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Last glacial period
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For the most recent period cooler than present but without significant glaciation, see Little Ice Age. For the full sequence of geologically recent glacial advances and retreats, see Quaternary glaciation. For the geological epoch often associated with or referred to as "The Ice Age", see Pleistocene.
For a generic geological period of reduced temperature and increased glaciation, see Ice age.
"Last glacial" redirects here. For the period of maximum glacier extent during this time, see Last Glacial Maximum.
Chronology of climatic events of importance for the last glacial period (about the last 120,000 years)
The last glacial period occurred from the end of the Eemian interglacial to the end of the Younger Dryas, encompassing the period c. 110,000 – c. 11,700 years ago. This most recent glacial period is part of a larger pattern of glacial and interglacial periods known as the Quaternary glaciation extending from c. 2,588,000 years ago to present.[1]
During this last glacial period there were alternating episodes of glacier advance and retreat. Within the last glacial period the Last Glacial Maximum was approximately 22,000 years ago. While the general pattern of global cooling and glacier advance was similar, local differences in the development of glacier advance and retreat make it difficult to compare the details from continent to continent (see picture of ice core data below for differences). Approximately 13,000 years ago, the Late Glacial Maximum began. The end of the Younger Dryas about 11,700 years ago marked the beginning of the Holocene geological epoch, which includes the Holocene glacial retreat.
From the point of view of human archaeology, the last glacial period falls in the Paleolithic and early Mesolithic periods. When the glaciation event started, Homo sapiens was confined to lower latitudes and used tools comparable to those used by Neanderthals in western and central Eurasia and by Homo erectus in Asia. Near the end of the event, Homo sapiens migrated into Eurasia and Australia. Archaeological and genetic data suggest that the source populations of Paleolithic humans survived the last glacial period in sparsely wooded areas and dispersed through areas of high primary productivity while avoiding dense forest cover.[2] The retreat of the glaciers 15,000 years ago allowed groups of humans from Asia to migrate to the Americas.
Artist impression of the last glacial period at glacial maximum[3]
Contents
[hide]
1 Origin and definition
2 Overview
2.1 Northern Hemisphere
2.2 Southern Hemisphere
3 Deglaciation
4 Named local glaciations
4.1 Antarctica glaciation
4.2 Europe
4.2.1 Devensian and Midlandian glaciation (Britain and Ireland)
4.2.2 Weichselian glaciation (Scandinavia and northern Europe)
4.2.3 Würm glaciation (Alps)
4.3 North America
4.3.1 Pinedale or Fraser glaciation (Rocky Mountains)
4.3.2 Wisconsin glaciation
4.3.3 Tahoe, Tenaya, and Tioga, Sierra Nevada
4.3.4 Greenland glaciation
4.4 South America
4.4.1 Mérida glaciation (Venezuelan Andes)
4.4.2 Llanquihue glaciation (Southern Andes)
5 See also
6 Notes
7 References
8 Further reading
9 External links
Origin and definition[edit]
The last glacial period is sometimes colloquially referred to as the "last ice age", though this use is incorrect because an ice age is a longer period of cold temperature in which year-round ice sheets are present near one or both poles. Glacials are colder phases within an ice age in which glaciers advance; glacials are separated by interglacials. Thus, the end of the last glacial period, which was about 11,700 years ago, is not the end of the last ice age since extensive year-round ice persists in Antarctica and Greenland. Over the past few million years the glacial-interglacial cycles have been "paced" by periodic variations in the Earth's orbit via Milankovitch cycles.
The last glacial period is the best-known part of the current ice age, and has been intensively studied in North America, northern Eurasia, the Himalaya and other formerly glaciated regions around the world. The glaciations that occurred during this glacial period covered many areas, mainly in the Northern Hemisphere and to a lesser extent in the Southern Hemisphere. They have different names, historically developed and depending on their geographic distributions: Fraser (in the Pacific Cordillera of North America), Pinedale (in the Central Rocky Mountains), Wisconsinan or Wisconsin (in central North America), Devensian (in the British Isles), Midlandian (in Ireland), Würm (in the Alps), Mérida (in Venezuela), Weichselian or Vistulian (in Northern Europe and northern Central Europe), Valdai in Russia and Zyryanka in Siberia, Llanquihue in Chile, and Otira in New Zealand. The geochronological Late Pleistocene comprises the late glacial (Weichselian) and the immediately preceding penultimate interglacial (Eemian) period.
Overview[edit]
Vegetation types at time of Last Glacial Maximum
Last glacial period, as seen in ice core data from Antarctica and Greenland
The last glaciation centered on the huge ice sheets of North America and Eurasia. Considerable areas in the Alps, the Himalaya and the Andes were ice-covered, and Antarctica remained glaciated.
