The African humid period (AHP; also known by other names) is a climate period in Africa during the late Pleistocene and Holocene geologic epochs, when northern Africa was wetter than today. The covering of much of the Sahara desert by grasses, trees and lakes was caused by changes in the Earth's axial tilt; changes in vegetation and dust in the Sahara which strengthened the African monsoon; and increased greenhouse gases. During the preceding Last Glacial Maximum, the Sahara contained extensive dune fields and was mostly uninhabited. It was much larger than today, and its lakes and rivers such as Lake Victoria and the White Nile were either dry or at low levels. The humid period began about 14,600–14,500 years ago at the end of Heinrich event 1, simultaneously to the Bølling–Allerød warming. Rivers and lakes such as Lake Chad formed or expanded, glaciers grew on Mount Kilimanjaro and the Sahara retreated. Two major dry fluctuations occurred; during the Younger Dryas and the short 8.2 kiloyear event. The African humid period ended 6,000–5,000 years ago during the Piora Oscillation cold period. While some evidence points to an end 5,500 years ago, in the Sahel, Arabia and East Africa, the end of the period appears to have taken place in several steps, such as the 4.2-kiloyear event.

The AHP led to a widespread settlement of the Sahara and the Arabian Deserts, and had a profound effect on African cultures, such as the birth of the Ancient Egyptian civilization. People in the Sahara lived as hunter-gatherers and domesticated cattle, goats and sheep. They left archaeological sites and artifacts such as one of the oldest ships in the world, and rock paintings such as those in the Cave of Swimmers and in the Acacus Mountains. Earlier humid periods in Africa were postulated after the discovery of these rock paintings in now-inhospitable parts of the Sahara. When the period ended, humans gradually abandoned the desert in favour of regions with more secure water supplies, such as the Nile Valley and Mesopotamia, where they gave rise to early complex societies.

Research history

Herodotus in 440 BC and Strabo in 23 AD discussed the existence of a greener Sahara, although their reports were at first questioned owing to their anecdotal nature. In 1850 the researcher Heinrich Barth discussed the possibility of past climate change leading to increased wetness in the Sahara after discovering petroglyphs in the Murzuq Desert, and further discoveries of petroglyphs led desert explorer László Almásy to coin the concept of a Green Sahara in the 1930s. Later in the 20th century, conclusive evidence of a past greener Sahara, the existence of lakes^[1][2] and higher Nile flow levels was increasingly reported^[3] and it was recognized that the Holocene featured a humid period in the Sahara.^[4]

The idea that changes in Earth's orbit around the Sun influence the strength of the monsoons was already advanced in 1921, and while the original description was partly inaccurate, later widespread evidence for such orbital controls on climate was found.^[1] At first it was believed that humid periods in Africa correlate with glacial stages ("pluvial hypothesis") before radiocarbon dating became widespread.^[5]

The development and existence of the African humid period has been investigated with archaeology, climate modelling and paleoproxies,^[6] with archaeological sites,^[7] dunes and deposits left by lakes, aeolian deposits and leaf wax in the sea and wetlands playing an important role.^[2][8] Pollen, lake deposits and former levels of lakes have been used to study the ecosystems of the African humid period,^[9] and charcoal and leaf impressions have been used to identify vegetation changes.^[10] Questions in AHP research are its beginning, cause, intensity, end, land feedbacks and fluctuations during the AHP.^[11] The time 6,000 years ago has received particular attention, especially since that period of the AHP has been used as an experiment in the Paleoclimate Modelling Intercomparison Project.^[12] Most recently, the effects of the Sahara greening on other continents has drawn scientific attention.^[13] The concept of a Sahara significant different than today, and the rich record it left, has driven the imagination of the public and scientists alike.^[11]

Research issues

While the precipitation changes since the last glacial cycle are well established, the magnitude and timing of the changes are unclear.^[14] Depending on how and where measurements and reconstructions are made, different beginning dates, ending dates, durations^[3] and precipitation levels^[15] have been determined for the African humid period.^[3] The amounts of precipitation reconstructed from paleoclimate records and simulated by climate modelling are often inconsistent with each other;^[16] in general, the simulation of the Green Sahara is considered a problem for earth system models.^[17] There is more evidence of the late phase of the AHP than its beginning.^[18] Erosion of lake sediments and carbon reservoir effects make it difficult to date when they dried up.^[19] Vegetation changes by themselves do not necessarily indicate precipitation changes, as changes in seasonality, plant species composition and changes in land use also play a role in vegetation changes.^[20] Isotope ratios such as the hydrogen/deuterium ratio that have been used to reconstruct past precipitation values likewise are under the influence of various physical effects, which complicates their interpretation.^[21] Most records of Holocene precipitation in eastern Africa come from low altitudes.^[22]

Terminology

The term "African humid period" was coined in 2000 by deMenocal et al.^[23] Earlier humid periods are sometimes known as "African humid periods"^[24] and a number of dry/wet periods have been defined for the Central Africa region.^[25] In general, these types of climate fluctuations between wetter and drier periods are known as "pluvials" and "interpluvials", respectively.^[26] Because the AHP did not affect all of Africa, there have been calls to not use the term^[27] also because it has supposedly colonial implications,^[28] and some researchers have specified "North African humid period" and "Northern African humid period".^[29]

