. (3 April 2023). "Multi-proxy constraints on Atlantic circulation dynamics since the last ice age". Nature Geoscience 16 (4): 349–356. doi:10.1038/s41561-023-01140-3. PMID 37064010. Bibcode: 2023NatGe..16..349P.
95. ↑ Keigwin, Lloyd D. (3 November 2004). "Radiocarbon and stable isotope constraints on Last Glacial Maximum and Younger Dryas ventilation in the western North Atlantic". Paleoceanography and Paleoclimatology 19 (4): 1–15. doi:10.1029/2004PA001029. Bibcode: 2004PalOc..19.4012K.
96. ↑ Pöppelmeier, Frerk; Lippold, Jörg; Blaser, Patrick; Gutjahr, Marcus; Frank, Martin; Stocker, Thomas F. (1 March 2022). "Neodymium isotopes as a paleo-water mass tracer: A model-data reassessment". Quaternary Science Reviews 279. doi:10.1016/j.quascirev.2022.107404. Bibcode: 2022QSRv..27907404P.
97. ↑ Henderiks, Jorijntje; Renaud, Sabrina (2004). [§N2077.pdf "Coccolith size increase of Calcidiscus leptoporus offshore Morocco during the Last Glacial Maximum: an expression of enhanced glacial productivity?"]. Journal of Nannoplankton Research 26 (1): 1–12. doi:10.58998/jnr2114. https://ina.tmsoc.org/JNR/online/26/Henderiks & Renaud 2004 JNR 26-1 Calc lept [§N2077].pdf. Retrieved 13 April 2024.
98. ↑ Penaud, A.; Eynaud, F.; Turon, J.L.; Blamart, D.; Rossignol, L.; Marret, F.; Lopez-Martinez, C.; Grimalt, J.O. et al. (July 2010). "Contrasting paleoceanographic conditions off Morocco during Heinrich events (1 and 2) and the Last Glacial Maximum" (in en). Quaternary Science Reviews 29 (15–16): 1923–1939. doi:10.1016/j.quascirev.2010.04.011. Bibcode: 2010QSRv...29.1923P. https://linkinghub.elsevier.com/retrieve/pii/S0277379110001204. Retrieved 11 April 2024.
99. ↑ Pöppelmeier, F.; Gutjahr, M.; Blaser, P.; Oppo, D. W.; Jaccard, S. L.; Regelous, M.; Huang, K.-F.; Süfke, F. et al. (1 February 2020). "Water mass gradients of the mid-depth Southwest Atlantic during the past 25,000 years". Earth and Planetary Science Letters 531. doi:10.1016/j.epsl.2019.115963. Bibcode: 2020E&PSL.53115963P. https://www.sciencedirect.com/science/article/abs/pii/S0012821X19306557. Retrieved 15 May 2023.
100. ↑ "Mauna Kea Hawaiʻi's Tallest Volcano". USGS. https://hvo.wr.usgs.gov/volcanoes/maunakea/.
101. ↑ Shi, X.; Wu, Y.; Zou, J.; Liu, Y.; Ge, S.; Zhao, M.; Liu, J.; Zhu, A. et al. (18 September 2014). "Multiproxy reconstruction for Kuroshio responses to northern hemispheric oceanic climate and the Asian Monsoon since Marine Isotope Stage 5.1 (∼88 ka)" (in en). Climate of the Past 10 (5): 1735–1750. doi:10.5194/cp-10-1735-2014. ISSN 1814-9332. Bibcode: 2014CliPa..10.1735S. https://cp.copernicus.org/articles/10/1735/2014/. Retrieved 2 October 2023.
102. ↑ Du, Jianghui; Haley, Brian A.; Mix, Alan C.; Walczak, Maureen H.; Praetorius, Summer K. (13 August 2018). "Flushing of the deep Pacific Ocean and the deglacial rise of atmospheric CO2 concentrations". Nature Geoscience 11 (10): 749–755. doi:10.1038/s41561-018-0205-6. Bibcode: 2018NatGe..11..749D. https://www.nature.com/articles/s41561-018-0205-6?error=cookies_not_supported&code=9d162079-aec8-49e7-b8b1-e0a819250ed2. Retrieved 8 January 2023.
103. ↑ Rein, Bert; Lückge, Andreas; Reinhardt, Lutz; Sirocko, Frank; Wolf, Anja; Dullo, Wolf-Christian (December 2005). "El Niño variability off Peru during the last 20,000 years: EL NIÑO VARIABILITY OFF PERU, 0-20 KYR" (in en). Paleoceanography and Paleoclimatology 20 (4): n/a. doi:10.1029/2004PA001099.
104. ↑ Glock, Nicolaas; Erdem, Zeynep; Schönfeld, Joachim (5 December 2022). "The Peruvian oxygen minimum zone was similar in extent but weaker during the Last Glacial Maximum than Late Holocene". Communications Earth & Environment 3 (1): 307. doi:10.1038/s43247-022-00635-y. Bibcode: 2022ComEE...3..307G.