Northern Hemisphere[edit]
Canada was nearly completely covered by ice, as well as the northern part of the United States, both blanketed by the huge Laurentide Ice Sheet. Alaska remained mostly ice free due to arid climate conditions. Local glaciations existed in the Rocky Mountains and the Cordilleran Ice Sheet and as ice fields and ice caps in the Sierra Nevada in northern California.[4] In Britain, mainland Europe, and northwestern Asia, the Scandinavian ice sheet once again reached the northern parts of the British Isles, Germany, Poland, and Russia, extending as far east as the Taymyr Peninsula in western Siberia.[5] The maximum extent of western Siberian glaciation was reached by approximately 16,000–15,000 BC and thus later than in Europe (c. 20,000 – c. 16,000 BC).[6] Northeastern Siberia was not covered by a continental-scale ice sheet.[7] Instead, large, but restricted, icefield complexes covered mountain ranges within northeast Siberia, including the Kamchatka-Koryak Mountains.[8][9]
The Arctic Ocean between the huge ice sheets of America and Eurasia was not frozen throughout, but like today probably was only covered by relatively shallow ice, subject to seasonal changes and riddled with icebergs calving from the surrounding ice sheets. According to the sediment composition retrieved from deep-sea cores there must even have been times of seasonally open waters.[10]
Outside the main ice sheets, widespread glaciation occurred on the Alps−Himalaya mountain chain. In contrast to the earlier glacial stages, the Würm glaciation was composed of smaller ice caps and mostly confined to valley glaciers, sending glacial lobes into the Alpine foreland. To the east the Caucasus and the mountains of Turkey and Iran were capped by local ice fields or small ice sheets.[11]
In the Himalaya and the Tibetan Plateau, glaciers advanced considerably, particularly between 45,000 and 25,000 BC,[12] but these datings are controversial.[13][14] The formation of a contiguous ice sheet on the Tibetan Plateau[15][16] is controversial.[17]
Other areas of the Northern Hemisphere did not bear extensive ice sheets, but local glaciers in high areas. Parts of Taiwan, for example, were repeatedly glaciated between 42,250 and 8,680 BCE[18] as well as the Japanese Alps. In both areas maximum glacier advance occurred between 58,000 and 28,000 BCE.[19] To a still lesser extent glaciers existed in Africa, for example in the High Atlas, the mountains of Morocco, the Mount Atakor massif in southern Algeria, and several mountains in Ethiopia. In the Southern Hemisphere, an ice cap of several hundred square kilometers was present on the east African mountains in the Kilimanjaro massif, Mount Kenya and the Rwenzori Mountains, still bearing remnants of glaciers today.[20]
Southern Hemisphere[edit]
Glaciation of the Southern Hemisphere was less extensive because of current configuration of continents. Ice sheets existed in the Andes (Patagonian Ice Sheet), where six glacier advances between 31,500 and 11,900 BC in the Chilean Andes have been reported.[21] Antarctica was entirely glaciated, much like today, but the ice sheet left no uncovered area. In mainland Australia only a very small area in the vicinity of Mount Kosciuszko was glaciated, whereas in Tasmania glaciation was more widespread.[22] An ice sheet formed in New Zealand, covering all of the Southern Alps, where at least three glacial advances can be distinguished.[23] Local ice caps existed in Irian Jaya, Indonesia, where in three ice areas remnants of the Pleistocene glaciers are still preserved today.[24]
Small glaciers developed in a few favorable places in Southern Africa during the last glacial period.[25][A][B] These small glaciers would have developed in the Lesotho Highlands and parts of the Drakensberg.[27][28] The development of glaciers was likely aided by localized cooling indebted to shading by adjacent cliffs.[28] Various moraines and former glacier niches have been identified in the eastern Lesotho Highlands, above 3,000 m.a.s.l. and on south-facing slopes, a few kilometres west of the Great Escarpment.[27] Studies suggest the mountains of Southern Africa were mostly subject to mild periglaciation during the last glacial cycle and the annual average temperatures were about 6 °C colder than at present. The estimated 6 °C temperature drop for Southern Africa is in line with temperature drops estimated for Tasmania and southern Patagonia during the same time.[25][26] The environment of the Lesotho Highlands during the Last Glacial Maximum was one of a relatively arid periglaciation without permafrost but with deep seasonal freezing on south-facing slopes. Periglaciation in the Eastern Drakensberg and Lesotho Highlands produced solifluction deposits, blockfields and blockstreams, and stone garlands.[25][26]
Deglaciation[edit]
See also: Bølling-Allerød warming, Meltwater pulse 1A, and Deglaciation
Scientists from the Center for Arctic Gas Hydrate, Environment (CAGE) and Climate at the Arctic University of Norway, published a study in June 2017[29] describing over a hundred ocean sediment craters, some 3,000 meters wide and up to 300 meters deep, formed by explosive eruptions of methane from destabilized methane hydrates, following ice-sheet retreat during the last glacial period, around 12,000 years ago. These areas around the Barents Sea still seep methane today. The study hypothesized that existing bulges containing methane reservoirs could eventually have the same fate.
Named local glaciations[edit]
Antarctica glaciation[edit]
During the last glacial period Antarctica was blanketed by a massive ice sheet, much as it is today. The ice covered all land areas and extended into the ocean onto the middle and outer continental shelf.[30][31] According to ice modelling, ice over central East Antarctica was generally thinner than today.[32]
Europe[edit]
Devensian and Midlandian glaciation (Britain and Ireland)[edit]
The name Devensian glaciation is used by British geologists and archaeologists and refers to what is often popularly meant by the latest ice age. Irish geologists, geographers, and archaeologists refer to the Midlandian glaciation as its effects in Ireland are largely visible in the Irish Midlands. The name Devensian is derived from the Latin Dēvenses, people living by the Dee (Dēva in Latin), a river on the Welsh border near which deposits from the period are particularly well represented.[33]
The effects of this glaciation can be seen in many geological features of England, Wales, Scotland, and Northern Ireland. Its deposits have been found overlying material from the preceding Ipswichian stage and lying beneath those from the following Flandrian interglacial stage of the Holocene.