Other terms that have been applied to the Holocene AHP or correlative climate phases are "Holocene humid period", which also covers an analogous episode in Arabia and Asia;^[30][31] "early to mid-Holocene humid episode";^[32] "Holocene Pluvial";^[33] "Holocene Wet Phase";^[34] "Kibangien A" in Central Africa;^[35] "Makalian" for the Neolithic period of northern Sudan;^[36] "Nabtian Pluvial",^[37] "Nabtian Wet Phase"^[38] or "Nabtian period" for the 14,000–6,000 humid period over the Eastern Mediterranean and Levant;^[39] "Neolithic pluvial";^[40] "Neolithic Subpluvial";^[34] "Neolithic wet phase";^[41] "Nouakchottien" of the Western Sahara 6,500 – 4,000 years before present;^[42] "Subpluvial II"^[41] and "Tchadien" in the Central Sahara 14,000 – 7,500 years before present.^[42] The terms "Big Dry",^[43] "Léopoldvillien"^[44] and Ogolien [fr] have been applied to the dry period in the last glacial maximum,^[45] the latter is equivalent to the "Kanemian";^[46] "Kanemian dry period" refers to a dry period between 20,000 and 13,000 years before present in the Lake Chad area.^[47]

Background and beginning

The African humid period took place in the late Pleistocene^[48] and early-middle Holocene,^[49] and saw increased precipitation in Northern and Western Africa due to a northward migration of the tropical rainbelt.^[20][50] The AHP is the most profound climate change of the low latitudes during the last 100,000 years^[51] and stands out within the otherwise relatively climatically stable Holocene.^[52] It is part of the so-called Holocene climatic optimum^[53] and coincides with a global warm phase, the Holocene Thermal Maximum.^[54][a] Liu et al. 2017^[57] subdivided the humid period into an "AHP I" which lasted until 8,000 years ago, and an "AHP II" from 8,000 years onward,^[58] with the former being wetter than the latter.^[59]

The African humid period was not the first such phase; evidence for about 230 older such "green Sahara"/wet periods exist going back perhaps to the first appearance of the Sahara 7–8 million years ago,^[1] for example during Marine Isotope Stage 5 a and c.^[60] Earlier humid periods appear to have been more intense than the AHP of the Holocene,^[61][62] including the exceptionally intense Eemian humid period. This humid period provided the pathways for early humans to cross Arabia and Northern Africa^[63] and which, together with later moist periods, has been linked to expansions of the Aterian populations^[64] and the speciation of insect species.^[65] Such humid periods are usually associated with interglacials, while glacial stages correlate to dry periods;^[24] they occur during precession minima, unless large ice sheets or insufficient greenhouse gas concentrations suppress their onset.^[66]

The Bølling–Allerød warming appears to be synchronous with the onset of the African humid period^[67][68][69] as well as to increased humidity in Arabia.^[70] Later, in the Blytt–Sernander sequence the humid period coincides with the Atlantic period.^[71]

Conditions before the African humid period

During the Last Glacial Maximum, the Sahara and Sahel had been extremely dry^[72] with less precipitation than today^[73][74] as reflected by the extent of dune sheets and water levels in closed lakes.^[72] The Sahara was much larger,^[75] extending 500–800 kilometres (310–500 mi) farther south^[76] to about 12° northern latitude.^[77] Dunes were active much closer to the equator,^[76][78][b] and rainforests had retreated in favour of afromontane and savannah landscapes as temperatures, rainfall, and humidity decreased.^[44][81][82]

There is little and often equivocal evidence of human activity in the Sahara or Arabia at that time, reflecting its drier nature;^[83][84][85] in the Acacus Mountains the last human presence was recorded 70,000-61,000 years ago and by the LGM humans had largely retreated to the Mediterranean coast and the Nile Valley.^[86] The aridity during the Last Glacial Maximum appears to have been the consequence of the colder climate and larger polar ice sheets, which squeezed the monsoon belt to the equator and weakened the West African Monsoon. The atmospheric water cycle and the Walker and Hadley circulations were weaker as well.^[87] Exceptional dry phases are linked to Heinrich events^[88] when there are a large number of icebergs in the North Atlantic;^[89] the discharge of large amounts of such icebergs between 11,500 and 21,000 years before present coincided with droughts in the subtropics.^[90]

Before the onset of the AHP, it is thought that Lake Victoria, Lake Albert, Lake Edward,^[91] Lake Turkana^[92] and the Sudd swamps had dried out.^[93] The White Nile had become a seasonal river^[93] whose course^[94] along with that of the main Nile may have been dammed by dunes.^[95] The Nile Delta was partially dry, with sandy plains extending between ephemeral channels and exposed seafloor, and it became a source of sand for ergs^[c] farther east.^[97] Other lakes across Africa, such as Lake Chad and Lake Tanganyika, also had shrunk^[d] during this time,^[98] and both the Niger River and Senegal River were stunted.^[99]

Early humidity increases

Whether some parts of the desert such as highlands like the Red Sea Hills were reached by the westerlies^[100] or weather systems associated with the subtropical jet stream^[101]—and thus received precipitation—is contentious. It is only clearly supported for the Maghreb in northwestern Africa,^[100] though river flow^[78]/terrace formation^[102] and lake development in the Tibesti and Jebel Marra mountains^[103][104] and residual Nile flow may be explained in this way.^[105] The highlands of Africa appear to have been less affected by drought during the last glacial maximum.^[106]

The end of the glacial drought occurred between 17,000 and 11,000 years ago,^[104] with an earlier beginning noted in the Acacus^[18] and Saharan mountains^[107][81] 26,500 - 22,500^[18] and (possibly) 18,500 years ago, respectively.^[108] In southern and central Africa earlier starts 17,000 and 17,500 years ago, respectively, may be linked to Antarctic warming,^[109][35] while Lake Malawi appears to have been low until about 10,000 years ago.^[110]