105. ↑ Struve, Torben; Wilson, David J.; Hines, Sophia K. V.; Adkins, Jess F.; Van de Flierdt, Tina (30 June 2022). "A deep Tasman outflow of Pacific waters during the last glacial period". Nature Communications 13 (1): 3763. doi:10.1038/s41467-022-31116-7. PMID 35773248. Bibcode: 2022NatCo..13.3763S.
106. ↑ Webster, Jody M.; Braga, Juan Carlos; Humblet, Marc; Potts, Donald C.; Iryu, Yasufumi; Yokoyama, Yusuke; Fujita, Kazuhiko; Bourillot, Raphael et al. (28 May 2018). "Response of the Great Barrier Reef to sea-level and environmental changes over the past 30,000 years". Nature Geoscience 11 (1): 426–432. doi:10.1038/s41561-018-0127-3. Bibcode: 2018NatGe..11..426W. https://www.nature.com/articles/s41561-018-0127-3. Retrieved 21 April 2023.
107. ↑ Braga, Juan C.; Puga-Bernabéu, Ángel; Heindel, Katrin; Patterson, Madhavi A.; Birgel, Daniel; Peckmann, Jörn; Sánchez-Almazo, Isabel M.; Webster, Jody M. et al. (15 January 2019). "Microbialites in Last Glacial Maximum and deglacial reefs of the Great Barrier Reef (IODP Expedition 325, NE Australia)". Palaeogeography, Palaeoclimatology, Palaeoecology 514: 1–17. doi:10.1016/j.palaeo.2018.10.007. ISSN 0031-0182. Bibcode: 2019PPP...514....1B. https://www.sciencedirect.com/science/article/abs/pii/S0031018218306436. Retrieved 9 September 2024.
108. ↑ Chang, Liao; Hoogakker, Babette A. A.; Heslop, David; Zhao, Xiang; Roberts, Andrew P.; De Deckker, Patrick; Xue, Pengfei; Pei, Zhaowen et al. (10 August 2023). "Indian Ocean glacial deoxygenation and respired carbon accumulation during mid-late Quaternary ice ages" (in en). Nature Communications 14 (1): 4841. doi:10.1038/s41467-023-40452-1. ISSN 2041-1723. PMID 37563128. PMC 10415292. Bibcode: 2023NatCo..14.4841C. https://www.researchgate.net/publication/373046261. Retrieved 19 December 2023.
109. ↑ Gottschalk, Julia; Michel, Elisabeth; Thöle, Lena M.; Studer, Anja S.; Hasenfratz, Adam P.; Schmid, Nicole; Butzin, Martin; Mazaud, Alain et al. (3 December 2020). "Glacial heterogeneity in Southern Ocean carbon storage abated by fast South Indian deglacial carbon release" (in en). Nature Communications 11 (1): 6192. doi:10.1038/s41467-020-20034-1. ISSN 2041-1723. PMID 33273459. Bibcode: 2020NatCo..11.6192G.
110. ↑ Nagoji, Sidhesh; Tiwari, Manish (29 January 2021). "Causes and climatic influence of centennial-scale denitrification variability in the southeastern Arabian Sea since the last glacial period" (in en). Quaternary Research 101: 156–168. doi:10.1017/qua.2020.118. ISSN 0033-5894. Bibcode: 2021QuRes.101..156N. https://www.cambridge.org/core/journals/quaternary-research/article/abs/causes-and-climatic-influence-of-centennialscale-denitrification-variability-in-the-southeastern-arabian-sea-since-the-last-glacial-period/8CBBF1EFD823E1B0D26512F51D106AF0. Retrieved 17 September 2023.
111. ↑ Shin, Ji Young; Kim, Sunghan; Xiang, Zhao; Yoo, Kyu-Cheul; Yu, Yongjae; Lee, Jae Il; Lee, Min Kyung; Yo, Il Hoon (1 November 2020). "Particle-size dependent magnetic properties of Scotia Sea sediments since the Last Glacial Maximum: Glacial ice-sheet discharge controlling magnetic proxies". Palaeogeography, Palaeoclimatology, Palaeoecology 557. doi:10.1016/j.palaeo.2020.109906. Bibcode: 2020PPP...55709906S. https://www.sciencedirect.com/science/article/abs/pii/S0031018220303515. Retrieved 4 December 2022.
112. ↑ Nair, Abhilash; Mohan, Rahul; Crosta, Xavier; Manoj, M. C.; Thamban, Meloth; Marieu, Vincent (1 June 2019). "Southern Ocean sea ice and frontal changes during the Late Quaternary and their linkages to Asian summer monsoon". Quaternary Science Reviews 213: 93–104. doi:10.1016/j.quascirev.2019.04.007. ISSN 0277-3791. Bibcode: 2019QSRv..213...93N. https://www.sciencedirect.com/science/article/pii/S0277379119300125. Retrieved 31 December 2023.
113. ↑ Stone, P.. "Late glacial period, Quaternary, Northern England". British Geological Survey. https://earthwise.bgs.ac.uk/index.php/Late_glacial_period,_Quaternary,_Northern_England.