The latter part of the Devensian includes Pollen zones I-IV, the Allerød oscillation and Bølling oscillation, and the Older Dryas and Younger Dryas climatic stages.
Weichselian glaciation (Scandinavia and northern Europe)[edit]
Main article: Weichselian glaciation
Europe during the last glacial period
Alternative names include: Weichsel glaciation or Vistulian glaciation (referring to the Polish river Vistula or its German name Weichsel). Evidence suggests that the ice sheets were at their maximum size for only a short period, between 25,000 and 13,000 BP. Eight interstadials have been recognized in the Weichselian, including: the Oerel, Glinde, Moershoofd, Hengelo and Denekamp; however correlation with isotope stages is still in process.[34][35] During the glacial maximum in Scandinavia, only the western parts of Jutland were ice-free, and a large part of what is today the North Sea was dry land connecting Jutland with Britain (see Doggerland). It is also in Denmark that the only Scandinavian ice-age animals older than 13,000 BCE are found.[citation needed]
The Baltic Sea, with its unique brackish water, is a result of meltwater from the Weichsel glaciation combining with saltwater from the North Sea when the straits between Sweden and Denmark opened. Initially, when the ice began melting about 10,300 BP, seawater filled the isostatically depressed area, a temporary marine incursion that geologists dub the Yoldia Sea. Then, as post-glacial isostatic rebound lifted the region about 9500 BP, the deepest basin of the Baltic became a freshwater lake, in palaeological contexts referred to as Ancylus Lake, which is identifiable in the freshwater fauna found in sediment cores. The lake was filled by glacial runoff, but as worldwide sea level continued rising, saltwater again breached the sill about 8000 BP, forming a marine Littorina Sea which was followed by another freshwater phase before the present brackish marine system was established. "At its present state of development, the marine life of the Baltic Sea is less than about 4000 years old", Drs. Thulin and Andrushaitis remarked when reviewing these sequences in 2003.
Overlying ice had exerted pressure on the Earth's surface. As a result of melting ice, the land has continued to rise yearly in Scandinavia, mostly in northern Sweden and Finland where the land is rising at a rate of as much as 8–9 mm per year, or 1 meter in 100 years. This is important for archaeologists since a site that was coastal in the Nordic Stone Age now is inland and can be dated by its relative distance from the present shore.
Würm glaciation (Alps)[edit]
Main article: Würm glaciation
Extent of Alpine glaciation during the Würm ice age. Blue: extent of the early ice ages:
The term Würm is derived from a river in the Alpine foreland, approximately marking the maximum glacier advance of this particular glacial period. The Alps were where the first systematic scientific research on ice ages was conducted by Louis Agassiz at the beginning of the 19th century. Here the Würm glaciation of the last glacial period was intensively studied. Pollen analysis, the statistical analyses of microfossilized plant pollens found in geological deposits, chronicled the dramatic changes in the European environment during the Würm glaciation. During the height of Würm glaciation, c. 24,000 – c. 10,000 BP, most of western and central Europe and Eurasia was open steppe-tundra, while the Alps presented solid ice fields and montane glaciers. Scandinavia and much of Britain were under ice.
During the Würm, the Rhône Glacier covered the whole western Swiss plateau, reaching today's regions of Solothurn and Aarau. In the region of Bern it merged with the Aar glacier. The Rhine Glacier is currently the subject of the most detailed studies. Glaciers of the Reuss and the Limmat advanced sometimes as far as the Jura. Montane and piedmont glaciers formed the land by grinding away virtually all traces of the older Günz and Mindel glaciation, by depositing base moraines and terminal moraines of different retraction phases and loess deposits, and by the pro-glacial rivers' shifting and redepositing gravels. Beneath the surface, they had profound and lasting influence on geothermal heat and the patterns of deep groundwater flow.
North America[edit]
Pinedale or Fraser glaciation (Rocky Mountains)[edit]
The Pinedale (central Rocky Mountains) or Fraser (Cordilleran Ice Sheet) glaciation was the last of the major glaciations to appear in the Rocky Mountains in the United States. The Pinedale lasted from approximately 30,000 to 10,000 years ago and was at its greatest extent between 23,500 and 21,000 years ago.[36] This glaciation was somewhat distinct from the main Wisconsin glaciation as it was only loosely related to the giant ice sheets and was instead composed of mountain glaciers, merging into the Cordilleran Ice Sheet.[37] The Cordilleran Ice Sheet produced features such as glacial Lake Missoula, which would break free from its ice dam causing the massive Missoula Floods. USGS geologists estimate that the cycle of flooding and reformation of the lake lasted an average of 55 years and that the floods occurred approximately 40 times over the 2,000 year period between 15,000 and 13,000 years ago.[38] Glacial lake outburst floods such as these are not uncommon today in Iceland and other places.
Wisconsin glaciation[edit]
The Wisconsin Glacial Episode was the last major advance of continental glaciers in the North American Laurentide Ice Sheet. At the height of glaciation the Bering land bridge potentially permitted migration of mammals, including people, to North America from Siberia.
