Epoch of Extreme Inundations

The Epoch of Extreme Inundations (EEI) is a hypothetical epoch during which four landforms in the Pontic–Caspian steppe—marine lowlands (marine transgressions), river valleys (outburst floods), marine transgressions (thermocarst lakes) and slopes (solifluction flows)—were widely inundated.[1] Catastrophic events during the epoch are theorized to have influenced prehistoric human life.

Research history

In 2002, Russian geographer Andrey L. Chepalyga of the Institute of Geography at the Russian Academy of Sciences formulated the theory[2][3] to explain natural events, with field investigation and laboratory work supporting the theory. Archaeological data indicated that the period impacted human life. During the first stage of research, sources were examined for extreme hydro-climatic events between 16000 and 18000 BCE in the Caspian drainage basin. Research focused on sources of water for these events, such as megafloods in river valleys and melting permafrost augmenting watersheds. The investigation's second stage included chronological correlation of the events using stratigraphy, geomorphology and radiocarbon dating. This was followed by paleohydrologic reconstruction of the basins, including their level, area, volume and water exchange between basins. Based on archeological data, the influence of the events on prehistoric human life was studied. The investigation aimed to comprehensively describe the period.

Time and place

During the deglaciation following the Last Glacial Maximum, northwestern Eurasia experienced widespread flooding from the Atlantic Ocean to the Yenisei River, including the subarctic and Himalayas: over 10,000,000 square kilometres (3,900,000 sq mi). Flooding occurred in four landforms: marine lowlands, river valleys, watersheds and slopes, and peaked 17,000 to 15,000 years ago.

Geology

The basins' bottom and littoral sediments and their fossils contain geological evidence of the EEI. In the Caspian basin, bottom sediments attributable to the epoch differ from the under- and overlying layers in a number of ways[4][5][6] and are called "chocolate clays" because of their reddish-brown color. The chocolate clays and related Khvalynean sediments are usually 3–5 metres (9.8–16.4 ft), occasionally exceeding 20–25 metres (66–82 ft). They are primarily limited to the Caspian Depression, from the modern Caspian coast to the foothills of the surrounding mountains.

Stratigraphy

In the marine sequence of the Caspian basin, the Khvalynean layers are above the Late Khazarian ones (which date to the last interglacial period) and below the New Caspian (Holocene) deposits. They are separated from the Lower Khazarian series by continental Atelian layers synchronous to marine sediments from the Atelian basin. The level of the latter was 110–120 metres (360–390 ft) below the present Caspian level—in other words, 140–150 metres (460–490 ft) below sea level.[7][8] In the Caspian Depression, the Khvalynean sediments occur primarily near the surface; younger still (and higher in the sequence) are the Holocene floodplain lacustrine and marine (New Caspian) sediments.

EEI deposits in the Black Sea basin occur in the New Euxinian series. On the continental slope and in the deep-sea basin, they are a light reddish-brown and a pale yellow mud .5–1 metre (20–39 in) thick.[9] In color they resemble the chocolate clays of the Caspian basin, and their age is near that of the latter (15,000 BP).

Fossils

Indicators of an EEI are brackish-water mollusk species close to modern North Caspian ones. Among these are Caspian endemic species of the Limnocardiidae family, such as the Didacna Eichwald genus.[10] Although the latter is not presently found outside the Caspian Sea, it occurred widely in the Azov—Black Sea basin during the Pleistocene until the Karangatian era.

Gastropods are represented by the Caspian endemic genera Caspia and Micromelania. Shells of the Early Khvalynean complex are distinguished by their small size (two to three times smaller than present ones) and thin walls. The complex is usually considered as a product of cold climate and low salinity. New Black Sea sediments contain mollusks of the Caspian type.[11]

Eurasian basins

Marine basins and spillways

Marine transgressions in the Black and Caspian Sea basins formed a number of sea-lakes (the Aral, Caspian and Black Seas and the Sea of Marmara) connected by spillways:[12] the Uzboy River, the Kuma–Manych Depression, the Bosphorus and the Dardanelles. The large basin covered about 1,500,000 square kilometres (580,000 sq mi) and held up to 700,000 km3 of water and 5000 km3 (10 billion tons) of salt. Discharging more than 60,000 m3 per second, it ran 3,000 km west to east (from the Mediterranean to Central Asia) and 2,500 km (from 57 to 35°N) north to south. Its drainage basin covered more than three million km3.

The Eurasian cascade system of seas and lakes is unparalleled in water area. The largest intra-continental lake system of today (the Great Lakes of North America) is six times smaller (245,000 km2), with a water volume 30 times smaller (22,700 km3), a discharge four times smaller (14,000 m3/s) and a drainage basin three times smaller.