## Further reading

* Developments in Quaternary Science Series
* Gillespie, Alan R.; Porter, Stephen C.; Atwater, Brian F. (2003). The Quaternary Period in the United States. Elsevier. ISBN 978-0-444-51471-4. https://books.google.com/books?id=ys2keOYC5AoC.
* Ehlers, Jürgen; Gibbard, Philip L. (2004). Quaternary Glaciations Extent and Chronology. 1. Europe. Elsevier. ISBN 978-0-444-51462-2. https://books.google.com/books?id=rKsL8CFcdAoC.
* Ehlers, Jürgen; Gibbard, Philip L. (2004). Quaternary Glaciations: Extent and Chronology. 2. North America. Elsevier. ISBN 978-0-444-51592-6. https://books.google.com/books?id=c0wnQqpIF-QC.
* Ehlers, Jürgen; Gibbard, Philip L. (2004). Quaternary Glaciations: Extent and Chronology. 3. South America, Asia, Africa, Australia, Antarctica. Elsevier. ISBN 978-0-444-51593-3. https://books.google.com/books?id=2xpIEPH7RW4C.
* Šibrava, Vladimír (1986). "Quaternary Glaciations in the Northern Hemisphere". Quaternary Science Reviews 5: 1–514. doi:10.1016/0277-3791(86)90167-8. Bibcode: 1986QSRv....5....1S. http://www.sciencedirect.com/science/journal/02773791/5.

## External links

* Adams, J.M. (1997). "Global land environments since the last interglacial". Atlas of Palaeovegetation: Preliminary land ecosystem maps of the world since the Last Glacial Maximum. Oak Ridge National Laboratory, TN. http://www.esd.ornl.gov/projects/qen/nerc.html.
* "Map and GIS database of glacial landforms and features related to the last British Ice Sheet". BRITICE. Department of Geology, University of Sheffield. 2004. http://www.sheffield.ac.uk/geography/staff/clark_chris/britice.html.
* Dyke, A.S.; Moore, A.; Robertson, L. (2003). "Deglaciation of North America". Geological Survey of Canada Open File, 1574. http://geopub.nrcan.gc.ca/moreinfo_e.php?id=214399. (32 digital maps at 1:7 000 000 scale with accompanying digital chronological database and one poster (two sheets) with full map series.)
* Manley, W.; Kuaffman, D.. "Alaska PaleoGlacier Atlas: A Geospatial Compilation of Pleistocene Glacier Extents". INSTAAR. University of Colorado. http://instaar.colorado.edu/QGISL/ak_paleoglacier_atlas/index.html.
* Paleoclimate Modelling Intercomparison Project (PMIP) PMIP Web Site and 'Publications : Last Glacial Maximum.
* Paleoclimate Modelling Intercomparison Project Phase II (PMIP2) PMIP2 Home page and PMIP 2 Publications.
* Osipov, Eduard Y.; Khlystov, Oleg M.. "Glaciers and meltwater flux to Lake Baikal during the Last Glacial Maximum". http://ice.tsu.ru/index.php?option=com_content&view=category&layout=blog&id=43&Itemid=88&limitstart=5.