It radically altered the geography of North America north of the Ohio River. At the height of the Wisconsin Episode glaciation, ice covered most of Canada, the Upper Midwest, and New England, as well as parts of Montana and Washington. On Kelleys Island in Lake Erie or in New York's Central Park, the grooves left by these glaciers can be easily observed. In southwestern Saskatchewan and southeastern Alberta a suture zone between the Laurentide and Cordilleran ice sheets formed the Cypress Hills, which is the northernmost point in North America that remained south of the continental ice sheets.
The Great Lakes are the result of glacial scour and pooling of meltwater at the rim of the receding ice. When the enormous mass of the continental ice sheet retreated, the Great Lakes began gradually moving south due to isostatic rebound of the north shore. Niagara Falls is also a product of the glaciation, as is the course of the Ohio River, which largely supplanted the prior Teays River.
With the assistance of several very broad glacial lakes, it released floods through the gorge of the Upper Mississippi River, which in turn was formed during an earlier glacial period.
In its retreat, the Wisconsin Episode glaciation left terminal moraines that form Long Island, Block Island, Cape Cod, Nomans Land, Martha's Vineyard, Nantucket, Sable Island, and the Oak Ridges Moraine in south central Ontario, Canada. In Wisconsin itself, it left the Kettle Moraine. The drumlins and eskers formed at its melting edge are landmarks of the Lower Connecticut River Valley.
Tahoe, Tenaya, and Tioga, Sierra Nevada[edit]
In the Sierra Nevada, there are three named stages of glacial maxima (sometimes incorrectly called ice ages) separated by warmer periods. These glacial maxima are called, from oldest to youngest, Tahoe, Tenaya, and Tioga.[39] The Tahoe reached its maximum extent perhaps about 70,000 years ago. Little is known about the Tenaya. The Tioga was the least severe and last of the Wisconsin Episode. It began about 30,000 years ago, reached its greatest advance 21,000 years ago, and ended about 10,000 years ago.
Greenland glaciation[edit]
In Northwest Greenland, ice coverage attained a very early maximum in the last glacial period around 114,000. After this early maximum, the ice coverage was similar to today until the end of the last glacial period. Towards the end, glaciers readvanced once more before retreating to their present extent.[40] According to ice core data, the Greenland climate was dry during the last glacial period, precipitation reaching perhaps only 20% of today's value.[41]
South America[edit]
Mérida glaciation (Venezuelan Andes)[edit]
Map showing the extent of the glaciated area in Venezuelan Andes during the Mérida glaciation
The name Mérida Glaciation is proposed to designate the alpine glaciation which affected the central Venezuelan Andes during the Late Pleistocene. Two main moraine levels have been recognized: one with an elevation of 2,600–2,700 m (8,500–8,900 ft), and another with an elevation of 3,000–3,500 m (9,800–11,500 ft). The snow line during the last glacial advance was lowered approximately 1,200 m (3,900 ft) below the present snow line, which is 3,700 m (12,100 ft). The glaciated area in the Cordillera de Mérida was approximately 600 km2 (230 sq mi); this included the following high areas from southwest to northeast: Páramo de Tamá, Páramo Batallón, Páramo Los Conejos, Páramo Piedras Blancas, and Teta de Niquitao. Approximately 200 km2 (77 sq mi) of the total glaciated area was in the Sierra Nevada de Mérida, and of that amount, the largest concentration, 50 km2 (19 sq mi), was in the areas of Pico Bolívar, Pico Humboldt [4,942 m (16,214 ft)], and Pico Bonpland [4,983 m (16,348 ft)]. Radiocarbon dating indicates that the moraines are older than 10,000 BP, and probably older than 13,000 BP. The lower moraine level probably corresponds to the main Wisconsin glacial advance. The upper level probably represents the last glacial advance (Late Wisconsin).[42][43][44][45]
Llanquihue glaciation (Southern Andes)[edit]
Main article: Llanquihue glaciation
Map showing the extent of the Patagonian Ice Sheet in the Strait of Magellan area during the last glacial period. Selected modern settlements are shown with yellow dots.