The peak inundation apparently centered on the Khvalynean basin (the recent Caspian Sea). Its level rose and its area increased six times, to one million square kilometers. Its water volume doubled (to 130,000 km3), with a salinity of 10-12‰. Its waters overflowed the Caspian depression down the Manych-Kerch spillway.[13][14][15]

Sources of water

Additional water sources would have been necessary for the EEI. To fill the Caspian basin to a level of more than 50 metres (160 ft) would require as much as 70,000 km3 of water, equivalent to 200 years of river discharge into the Caspian Sea. Water flowed through the Manych Spillway (250 to 1,000 km3 per year) and some (more than 100 km3 per year) was lost through evaporation. Water may have come from:

Outburst floods have been inferred from studies of macromeanders in river valleys.[16][17] Macromeanders dated to the EEI exceed modern ones in size. Their width tends to increase from north to south; they are similar to modern meanders on the tundra, two to three times wider at the tree line, three to five times wider in the taiga, five to eight times wider in the mixed-forest zone, 10 times wider in the broadleaf zone and 13 times in the forest steppe and the steppe.[18]

Catastrophe

The rate of water-level rise during the EEI may be inferred from the duration of the epoch, estimated at five to six hundred years. Assuming an equal length of the phases of rising, high water and subsiding (150 to 200 years each), the sea level would rise by 180–190 metres (590–620 ft) at a rate of at least one meter per year.

The Caspian Sea has risen 2.5 metres (8 ft 2 in) since 1978, as much as 10 centimetres (3.9 in) per year, with an adverse impact on human activity. The Khvalynean transgression was more catastrophic, especially the rate of coastline shift in the plains of the North Caspian region. The coastline moved from the Atelian coast (near the Mangyshlak sill) 1,000 kilometres (620 mi) north, 5 to 10 kilometres (3.1 to 6.2 mi) a year. Even greater was the northward migration of the mouth of the Volga River, which moved more than 2,000 kilometres (1,200 mi) upstream in 150 to 200 years—more than 10 kilometres (6.2 mi) annually, or about 30 metres (98 ft) per day.

Influence on humans

Floodplains and natural spillways influenced human migration. P. M. Dolukhanov of the School of Historical Studies at Newcastle University has concluded that the Caspian-Black Sea spillway across the Kumo-Manych valley isolated the Caucasus and Central Asia. The spread of Upper Paleolithic technology in the region became possible only after the crest of the Upper Khvalynian transgression from 12,500 to 12,000 BP.[19][20] At Kamennaya Balka,[21][22] an Upper Paleolithic site in Russia, of three layers the lower and upper ones contain small stone tools of Near Eastern origin.[23] This indicates cultural connections in the southern regions (the Caucasus and Iraq). The middle layer indicates an indigenous Kamennaya Balka culture, without small stone tools. Its age (17,000 to 15,000 BP) coincides with Manych-Kerch spillway activity, which may have been a barrier to cultural connections with the Near East.[24] The EEI affected human activity; there is no archaeological evidence that it destroyed civilizations, although A. L. Chepalyga suggests that it may have been the basis for flood myths.[25][26][27][28]