High lake levels occurred in the Jebel Marra and Tibesti Mountains between 15,000 and 14,000 years ago^[111] and the youngest stage of glaciation in the High Atlas mountains took place at the same time as the Younger Dryas and early African humid period.^[112] Around 14,500 years ago, lakes started to appear in the arid areas.^[113]

Onset

The humid period began about 15,000^[109][114]-14,500 years ago.^[e][48] The onset of the humid period took place almost simultaneously over all of Northern^[f] and Tropical Africa,^[118] with impacts as far as Santo Antão on Cape Verde.^[119][120] In Arabia, wet conditions apparently took about two millennia to advance northward,^[117][121] a gradual advance is supported by tephrochronological data.^[122] Likewise, in the Sahara there might have been a delay of about a millennium between the onset of the AHP and the full establishment of humid conditions, as vegetation growth and the filling of river systems took time.^[123]

Lake Victoria reappeared and overflowed;^[113] Lake Albert also overflowed into the White Nile^[111] 15,000–14,500 years ago^[91] and so did Lake Tana, into the Blue Nile.^[111] The White Nile flooded part of its valley^[124] and reconnected to the main Nile.^[114][g] In Egypt widespread flooding by the "Wild Nile" took place;^[111] this "Wild Nile" period^[126] led to the largest recorded floods on this river,^[95] sedimentation in floodplains,^[127] and probably also impacted human populations along the river.^[128] Even earlier, 17,000–16,800 years ago, meltwater from glaciers in Ethiopia – which were retreating at that time – may have begun to increase the flow of water and sediment in the Nile.^[129] In the East African Rift water levels in lakes began to rise by about 15,500/15,000^[130]-12,000 years ago;^[131] Lake Kivu began overflowing into Lake Tanganyika by about 10,500 years ago.^[132]

About the same time that the AHP started, the cold glacial climate in Europe associated with Heinrich event 1 ended^[113] with climate changing as far as Australasia.^[111] A warming and retreat of sea ice around Antarctica coincides with the start of the African humid period,^[133] although the Antarctic Cold Reversal also falls into this time^[35] and may relate to a drought interval recorded in the Gulf of Guinea.^[134]

Causes

The African humid period was caused by a stronger West African Monsoon^[135] directed by changes in solar irradiance and in albedo feedbacks.^[16] These led to increased moisture import from both the equatorial Atlantic into West Africa, as well as from the North Atlantic and the Mediterranean Sea towards the Mediterranean coasts of Africa.^[136][137] There were complex interactions with the atmospheric circulation of the extratropics and between moisture coming from the Atlantic Ocean and the Indian Ocean,^[138] and an increased overlap between the areas wetted by the monsoon and those wetted by extratropical cyclones.^[139]

Climate models indicate that changes from a dry to a green Sahara and back have threshold behaviour, with the change occurring once a certain level of insolation is exceeded;^[140] likewise, a gradual drop of insolation often leads to a sudden transition back to a dry Sahara.^[141] This is due to various feedback processes which are at work,^[20] and in climate models there is often more than one stable climate-vegetation state.^[142] Sea surface temperature and greenhouse gas changes synchronized the beginning of the AHP across Africa.^[118]

Orbital changes

The African humid period has been explained by increased insolation during Northern Hemisphere summer.^[20] Due to precession, the season at which Earth passes closest to the Sun on its elliptical orbit – the perihelion – changes, with maximum summer insolation occurring when this happens during Northern Hemisphere summer.^[143] Between 11,000 and 10,000 years ago, Earth passed through the perihelion at the time of summer solstice, increasing the amount of solar radiation by about 8%,^[48] resulting in the African monsoon becoming both stronger and reaching farther north.^[144] Between 15,000 and 5,000 years ago, summer insolation was at least 4% higher than today.^[51] The obliquity also decreased during the Holocene^[145] but the effect of obliquity changes on the climate is focused on the high latitudes and its influence on the monsoon is unclear.^[146]

During summer, solar heating is stronger over the North African land than over the ocean, forming a low pressure area that draws moist air and precipitation in^[48] from the Atlantic Ocean.^[147] This effect was strengthened by the increased summer insolation,^[148] leading to a stronger monsoon that also reached farther north.^[145] The effects of these circulation changes reached as far as the subtropics.^[19]

Obliquity and precession are responsible for two of the foremost Milankovich cycles and are responsible not only for the onset and cessation of ice ages^[149] but also for monsoon strength variations.^[146] Southern Hemisphere monsoons are expected to have the opposite response of Northern Hemisphere monsoons to precession, as the insolation changes are reversed; this observation is borne out by data from South America.^[150] The precession change increased seasonality in the Northern Hemisphere while decreasing it in the Southern Hemisphere.^[145]

Albedo feedbacks

According to climate modelling,^[1] orbital changes by themselves cannot increase precipitation over Africa enough to explain the formation of the large desert lakes such as 330,000 square kilometres (130,000 sq mi) Lake Megachad^[h][19] or the northward expansion of vegetation^{[154][155][145]} unless ocean and land surface changes are factored in.^[20]

Decreasing albedo resulting from vegetation changes is an important factor in the precipitation increase.^[19] Specifically, increased precipitation increases the amount of vegetation; vegetation absorbs more sunlight and thus more energy is available for the monsoon. In addition, evapotranspiration from vegetation adds more moisture, although this effect is less pronounced than the albedo effect.^[72] Heat fluxes in the soil and evaporation are also altered by the vegetation.^[156]