The Llanquihue glaciation takes its name from Llanquihue Lake in southern Chile which is a fan-shaped piedmont glacial lake. On the lake's western shores there are large moraine systems of which the innermost belong to the last glacial period. Llanquihue Lake's varves are a node point in southern Chile's varve geochronology. During the last glacial maximum the Patagonian Ice Sheet extended over the Andes from about 35°S to Tierra del Fuego at 55°S. The western part appears to have been very active, with wet basal conditions, while the eastern part was cold based. Cryogenic features like ice wedges, patterned ground, pingos, rock glaciers, palsas, soil cryoturbation, solifluction deposits developed in unglaciated extra-Andean Patagonia during the Last Glaciation. However, not all these reported features have been verified.[46] The area west of Llanquihue Lake was ice-free during the LGM, and had sparsely distributed vegetation dominated by Nothofagus. Valdivian temperate rain forest was reduced to scattered remnants in the western side of the Andes.[47]
Modelled maximum extent of the Antarctic ice sheet 21,000 years before present
See also[edit]
Glacial history of Minnesota
Glacial lake outburst flood
Glacial period
Ice age
Last Glacial Maximum
Pleistocene
Pleistocene megafauna
Plio-Pleistocene
Quaternary extinction event
Quaternary glaciation
Sea level rise
Stone Age
Timeline of glaciation
Valparaiso Moraine
Notes[edit]
Jump up ^ Prior to the 2010s there was considerable debate on whether Southern Africa was glaciated during the last glacial cycle or not.[25][26]
Jump up ^ The former existence of large glaciers or deep snow cover over much of the Lesotho Highlands has been judged unlikely considering the lack of glacial morphology (e.g. rôche moutonnées) and the existence of periglacial regolith that has not been reworked by glaciers.[26] Estimates of the mean annual temperature in Southern Africa during the Last Glacial Maximum indicate the temperatures were not low enough to initiate or sustain a widespread glaciation. The former existence of rock glaciers or large glaciers is according to the same study ruled out, because of a lack of conclusive field evidence and the implausibility of the 10-17° C temperature drop, relative to the present, that such features would imply.[25]
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Jump up ^ Huybrechts, P. (2002). "Sea-level changes at the LGM from ice-dynamic reconstructions of the Greenland and Antarctic ice sheets during the glacial cycles". Quaternary Science Reviews. 21 (1–3): 203–231. doi:10.1016/S0277-3791(01)00082-8.
Jump up ^ OED
Jump up ^ Behre Karl-Ernst, van der Plicht Johannes (1992). "Towards an absolute chronology for the last glacial period in Europe: radiocarbon dates from Oerel, northern Germany". Vegetation History and Archaeobotany. 1 (2): 111–117. doi:10.1007/BF00206091.
Jump up ^ Davis, Owen K. (2003) "Non-Marine Records: Correlations with the Marine Sequence" Introduction to Quaternary Ecology University of Arizona web site, doi: 2003618-145735g
Jump up ^ "Brief geologic history". Rocky Mountain National Park. Archived from the original on May 15, 2006.
Jump up ^ "Ice Age Floods". U.S. National Park Service.
Jump up ^ Waitt, Jr., Richard B. (October 1985). "Case for periodic, colossal jökulhlaups from Pleistocene glacial Lake Missoula". Geological Society of America Bulletin. 96 (10): 1271–86. doi:10.1130/0016-7606(1985)96<1271:CFPCJF>2.0.CO;2. CS1 maint: Multiple names: authors list (link)
Jump up ^ Ehlers, Gibbard & 2004 II, p. 57
Jump up ^ Funder, Svend "Late Quaternary stratigraphy and glaciology in the Thule area, Northwest Greenland". MoG Geoscience. 22: 63. 1990. Archived from the original on June 6, 2007.
Jump up ^ Johnsen, Sigfus J.; et al. (1992). "A "deep" ice core from East Greenland". MoG Geoscience. 29: 22. Archived from the original on June 6, 2007.
Jump up ^ Schubert, Carlos (1998). "Glaciers of Venezuela". US Geological Survey (USGS P 1386-I).
Jump up ^ Schubert, C.; Valastro, S. (1974). "Late Pleistocene glaciation of Páramo de La Culata, north-central Venezuelan Andes" (PDF). Geologische Rundschau. 63 (2): 516–538. doi:10.1007/BF01820827.
Jump up ^ Mahaney, William C.; Milner, M.W., Kalm, Volli; Dirsowzky, Randy W.; Hancock, R.G.V.; Beukens, Roelf P. (April 1, 2008). "Evidence for a Younger Dryas glacial advance in the Andes of northwestern Venezuela". Geomorphology. 96 (1–2): 199–211. doi:10.1016/j.geomorph.2007.08.002. CS1 maint: Multiple names: authors list (link)
Jump up ^ Maximiliano, B.; Orlando, G.; Juan, C.; Ciro, S. "Glacial Quaternary geology of las Gonzales basin, páramo los conejos, Venezuelan andes".
Jump up ^ Trombotto Liaudat, Darío (2008). "Geocryology of Southern South America". In Rabassa, J. The Late Cenozoic of Patagonia and Tierra del Fuego. pp. 255–268. ISBN 978-0-444-52954-1.
Jump up ^ Adams, Jonathan. "South America during the last 150,000 years". Archived from the original on January 30, 2010.
Further reading[edit]
Bowen, D.Q. (1978). Quaternary geology: a stratigraphic framework for multidisciplinary work. Oxford UK: Pergamon Press. ISBN 978-0-08-020409-3.
Ehlers, J.; Gibbard, P. L., eds. (2004). Quaternary Glaciations: Extent and Chronology 2: Part II North America. Amsterdam: Elsevier. ISBN 0-444-51462-7.
Ehlers, J.; Gibbard, P. L., eds. (2004). Quaternary Glaciations: Extent and Chronology 3: Part III: South America, Asia, Africa, Australia, Antarctica. Amsterdam: Elsevier. ISBN 0-444-51593-3.
Gillespie, A. R., Porter, S. C.; Atwater, B. F. (2004). The Quaternary Period in the United States [of America]. Developments in Quaternary Science. 1. Amsterdam: Elsevier. ISBN 978-0-444-51471-4. CS1 maint: Multiple names: authors list (link)
Harris, A. G.; Tuttle, E.; Tuttle, S. D. (1997). Geology of National Parks (5th ed.). Iowa: Kendall/Hunt. ISBN 0-7872-5353-7.