See also

References

  1. ↑ The dynamics of landscape components and inner marine basins of Northern Eurasia over the past 130,000 years. Edited by A.A. Svitoch. GEOS. Moscow. Russia. 2002. ISBN 5-89118-268-8
  2. ↑ Chepalyga A.L., H. Arslanov, T. Yanina. Detailed age control of Khvalynean basin history. Collection papers of Intern. geosciens programme conference, project 521 "Black Sea -Mediterranean corridor" Izmir 2009 p.p. 71-75
  3. ↑ Chepalyga A.L. Epoch of Extremal Floodings and human adaptation in the North Black Sea basin. Second Plenary Meeting and Field Trip of Project IGCP 521 "Black Sea-Mediterranean Corridor during last 30 ky: Sea level change and human adaptation", Odessa, Ukraine, August 20-28, 2006
  4. ↑ Badyukova E.N. (2000). Genesis of the Khvalynian (Pleistocene) chocolate clays of Northern Caspian region. Buil. Moscow Soc. Naturalists. Sect. geol. V.75, 5. pp. 25–31
  5. ↑ Chistyakova I.A. (2001) Material composition of the early Khvalynian sediments. Buil. Com. Quat Res. 64. pp. 61–69. (In Russian)
  6. ↑ Leontyev O.K., Maev E.G., Rychagov G.I. 1977. Geomorphology of coasts and floor of the Caspian Sea. . Moscow: Moscow University Press. (In Russian
  7. ↑ Lokhin M.Yu., Maev E.G. (1990) The late Pleistocene deltas on the northern shelf of the Northern Caspian Sea. Vestnik MGU, Ser. Geogr. 3, 34–40. (In Russian)
  8. ↑ Maev E.G. (1994) Caspian regressions: their place in the Quaternary history of the Caspian Sea and impact on the sea floor relief formation. Geomorphologiya. 2, 94–101. (In Russian)
  9. ↑ Ryan W.B.F., Pitman W.C.I., Major C.O., Shimkus K., Moskalenko V., et al. 1997. An abrupt drowning of the Black Sea shelf. Mar. Geol. 138: 119–26
  10. ↑ Nevesskaya L.A. (1965) Late Quaternary bivalve mollusks of the Black Sea: their systematics and ecology. Acad. nauk SSSR Paleont. Inst. Trudy 105: 1–390 (In Russian)
  11. ↑ Algan O., Cagatay N., Tchepalyga A., Ongan D., Eastoe C., Gokasan E. (2001) Stratigraphy of the sediment fill in Bosphorus Strait: water exchange between the Black and Mediterranean Seas during the last glacial – Holocene. Geo.-Mar.Lett. 20:209-18
  12. ↑ Popov G.I. Pleistocene of the Black Sea–Caspian straits. Moscow: Nauka Press. 215 pp. 1983.
  13. ↑ Paleohydrological Reconstruction of Manych-Kerch Spillway, archived from the original on 5 April 2011, retrieved 27 January 2016
  14. ↑ Chepalyga A.L., Pirogov A.N. Extreme sedimentation in the Manych valley during Khvalynean transgression. Proceedings of the tenth international symposium on river sedimentation. August 1–4,. 2007. MSU. Moscow
  15. ↑ Pirogov A.N. Paleogeographic reconstruction of the Manych-Kerch spillway. In: Geology and geochemistry. MPSU. Moscow. 2004. pp. 34-35
  16. ↑ Sidorchuk A., Borisova O., Panin A. (2001) Fluvial response to the Late Valdai/Holocene environmental change on the East European Plain. Global and Planetary Change, 28: 303–318
  17. ↑ Sidorchuk A., Panin A., Borisova O., Kovalyukh N. (2001b). Lateglacial and Holocene palaeohydrology of the lower Vychegda river, western Russia. In: River basin sediment systems: Archives of environmental change. D.Maddy, M.G.Macklin & J.C.Woodward, eds. A.A.Balkema Publishers. Pp. 265–295
  18. ↑ Sidorchuk A., Panin A., Borisova O. 2003. The Lateglacial and Holocene palaeohydrology of Northern Eurasia. In: Palaeohydrology: Understanding Global Change. K.J.Gegory and G. Benito, eds. John Wiley & Sons, Ltd. pp. 61-75
  19. ↑ P.M. Dolukhanov at all. Late Quaternary Caspian: Sea-Levels, Environments and Human Settlement. The open geography journal. 2. 2009. pp.1-15
  20. ↑ Arslanov KA, Dolukhanov PM, Gei NA. Climate, Black Sea levels and human settlements in Caucasus Littoral 50,000 - 9,000 BP. Quaternary International 2007; 167-168: 121-7.
  21. ↑ Leonova N. The Caucasus and Russian Plain in the Late Pleistocene (cultural contacts and migrations) // Annual meeting Society American Archaeologists, Seattle, 2002.
  22. ↑ Leonova N.B, Minkov E.V. Spatial Analysis of Faunal Remains from Kamennaya Balka II.
  23. ↑ N.B. Leonova, S.A. Nesmeyanov, E.A. Vinogradova, O.A. Voeikova, M.D. Gvozdover, E. V. Min'kov, E.A. Spiridonova, S.A. Sycheva. The Paleoecology Of The Plains Paleolithic (The Kamennaja Balka Upper Paleolithic Sites North Of Sea Of Azov).Institute of Environment Geoscience RAS. Moscow. 2006.
  24. ↑ A.L. Chepalyga, T.A. Sadchikova, A.N. Pirogov. Influence of the Late Glacial Eurasian Water Flow on the Black Sea-Mediterranear Corridor (BSMS). In: UNESCO-IGCP-IUGC 1st Plenary meeting and field trip of project IGCP – 521 Black Sea-Mediterranean corridor during the last 30 ky: sea level change and human adaptation (2005-2009), 8-15 October 2005, Istanbul.
  25. ↑ Chepalyga A.L. The late glacial Great Flood in the Ponto-Caspian basin. In: The Black Sea Flood question: changes in coastline, climate and human settlement. Springer. 2006. pp.119-148
  26. ↑ Chepalyga A.L. Vsemirnyj potop kak real'noe paleogidrologicheskoe sobytie. (Всемирный потоп как реальное палеогидрологическое событие) Jekstremal'nye gidrologicheskie situacii (Экстремальные гидрологические ситуации). Moscow, Media-PRESS, 2010. Pp. 180-214
  27. ↑ http://paleogeo.org/flood_en.html
  28. ↑ Late glacial great flood in the Black Sea and Caspian Sea (abstract) 2003-11-04. Conference: The Geological Society of America 2003 Seattle Annual Meeting, Seattle, Washington, Abstracts with Programs, v.35-6, p.460

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