Reduced dust generation from a wetter Sahara,^[157] where major dust-generating regions were submerged by lakes, influences the climate^[158] by reducing the amount of light absorbed by dust. Decreased dust emissions also modify cloud properties, making them less reflective and more efficient at inducing precipitation.^{[1][159][160]} In climate models, reduced amounts of dust in the troposphere together with vegetation changes can^[161][162] often but not always explain the northward expansion of the monsoon.^[163][164] There is not universal agreement on the effects of dust on precipitation in the Sahel, however,^[1] in part because the effects of dust on precipitation may be dependent on its size.^[165]

In addition to raw precipitation changes, changes in precipitation seasonality such as the length of dry seasons need to be considered when assessing the effects of climate change on vegetation,^[166] as well as the fertilizing effects of increased carbon dioxide concentrations in the atmosphere.^[156]

Other sources of albedo changes:

• Changes in soil properties result in changes in the monsoon; replacing desert soils with loamy ones results in increased precipitation,^[167] and soils that are wet^[156] or contain organic matter reflect less sunlight and accelerate the moistening process.^[1] Desert sand changes also modify the albedo.^[156]
• Albedo changes caused by lakes and wetlands^[16] can alter precipitation in climate models.^[167]

Intertropical Convergence Zone changes

Warmer extratropics during summer may have drawn the Intertropical Convergence Zone (ITCZ) northward^[161] by about five or seven degrees latitude,^[168] resulting in precipitation changes.^[169] Sea surface temperatures off North Africa warmed under orbital effects and through weaker trade winds, leading to a northward movement of the ITCZ and increasing moisture gradients between land and sea.^[72] Two temperature gradients, one between a cooler Atlantic during spring and an already warming African continent, the other between warmer temperatures north of 10° latitude and cooler south, may have assisted in this change.^[170] In Eastern Africa, ITCZ changes had relatively little effect on precipitation changes.^[171][172] The past position of the ITCZ in Arabia is also contentious.^[173]

Precipitation changes in East Africa

The African humid period that took place in East Africa appears to have been caused by different mechanisms.^[174] Among the proposed mechanisms are decreased seasonality of precipitation^[175] due to increased dry season precipitation,^[176] shortening of the dry season, increased precipitation^[177] and increased inflow of moisture from the Atlantic and Indian Oceans. The Atlantic moisture inflow was in part triggered by a stronger West African and Indian monsoon, perhaps explaining why the effects of the AHP extended into the Southern Hemisphere.^[171][178] The behaviour of the easterly trade winds is unclear; increased moisture transport by easterly trade winds may have aided in the development of the AHP^[135] but alternatively a stronger Indian Monsoon that draws easterly winds away from East Africa may have occurred.^[179]

Changes in the Congo Air Boundary^[i][180] or increased convergence along this boundary may have contributed;^[177][180] the Congo Air Boundary would have been shifted east by the stronger westerly winds^[178] directed by lower atmospheric pressure over Northern Africa,^[181] allowing additional moisture from the Atlantic to reach East Africa.^[182] The parts of East Africa that were isolated from Atlantic moisture did not become significantly wetter during the AHP^[115] although at one site in Somalia the seasonality of precipitation may^[183] or may not have decreased.^[184]

Various contributing factors may have led to the increased humidity in East Africa, not all of which were necessarily operating simultaneously during the AHP.^[185][186] That the "African humid period" reached this part of Africa has been doubted.^[187] Finally, increased greenhouse gas concentrations may have been involved in directing the onset of the AHP in tropical southeastern Africa;^[188] there, orbital changes would be expected to lead to climate variations opposite to those in the Northern Hemisphere.^[189] The pattern of humidity changes in south-eastern Africa are complex.^[190]