Kuhle, M. (1988). "The Pleistocene Glaciation of Tibet and the Onset of Ice Ages — An Autocycle HypothesisGeoJournal". GeoJournal. 17 (4): 581–596. doi:10.1007/BF00209444.
Mangerud, J.; Ehlers, J.; Gibbard, P., eds. (2004). Quaternary Glaciations : Extent and Chronology 1: Part I Europe. Amsterdam: Elsevier. ISBN 0-444-51462-7.
Sibrava, V.; Bowen, D.Q; Richmond, G. M. (1986). "Quaternary Glaciations in the Northern Hemisphere". Quaternary Science Reviews. 5: 1–514. doi:10.1016/S0277-3791(86)80002-6.
Pielou, E. C. (1991). After the Ice Age : The Return of Life to Glaciated North America. Chicago IL: University Of Chicago Press. ISBN 0-226-66812-6.
External links[edit]
Wikimedia Commons has media related to Ice age.
Pielou, E. C. After the Ice Age: The Return of Life to Glaciated North America (University of Chicago Press: 1992)
National Atlas of the USA: Wisconsin Glaciation in North America: Present state of knowledge
Ray, N.; Adams, J.M. (2001). "A GIS-based Vegetation Map of the World at the Last Glacial Maximum (25,000–15,000 BP)" (PDF). Internet Archaeology. 11.
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Pilgrims' Way
From Wikipedia, the free encyclopedia
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For other uses, see Pilgrims' Way (disambiguation).
Pilgrims' Way
Pilgrims' Way near Westwell, Kent
Length
192 km (119 mi)
Location
South Eastern England, United Kingdom
Trailheads
Winchester, Hampshire
Shrine of Thomas Becket, Canterbury, Kent
Use
Hiking, cycling and byway; former pilgrim way
Hiking details
Season
All year
The Pilgrims' Way (also Pilgrim's Way or Pilgrims Way)[a] is the historical route taken by pilgrims from Winchester in Hampshire, England, to the shrine of Thomas Becket at Canterbury in Kent. This name, of comparatively recent coinage, is applied to a pre-existing ancient trackway dated by archaeological finds to 600–450 BC, but probably in existence since the stone age.[1][2] The prehistoric route followed the "natural causeway" east to west on the southern slopes of the North Downs.[3]
The course was dictated by the natural geography: it took advantage of the contours, avoided the sticky clay of the land below but also the thinner, overlying "clay with flints" of the summits.[4] In places a coexisting ridgeway and terrace way can be identified; the route followed would have varied with the season, but it would not drop below the upper line of cultivation.[5][6] The trackway ran the entire length of the North Downs, leading to and from Folkestone: the pilgrims would have had to turn away from it, north along the valley of the Great Stour near Chilham, to reach Canterbury.
Contents
1 History
2 Route
3 Walk
4 Notes
5 References
6 External links
History[edit]
Map of Pilgrims Way near Titsey, Surrey. The upper route, on the brow of the North Downs, is the ancient trackway (note the archaeological finds at the top left); the lower, almost in the valley, is the route surmised by the Ordnance Survey in the 19th century
A section of the lower route, eroded into the slope, in Surrey
The prehistoric trackway extended further than the present Way, providing a link from the narrowest part of the English Channel to the important religious complexes of Avebury and Stonehenge, in Wiltshire, where it is known as the Harroway.[7][8] The route was still followed as an artery for through traffic in Roman times, a period of continuous use of more than 3000 years.[2]
From Thomas Becket's canonization in 1173, until the dissolution of the monasteries in 1538, his shrine at Canterbury became the most important in the country, indeed "after Rome...the chief shrine in Christendom",[9] and it drew pilgrims from far and wide. Winchester, apart from being an ecclesiastical centre in its own right (the shrine of St Swithin), was an important regional focus and an aggregation point for travellers arriving through the seaports on the south coast.[4] Indeed, this was the route taken by Henry II on his pilgrimage of atonement for the death of Bishop Thomas from France To Canterbury in July 1174.[10][11] Travellers from Winchester to Canterbury naturally used the ancient way, as it was the direct route, and research by local historians has provided much by way of detail—sometimes embellished—of the pilgrims' journeys. The numbers making their way to Canterbury by this route were not recorded, but the estimate by the Kentish historian William Coles Finch that it carried more than 100,000 pilgrims a year is surely an exaggeration.[12][13] A separate (and more reliably attested) route to Canterbury from London was by way of Watling Street, as followed by the storytellers in The Canterbury Tales by Geoffrey Chaucer.