* v
* t
* e

Continental glaciations

General|

* Cordilleran ice sheet
* Laurentide Ice Sheet
* Last Glacial Maximum
* Canadian Shield
* Glacial history of Minnesota
* List of prehistoric lakes
* Proglacial lake
* Lake Agassiz
* Lake Chicago
* Lake Tight
* Teays River
* Post-glacial rebound
* Timeline of glaciation

Landforms|

| Erosional|

* Fjord
* Glacial striae
* Ribbon lake
* Roche moutonnée
* Tunnel valley
* U-shaped valley

|

Depositional|

* Drumlin
* Erratic block
* Moraine
* Pulju moraine
* Rogen moraine
* Terminal moraine
* Till plain
* Veiki moraine

| Glacifluvial|

* Diluvium
* Esker
* Giant current ripples
* Kame
* Kame delta
* Kettle hole
* Outwash fan
* Sandur

|

North America|

| Canada|

* Arrowhead Provincial Park, Ontario
* Big Rock (glacial erratic), Alberta
* Cypress Hills (Canada), Saskatchewan
* Eramosa River, Ontario
* Eskers Provincial Park, British Columbia
* Foothills Erratics Train, Alberta
* Lion's Head Provincial Park, Ontario
* Origin of the Oak Ridges Moraine, Ontario
* Ovayok Territorial Park, Nunavut

|

United
States|

* Chippewa Moraine State Recreation Area, Wisconsin
* Coteau des Prairies, South Dakota
* Devil's Lake State Park, Wisconsin
* Glacial Lake Wisconsin, Wisconsin
* Glacial Lakes State Park, Minnesota
* Horicon Marsh State Wildlife Area, Wisconsin
* Ice Age Floods National Geologic Trail, Idaho, Oregon & Washington
* Ice Age National Scientific Reserve, Wisconsin
* Ice Age Trail, Wisconsin
* Interstate State Park, Minnesota & Wisconsin
* Kelleys Island, Ohio
* Kettle Moraine State Forest, Wisconsin
* Lake Bonneville, Utah
* Lake Lahontan, Nevada
* Lake Missoula, Montana
* Mill Bluff State Park, Wisconsin
* Oneida Lake, New York
* Two Creeks Buried Forest State Natural Area, Wisconsin
* Withrow Moraine and Jameson Lake Drumlin Field, Washington
* Yosemite National Park, California

Eurasia and
Antarctica|

* Antarctica
* Hardangerfjord
* Killary Harbour
* Lambert Glacier
* Monte Rosa
* Ross Ice Shelf
* Svalbard

Time periods|

* Quaternary glaciation
* Illinoian Stage
* Interglacial
* Interstadial
* Penultimate Glacial Period
* Last Glacial Period
* Last Glacial Maximum
* Mousterian Pluvial
* Holocene glacial retreat
* Oldest Dryas
* Older Dryas
* Pleistocene
* Pre-Illinoian Stage
* Quaternary glaciation
* Sangamonian Stage
* Wisconsin glaciation
* Bølling-Allerød warming
* Late Glacial Interstadial
* Huelmo–Mascardi Cold Reversal
* Younger Dryas
* African humid period
* 8.2 kiloyear event
* 4.2 kiloyear event
* Piora Oscillation
* Little Ice Age

* Category

* v
* t
* e

Ice ages

Quaternary /
Late Cenozoic|

| Quaternary|

* Antarctica
* Greenland
* Penultimate Glacial Period
* Last Glacial Period (Last Glacial Maximum)
* 1st: Würm, Wisconsin, Weichselian, Devensian/Midlandian, Pinedale/Fraser, Merida, Llanquihue
* 2nd: Riss, Illinoian, Saale, Wolstonian, Santa María
* 3rd–6th: Mindel, Pre-Illinoian, Elster, Anglian, Rio Llico
* 7th–8th: Günz, Pre-Illinoian, Elbe or Menapian, Beestonian, Caracol (2.5 to 0 Mya)

|

Pliocene
Miocene
Oligocene|

* Antarctic (34 to 2.5 Mya)

Carboniferous–Permian|

* Late Paleozoic icehouse (360 Mya to 260 Mya)

Late Ordovician glaciation|

* Andean-Saharan (460 Mya to 430 Mya)

Ediacaran|

* Gaskiers (579.88 to 579.63 Mya)
* Baykonurian (547 to 541.5 Mya)

Cryogenian|

* Sturtian (717 to 660 Mya); Marinoan (650 to 635 Mya)

Paleoproterozoic|

* Huronian (2.4 to 2.1 Gya)

Mesoarchean|

* Pongola (2.9 to 2.78 Gya)

Related topics|

* Greenhouse and icehouse Earth
* Great Oxygenation Event
* Snowball Earth
* Interglacial
* Milankovitch cycles
* Stadial

Timeline of glaciation

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