Additional factors

• Climate change in the far northern latitudes may have contributed to the onset of the AHP.^[135] The shrinkage of the Scandinavian and the Laurentide Ice Sheets occurred at its beginning,^[156] and in climate models, a retreat of the ice sheets is often required to simulate the humid period^[191] although their size has little influence on its intensity.^[192] Their existence might also explain why the AHP did not start immediately with the early insolation peak, as still existing ice sheets would have cooled the climate.^[193][194]
• Sea surface temperature changes in the Atlantic influence the African monsoon^[135] and may have influenced the onset of the AHP. Weaker trade winds and higher insolation would lead to warmer sea surface temperatures, increasing precipitation by increasing moisture gradients between land and sea.^[72] Changes in the Atlantic meridional overturning circulation (AMOC)^[164] and North Atlantic temperature gradients were also involved.^[147]
• Warming of the Mediterranean Sea increases the amount of Sahel precipitation; this effect is responsible for the recent anthropogenic global warming mediated increase in Sahel precipitation.^[1] Warmer sea surface temperatures there might also explain the increased precipitation recorded in the Mediterranean^[173] and increased intensity of precipitation reconstructed from former rivers in the Sahara during the AHP.^[195]
• Increased precipitation during winter is correlated with a larger spatial extent of Mediterranean precipitation and might have aided in the establishment of the AHP, especially in North Africa^{[196][197][198]} including Algeria,^[199] Morocco^[200] and Northern Egypt,^[201] around the northern Red Sea,^[202][136] in the Tibesti^[203][204] and in northern Arabia^[173] and generally at higher latitudes where the monsoon did not arrive.^[170] This precipitation may have extended to other parts of the Sahara; such would have led to the areas of summer and winter precipitation overlapping^[205][206] and the dry area between the monsoonal and westerlies-influenced climate zones becoming wetter or disappearing altogether.^[207] Such changes in Mediterranean-derived precipitation may correlate with changes in the North Atlantic and Arctic Oscillations^[196] and with the increased contrast between warm summers and cold winters.^[199]
• Trough-mediated northward transport of moisture during autumn and spring has also been proposed to explain the increased precipitation and its underestimation by climate models.^[16] In one climate model, increased northward moisture transport by such troughs increases autumn rainfall in the Sahara, especially in the mid-Holocene and when the climate is already moister than usual there.^[208]
• Weaker subtropical anticyclones were proposed as an explanation during the 1970s–1980s.^[209]
• In montane regions such as the Meidob volcanic field cold temperatures after the last glacial maximum may have reduced evaporation and thus allowed an early onset of humidity.^[210]
• Changes in the Earth's geomagnetic field may be linked to the humidity changes.^[211]
• Increased moisture supply from dispersed lakes^[212] and larger lakes like Lake Megachad may have increased the precipitation, although this effect is probably not adequate to explain the entire AHP^[213] and model-dependent.^[214] A similar role has been attributed to the extensive wetlands, drainages and lakes in the Eastern Sahara^[215] and to the ecosystem in general.^[216]
• Two high elevation winds, the African Easterly Jet and the Tropical Easterly Jet modulate atmospheric air flows over Africa and thus also the amount of precipitation; the Tropical Easterly Jet comes from India and is powered by temperature gradients between the tropics^[73] and the subtropics while the African Easterly Jet is powered by temperature gradients in the Sahel.^[217] A stronger West African Monsoon resulted in a weaker African Easterly Jet and thus decreased transport of moisture out of Africa.^[178]
• Increased atmospheric carbon dioxide concentrations may have played a role in triggering the AHP,^[156] especially its extension across the equator,^[218] as well as its resumption after the Younger Dryas and Heinrich event 1 through increased sea surface temperatures.^[219] Carbon dioxide concentrations have a strong influence on the intensity of orbital changes needed to start an AHP^[220] but do not play a major role in controlling its intensity.^[192]
• In some parts of the Sahara increased water supply from montane regions may have assisted in the development of moist conditions.^[221][222]
• Larger forests in Eurasia may have led to a northward shift of the ITCZ.^[223]
• Along the coast of Senegal, sea level rise helped the establishment of the AHP vegetation.^[224]
• Other proposed mechanisms involve convection occurring above the atmospheric boundary layer,^[225] increased latent heat fluxes,^[159] changes in tropical wave activity over Africa,^[226] low pressure in northwestern Africa drawing moisture into the Sahara,^[227] changes in the solar cycles^[228] and complex atmospheric flow phenomena.^[229]

Effects

The African humid period extended over most of Africa:^[11] The Sahara and eastern,^[57] southeastern and equatorial Africa. In general, forests and woodlands expanded through the continent.^[230] A similar wet episode took place in the tropical Americas,^[j] China, Asia,^{[k][232][233][50][72][234][235]} India,^[236] the Makran region,^[237] the Middle East and the Arabian Peninsula^{[232][233][50][72][234]} and appears to relate to the same orbital forcing as the AHP.^[232] An early Holocene monsoonal episode extended as far as the Mojave Desert in North America.^[238] In contrast, a drier episode is recorded from much of South America where Lake Titicaca, Lake Junin, the discharge of the Amazon River and water availability in the Atacama were lower.^[239]

The discharge of the Congo, Niger,^[240] Nile,^[241] Ntem,^[33] Rufiji,^[242] and Sanaga rivers increased.^[240] Runoff from Algeria,^[243] equatorial Africa, northeastern Africa and the western Sahara was also larger.^[244] Changes in the morphology of the river systems and their alluvial plains occurred in response to the increased discharge,^[35][33] and the Senegal River expanded its riverbed,^[245] breached dunes and re-entered the Atlantic Ocean.^[99]

Flora and fauna of the Sahara

During the African humid period, lakes, rivers, wetlands and vegetation including grass and trees covered the Sahara and Sahel^{[148][246][144]} creating a "Green Sahara"^[247] with a land cover that has no modern analogues.^[248] Evidence includes pollen data, archaeological sites, evidence of faunal activity such as diatoms, mammals, ostracods, reptiles and snails, buried river valleys, organic-rich mats, mudstones, evaporites as well as travertines and tufas deposited in subaqueous environments.^[49]

The vegetation cover then extended over almost all of the Sahara^[48] and consisted of an open grass savannah with shrubs and trees,^[147][249] with a moist savanna vegetation getting established in the mountains.^[250] In general, the vegetation expanded northward^[50] to 27–30° northern latitude in West Africa^[251][10] with a Sahel boundary at about 23° north,^[53] as the Sahara was populated by plants that today often occur about 400–600 kilometres (250–370 mi)^[252][253] farther south.^[254] The northward movement of vegetation took some time and some plant species moved faster than others.^[255] Plants that perform C3 carbon fixation became more common.^[256] The fire regime of the vegetation changed;^[257] in the desert the expansion of vegetation facilitated fire activity, while in the savanna the increased prevalence of woody vegetation reduced fire activity.^[258]

Forests and plants from the humid tropics were concentrated around lakes, rivers^[259] and the Atlantic Ocean coast of Senegal;^[260] waterbodies were also settled by aquatic and partially aquatic plants^[261] and the Senegalese coast by mangroves.^[224] The landscape during the AHP has been described as a mosaic between various vegetation types of semi-desert and humid origin^[262] rather than a simple northward displacement of plant species,^[263] and some brown or yellow vegetation communities persisted.^[1] There was no southward displacement of Mediterranean plants during the Holocene^[264] and on the Tibesti Mountains cold temperatures may have restricted the expansion of tropical plants.^[265] Pollen data often show a dominance of grasses over humid tropics trees.^[10] The tree Lophira alata and others may have spread out of the African forests during the AHP,^[266] and the Lactuca plants may have split into two species under the effects of the AHP and other climate changes in Africa during the Holocene.^[267]