Conversely, the concept of a single route called the Pilgrims' Way could be no older than the Victorian Ordnance Survey map of Surrey, whose surveyor, Edward Renouard James, published a pamphlet in 1871 entitled Notes on the Pilgrims' Way in West Surrey. Here he asserted that the route was "little studied" and that "very many persons in the neighbourhood" had not been aware of it.[14] His insertion of the route name on the Ordnance map gave an official sanction to his conjecture; and writers such as Hilaire Belloc were eager to follow it up. In fact, the route as shown on modern maps is not only unsuitable for the mass movement of travellers but has also left few traces of their activity.[15] The official history of the Ordnance Survey acknowledges the "enduring archaeological blunder", blaming the enthusiasm for history of the then Director, General Sir Henry James.[16] Together, romantically inclined authors have succeeded in creating "a fable of...modern origin" to explain the existence of the Way.[2] However, F.C.Elliston-Erwood, A Kentish historian, notes that tithe records dating from before 1815 use the well established name "Pilgrims' Way" to reference and locate pieces of land. Earlier still, surviving thirteenth century documents show a "Pilgrim Road" by the walls of Thornham Castle, Kent, on what is today considered the route.[17][18]
The Pilgrims' Way is at the centre of the Powell and Pressburger film A Canterbury Tale, with the camera panning along a map of the route at the start of the film.[19]
Route[edit]
In the Middle Ages the pilgrims' route left the ancient trackway to climb St Martha's Hill[2]
On the Pilgrims' Way near Trottiscliffe, Kent
Anyone walking the 'Pilgrims Way' from Winchester would have started along the Roman road east following the route through New Alresford, Four Marks, Alton and Bentley to Farnham. This roughly follows the modern A31.
The ancient main streets of towns along the route from Farnham (where the old trackway converges with the pilgrims' route)[2] through Guildford, Dorking and Reigate align west to east, strongly suggesting that this was the most important route that passed through them. On modern Ordnance Survey maps, part of the route is shown running east from Farnham via the heights by Guildford Castle, then north of the village of Shere, north of Dorking, Reigate, Merstham, Chaldon, Godstone, Limpsfield and Westerham, through Otford, Kemsing and Wrotham, north of Trottiscliffe, towards Cuxton (where it crossed the River Medway). South of Rochester, the Pilgrims' Way travels through the villages of Burham, Boxley, Detling and continuing in a south-east direction to the north of the villages of Harrietsham and Lenham. The route continues south-east along the top of the Downs past Charing, to Wye and then turns north to follow the valley of the Great Stour through Chilham and on to Canterbury.
Along some stretches the pilgrims' route left the ancient trackway to encompass religious sites, examples being Pewley Down, near Guildford, where the later way passed St Martha's Hill and The Chantries, some 500 metres to the south.[2] At Reigate the thirteenth-century chapel of St Thomas and a hospice were built for the pilgrims' use, although they were not on the route.[20][21] Boxley Abbey, with its revered Rood of Grace, was another recognised detour.[22]
Walk[edit]
The North Downs Way National Trail parallels the old Pilgrims' Way between Farnham and Canterbury. Much of the traditional route of the Pilgrims' Way is now part of the modern road network and the Ramblers has previously advised walkers wishing to follow it to use St. Swithuns Way between Winchester and Farnham and the North Downs Way between Farnham and Canterbury as an alternative.[23]
The route also links with the South Downs Way at Winchester.
Notes[edit]
Jump up ^ All three usages are noted on Ordnance Survey maps
References[edit]
Jump up ^ Brayley, Edward (1850). A topographical history of Surrey. 4. London: G Willis. p. 218. OCLC 4601837.
^ Jump up to: a b c d e f Margary, Ivan D (1948). Roman Ways in the Weald. London: J M Dent. pp. 260–263. ISBN 0-460-07742-2.
Jump up ^ Fagg, C. C.; Hutchings, G. E. (1928). "Prehistory". In Ogilvie, Alan Grant. Great Britain: essays in regional geography. Tansley, A. G. Cambridge, England: Cambridge University Press. p. 29. OCLC 59447377.
^ Jump up to: a b Wright, Christopher John (1971). A Guide to the Pilgrims' Way. Constable and Co, London. ISBN 0-09-456240-7
Jump up ^ Encyclopædia Britannica (1998) Pilgrims' Way.
Jump up ^ Wooldridge, Sidney; Hutchings, Geoffrey (1957). London's Countryside : Geographical field work for students and teachers of geography. London: Methuen. p. 121. OCLC 788928682.
Jump up ^ Castleden, Rodney (1987). "The High Roads". The Stonehenge People: An Exploration of Life in Neolithic Britain, 4700-2000 BC. Routledge. p. 114. ISBN 0-7102-0968-1.
Jump up ^ Crawford, Osbert (1953). Archaeology in the Field. London: Phoenix House. p. 7. OCLC 30245154.
Jump up ^ Wright (1971: 16)
Jump up ^ Cartwright, Julia (1911). "1: The Pilgrims' Way". The Pilgrims' Way: From Winchester to Canterbury. London: John Murray. OCLC 559472322. .
Jump up ^ Hooper, Wilfrid (1936). "The Pilgrims' Way and its supposed pilgrim use". Surrey Archaeological Collections. Guildford: Surrey Archaeological Society. 44: 53. A Pipe Roll record for the hire of horses for the King's escort is extant.
Jump up ^ Finch, William Coles (1925). In Kentish pilgrim land, its ancient roads and shrines. London: Charles William Daniel. p. 77. OCLC 6213389.
Jump up ^ Hooper (1936) 44 "In their train have followed the host of guide-books and popular writers who have expanded and embellished ad libitum as fancy prompted".
Jump up ^ James, Edward Renouard (1871). Notes on the Pilgrims Way in West Surrey. London: Edward Stanford. p. 6. OCLC 560914994.
Jump up ^ Parker, Eric (1947). "The Pilgrims Way". Surrey. London: Hale. OCLC 4320463.