The Sahara climate did not become entirely homogeneous; its central-eastern parts were probably drier than the western and central sectors^[268] and the Libyan sand sea was still a desert^[1] although pure desert areas retreated or became arid/semiarid.^[269] An arid belt may have existed north of 22° latitude,^[270] or the vegetation^[154] and the African monsoon might have reached 28–31° northern latitude;^[271] in general conditions between 21° and 28° northern latitude are poorly known.^[272] Dry areas may have persisted in the rain shadows of mountains and could have supported arid climate vegetation, explaining the presence of its pollen in sediment cores.^[273] In addition, north–south gradations in vegetation patterns have been reconstructed from charcoal and pollen data.^[274]

Fossils record changes in the animal fauna of the Sahara.^[275] This fauna included antelopes,^[48] baboons, cane rats,^[276] catfish,^[277][278] clams,^[279] cormorants,^[280] crocodiles,^[48] elephants,^[281] frogs,^[282] gazelles,^[281] giraffes,^[48] hartebeest,^[277][283] hares,^[281] hippos,^[277][283] molluscs, Nile perches,^[284] pelicans,^[285] rhinoceroses,^[276] snake-eagles,^[280] snakes,^[282] tilapia,^[279] toads,^[282] turtles^[277] and many more animals,^[286] and in Egypt there were African buffaloes, spotted hyenas, warthogs, wildebeest and zebra.^[287] Additional birds include brown-necked raven, coot, common moorhen, crested grebe, glossy ibis, long-legged buzzard, rock dove, spur-winged goose and tufted duck.^[288] Large herds of animals lived in the Sahara.^[289] Some animals expanded over the whole desert, while others were limited to places with deep water.^[284] Earlier humid periods in the Sahara may have allowed species to cross the now-desert.^[270] A reduction in open grasslands at the beginning of the AHP may explain the decline of the populations of some mammals during^[290] and a population bottleneck in cheetahs at the start of the humid period,^[291] while leading to the expansion of the population of other animals such as Hubert's multimammate mouse^[292] and Natal multimammate mouse.^[293]

Lakes and rivers of the Sahara

A number of lakes formed^[275] or expanded in the Sahara^[209] and the Hoggar and Tibesti Mountains.^[294] The largest of them was Lake Chad which increased to at least ten times its present-day size^[295] to form Lake Megachad.^[151] This enlarged Lake Chad reached dimensions of 1,000 by 600 kilometres (620 mi × 370 mi) in north–south and east–west direction respectively,^[296] covering the Bodélé Depression^[297] and perhaps as much as 8% of the present-day Sahara desert.^[298] It influenced the climate itself;^[299] for example rainfall would have been reduced at the centre of the lake and increased at its margins.^[1] Lake Chad was possibly fed from the north by rivers draining the Hoggar (Taffassasset drainage)^[300] and Tibesti Mountains, from the Ennedi Mountains in the east through the "Eastern palaeorivers"^[301] and from the south by the Chari-Logone and Komadugu Rivers.^[302] The Chari River was the main tributary^[303] while the rivers draining the Tibesti formed alluvial fans^[304]/the Angamma river delta at their entry into northern Lake Chad.^[305] Skeletons of elephants, hippos and hominins have been found in the Angamma delta, which is the dominant shoreline feature of northern Lake Chad.^[296] The lake overflowed into the Niger River^[306] during highstand through the Mayo Kebbi and the Benue River, eventually reaching the Gulf of Guinea.^[302] Older dune systems were submerged by Lake Chad.^[307]

Among the large^[308] lakes which may have formed in the Sahara are Lake Megafezzan in Libya^[309] and Lake Ptolemy in Sudan.^{[308][298][310][311]} Quade et al. 2018 raised some doubts about the size and existence of some of these lakes such as Lake Ptolemy, Lake Megafezzan, Lake Ahnet-Mouydir;^[312] it is possible that giant lakes only formed in the southern part of the Sahara.^[313] Other lakes are known from Adrar Bous in Niger,^[99] Era Kohor and Trou au Natron in the Tibesti Mountains,^[314] I-n-Atei in the Hoggar, at Ine Sakane^[315] and in Taoudenni^[l] in Mali,^[317] the Garat Ouda and Takarkori Lakes in the Acacus Mountains,^[278] Chemchane in Mauretania,^[318] at Guern El Louläilet in the Great Western Erg^[319] and Sebkha Mellala close to Ouargla, both in Algeria,^[320] at Wadi Shati and elsewhere in the Fezzan in Libya,^[321] at Bilma, Dibella, Fachi^[322] and Gobero in the Ténéré,^[9] Seeterrassental in Niger^[323] and at "Eight Ridges",^[324] El Atrun,^[325] Lake Gureinat, Merga,^[326] "Ridge",^[324] Sidigh,^[326] at Wadi Mansurab,^[4] Selima and Oyo in Sudan.^[327] The lakes of Ounianga merged into two large lakes^[328] and overflowed, either above surface or underground.^[329] Mosaics of small lakes developed in some regions,^[310] such as the Grand Erg Occidental.^[330] Wetlands also expanded during the AHP, but both their expansion and subsequent retreat were slower than that of lakes.^[331] The Niger River, which had been dammed by dunes during the LGM, formed a lake in the Timbuktu region that eventually overflowed and drained at some point during the AHP.^[332]

In some parts of the Sahara ephemeral lakes formed such as at Abu Ballas, Bir Kiseiba, Bir Sahara, Bir Tarfawi and Nabta Playa^[m] in Egypt,^[333][326] which may relate to later Egyptian religions,^[335] or swamp-lakes such as at Adrar Bous close to the Air Mountains.^[322] Ephemeral lakes developed between dunes,^[278][336] and a "freshwater archipelago" appears to have existed in the Murzuq basin.^[337] All these lake systems left fossils such as fish, limnic sediments^[338] and fertile soils that were later used for agriculture (El Deir, Kharga Oasis).^[339] Finally, crater lakes formed in volcanic fields^[340] such as Trou au Natron and Era Kohor in the Tibesti,^[341] and sometimes survive to this day as smaller remnant lakes such as Malha crater^[342] in the Meidob volcanic field.^[340] Potentially, the increased availability of water during the AHP may have facilitated the onset of phreatomagmatic eruptions such as maar formation in the Bayuda volcanic field, although the chronology of volcanic eruptions there is not well known enough to substantiate a link to the AHP.^[343]

Increased precipitation resulted in the formation or reactivation of river systems in the Sahara.^[344] The large Tamanrasset River^[345] flowed from the Atlas Mountains and Hoggar westward towards the Atlantic^[346] and entered it in the Bay of Arguin in Mauretania.^[347] It once formed the 12th largest watershed in the world^[348] and left a submarine canyon and riverine sediments.^[349] Together with other rivers it formed estuaries and mangroves in the Bay of Arguin.^[347] Other rivers in the same area also formed submarine canyons,^[350] and sediment patterns in marine sediment cores^[351] and the occurrence of submarine landslides in the area have been related to the activity of these rivers.^[352]

Rivers such as the Irharhar in Algeria, Libya and Tunisia^[353] and the Sahabi and Kufra rivers in Libya were active during this time^[354] although there is some doubt that they had perennial flow;^[355] they appear to have been more important in earlier humid periods.^[349] Small watersheds,^[356] wadis^[357] and rivers discharging into endorheic basins such as Wadi Tanezzuft also carried water during the AHP.^[358][359] In Egypt, some rivers active during the AHP are now gravel ridges.^[360] In the Air, Hoggar and Tibesti Mountains, the so-called "Middle Terrace" was emplaced at this time.^[361] The rivers of the Sahara,^[354] lakes and their watersheds may have acted as pathways for the spread of humans and animals;^[362][363] the rivers were often connected to each other by alluvial fans.^[354] Proposed examples of animals that spread through rivers are the Nile crocodile and the fish Clarias gariepinus and Tilapia zillii.^[273] It is possible that the name Tassili n'Ajjer, which means "plateau of the rivers" in Berber, is a reference to past river flows.^[364] On the other hand, intense flows of these rivers may have made their shores dangerous to humans and thus created additional impetus for human movement.^[365][366] Now-dry river valleys from the AHP in the eastern Sahara have been used as analogues for former river systems on Mars.^[367]

Humans of the Sahara

Conditions and resources were ripe for first hunter-gatherers, fishermen^[368] and, later, pastoralists;^[369] the exact chronology - when humans returned in the Sahara after the onset of the AHP - is disputed.^[370] They may have come either from the north (Maghreb or Cyrenaica)^[371][372] where the Capsian culture^[n] was located,^[374] the south (Sub-Saharan Africa), or the east (Nile Valley).^[371] The human population in the Sahara rapidly increased during the AHP, interrupted by a brief decline between 7,600 and 6,700 years ago.^[375] Traces of human activity have been found in the Acacus Mountains^[376] where caves and rock shelters were used as basecamps for humans,^[377] such as the Uan Afuda cave^[376] and the Uan Tabu and Takarkori rock shelters.^[378] The first occupation in Takarkori took place between 10,000 and 9,000 years ago;^[379] about five millennia of human cultural evolution are recorded there.^[369] At Gobero in the Ténéré desert a cemetery has been found, which has been used to reconstruct the lifestyle of these former inhabitants of the Sahara,^[9] and at Lake Ptolemy in Nubia humans settled close to the lake shore, using its resources and perhaps even engaging in leisure activities.^[380] At that time, many humans appear to have depended on water-bound resources, seeing as many of the tools left by the early humans are associated with fishery; hence this culture is also known as "aqualithic"^[209][246] although substantial differences between the cultures of various places have been found.^[381] The greening of the Sahara led to a demographic expansion^[382] and especially in the Eastern Sahara human occupancy coincides with the AHP.^[383] Conversely occupation decreased along the Nile valley, perhaps due to the expansion of wetlands there^[384] and frequent large-scale flooding of the Nile delta.^[385]