Jump up ^ Owen, Tim; Pilbeam, Elaine (1992). Ordnance Survey. Southampton, England: Ordnance Survey. p. 64. ISBN 0-319-00498-8.
Jump up ^ Elliston Erwood, F.C. (1927). "The "Pilgrim's Way" its antiquity and its alleged Mediæval Use". Archæologia Cantiana. 33: 2–3; 20.
Jump up ^ Ordnance Survey (1957). 172 Chatham & Madistone (Map). 1:63360. Chessington, England.
Jump up ^ Hauser, Kitty (2007). "From Pilgrims' Way to the railway". Shadow Sites: Photography, Archaeology, and the British Landscape, 1927-1955. Oxford, England: Oxford University Press. pp. 256–261. ISBN 0-19-920632-5.
Jump up ^ Wright (1971: 134)
Jump up ^ Malden, Henry Elliot, ed. (1902). A history of the County of Surrey. 3. London: Constable. pp. 229–245. OCLC 2979914.
Jump up ^ Cartwright 1911: "The Friary Aylesford"
Jump up ^ North Downs Way National Trail. Page archived (as at 2012-07-28) from the Ramblers' Association, accessed 2013-04-29
External links[edit]
A short history of the Pilgrims' Way, Countryside Agency
Pilgrims' Way Net - History and resource site for the Pilgrims' Way
Coordinates: 51°17′N 0°4′E / 51.283°N 0.067°E / 51.283; 0.067
Retrieved from "https://en.wikipedia.org/w/index.php?title=Pilgrims%27_Way&oldid=852085966"
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Kathleen Bradley
From Wikipedia, the free encyclopedia
Jump to: navigation, search
Kathleen Bradley
Bradley, 2007.
Born
Kathleen Joann Bradley
(1951-01-10) January 10, 1951 (age 66)
Girard, Ohio, U.S.
Other names
Kathleen Bradley–Overton
Spouse(s)
Bill Overton
(m. 1980; div. 1984)
Terrence Redd (m. 1988)[1]
Children
2
Modeling information
Height
5'9 (175 cm)
Hair color
Dark Brown
Eye color
Light Brown
Kathleen Joann Bradley (born January 10, 1951) is an American former model, actress and host. Bradley is primarily known as a "Barker's Beauty" on the CBS daytime game show The Price Is Right[2][3] from 1990 until 2000. Bradley is noted as the first permanent African-American model on the show.[4]
Contents
[hide]
1 Career
1.1 Departure from The Price Is Right
2 Personal
3 References
4 External links
Career[edit]
Born to Winifred Bradley in Girard, Ohio, Bradley was the only girl of four brothers. Bradley won the "Miss Black California" award in 1971. In 1979, Bradley was part of the short-lived disco group Destination, which had a hit single with a remake of Curtis Mayfield's "Move On Up." Bradley played the role of Mrs. Parker in the 1995 movie Friday.[5]
Departure from The Price Is Right[edit]
Bradley, along with longtime model Janice Pennington, was released from her modeling duties on The Price Is Right in October 2000, shortly after having testified during the lawsuit for slander and defamation of character host Bob Barker filed against model Holly Hallstrom. Barker lost his suit against Hallstrom and afterward fired Bradley, Pennington and other show staffers whose testimony contradicted Barker's. She accepted an undisclosed monetary settlement and did not pursue litigation.[6] In June 2014, Bradley released her memoirs, Backstage at The Price Is Right: Memoirs of a Barker Beauty.[5]
Personal[edit]
Bradley has been married twice. Her first marriage was to actor Bill Overton from 1980 to 1984.[7] Bradley has been married mechanical engineer Terrence Redd since 1988.[8] Bradley has two children; a daughter, Cheyenne Overton from her marriage with Overton[9], Terrence Redd II. Bradley's stepdaughter Dior is from Redd's marriage to actress Bern Nadette Stanis.[10]
References[edit]
Jump up ^ Ebony Magazine - Stepfamiles - September 1996
Jump up ^ JET Magazine - May 4, 1992
Jump up ^ JET Magazine - The Price Is Right! - August 19, 1996
Jump up ^ Atlanta Black Star - Showtime Series, 36-24-36 Reveals the Racism and Sexism The First Black TV Model of The Price Is Right Faced - October 29, 2015
^ Jump up to: a b Johnson, Ashley (June 11, 2014). "Kathleen Bradley visits Courier…talks about new book, career, Mrs. Parker". newpittsburghcourieronline.com. Retrieved July 8, 2014.
Jump up ^ Keck, William (December 12, 2000). "For Barker's Beauties, This Is Not a Game". latimes.com. Retrieved July 8, 2014.
Jump up ^ JET Magazine - Jayne Kennedy, Bill Overton: Newlyweds Talk About Love, Marriage, Baby And Careers - August 3, 1985
Jump up ^ Ebony Magazine - Stepmom - May 2000
Jump up ^ Ebony - 2000
Jump up ^ JET Magazine - Kathleen Bradley 'Price Is Right' Model Juggles Motherhood And TV Career - June 3, 1996
External links[edit]
Kathleen Bradley on IMDb

This biography article about a United States model is a stub. You can help Wikipedia by expanding it.
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Categories:
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American actresses
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African-American female singers
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