Humans were hunting large animals with weapons that have been found in archaeological sites^[386] and wild cereals occurring in the Sahara during the AHP such as brachiaria, sorghum and urochloa were an additional source of food.^[387] Humans also domesticated cattle,^[71] goats and sheep.^[388] Cattle domestication may have occurred especially in the more environmentally variable Eastern Sahara,^[389] where the lack of lakes (cattle having high requirements of drinking water) may however have limited the occurrence of cattle.^[390] Animal husbandry picked up in earnest around 7,000 years ago when domestic animals came to the Sahara, and a population boom may be linked to this change in cultural practice;^[391][368] cattle and goats spread southwestwards from northeasternmost Africa from 8,000 years before present.^[392] Dairying has been demonstrated in some locations^[393] and cattle-husbandry is supported by the frequent depiction of cattle in rock paintings.^[394] The relative importance of hunter-gatherer practices and pastoralism, and whether people were sedentary or migratory, is unclear.^[395] The Dufuna canoe, one of the oldest known ships in the world,^[396] appears to date to the Holocene humid period and implies that the waterbodies of that time were navigated by humans.^[397] The cultural units "Masara" and "Bashendi" existed in Dakhleh Oasis during the AHP.^[398] In the Acacus Mountains, several cultural horizons known as Early and Late Acacus and Early, Middle, Late and Final Pastoral have been identified^[399] while in Niger the Kiffian culture has been related to the beginning of the AHP.^[400] Ancient civilizations thrived,^[50] with farming and animal husbandry taking place in Neolithic settlements.^[318][401] Possibly, the domestication of plants in Africa was delayed by the increased food availability during the AHP, it only took place around 2,500 BC.^[402][403]

Humans created rock art such as petroglyphs and rock paintings in the Sahara, perhaps the largest density of such creations in the world.^[404] Scenes include animals^[144] and everyday life^[404] such as swimming which supports the presence of past wetter climates.^[343] One well-known such petroglyph location is the Cave of Swimmers in the Gilf Kebir mountains of Egypt;^[405] other well known sites are the Gabal El Uweinat mountains also of Egypt,^[71] Arabia^[406] and the Tassili n'Ajjer in Algeria where rock paintings from this time have been discovered.^[407] Humans also left artifacts such as Fesselsteine^[o] and ceramics in what today are inhospitable deserts.^[71] North Africa together with East Asia is one of the first places where pottery was developed^[369] probably under the influence of increased availability of resources during the AHP. The humid period also favoured its development and spread in West Africa during the 10th millennium BC;^[409] the so-called "wavy line" or "dotted wavy-line" motif was widespread across Northern Africa^[381] and as far as Lake Turkana.^[410]

These populations have been described as Epipaleolithic, Mesolithic and Neolithic^[411] and produced a variety of lithic tools and other assemblages.^[412] In West Africa, the cultural change from the African Middle Stone Age to the Late Stone Age accompanied the beginning of the AHP.^[413] In Sudan, the beginning of the early Khartoum culture coincides with the initiation of the AHP.^[414] Genetic and archaeological data indicate that these populations which exploited the resources of the AHP Sahara probably originated in Sub-Saharan Africa and moved north after some time, after the desert got wetter;^[415] this may be reflected in the northward spread of Macrohaplogroup L and Haplogroup U6 genomic lineages.^[416] In return, the AHP facilitated the movement of some Eurasian populations into Africa,^[417] and bidirectional travel across the Sahara more generally.^[418] Elsewhere, newly formed or expanded water courses may have restricted human mobility and isolated populations.^[419] These favourable conditions for human populations may be reflected in paradise myths such as the Garden of Eden in The Bible and Elysium and the Golden Age in Classical Antiquity,^[420] and in the spread of the Nilo-Saharan languages.^[273][381]

Additional manifestations in the Sahara

The expanded vegetation and soil formation stabilized previously active dunes,^[421] eventually giving rise to the present-day draa dunes in the Great Sand Sea of Egypt for example,^[336] although there is uncertainty about whether this stabilization was widespread.^[422] Soil development and biological activity in soils are attested in the Acacus Mountains^[423] and the Mesak Settafet area of Libya,^[424] but evidence of soil formation^[425]/pedogenesis^[61] such as bog iron^[426] are described from other parts of the Sahara as well.^[61] In the Selima Sand Sheet, the landscape underwent erosional truncation and bioturbation.^[427] The Central and Southern Sahara saw the development of alluvial deposits^[209] while sebkha deposits are known from the Western Sahara.^[428] Lightning strikes into soil left lightning-altered rocks in parts of the Central Sahara.^[429]

The increased precipitation also resulted in recharged aquifers^[430][411] such as the Nubian Sandstone Aquifer; presently, water from this aquifer maintains several lakes in the Sahara, such as the Lakes of Ounianga.^[431] Other groundwater systems were active at that time in the Acacus Mountains, Air Mountains, in the Fezzan^[432] and elsewhere in Libya^[433] and the Sahel.^[434] Raised groundwater tables provided water to plants and was discharged in depressions,^[435] lakes^[127] and valleys, forming widespread carbonate deposits^[p] and feeding lakes.^[436]

The formation of lakes^[79] and vegetation reduced the export of dust from the Sahara. This has been recorded in marine cores,^[437][157] including one core where dust export decreased by almost half,^[438] and in Italian lakes.^[439] In coastal places, such as in Oman, sea level rise also reduced the production of dust.^[79] In the Mediterranean, a decreased dust supply was accompanied by increased sediment input from the Nile, leading to changes in marine sediment composition.^[440] Conversely, the increased vegetation may have yielded more volatile organic compounds in the air.^[441]

Whether the strengthening of the monsoon enhanced or reduced upwelling off Northwestern Africa is debatable,^[442] with some research suggesting that the strengthening in upwelling decreased sea surface temperatures^{[443][444][445]} and increased the biological productivity of the sea,^[442] while other research suggests that the opposite occurred; less upwelling with more moisture.^[72] However, regardless of whether upwelling increased or decreased, it is possible that the strengthening of the monsoon boosted productivity off the coasts of Northern Africa because the increased river discharge delivered more nutrients to the sea.^{[443][444][445]} The decline of dust input may have caused the cessation of deep-water coral growth in the eastern Atlantic during the AHP by starving them of nutrients.^[446]

Arabia

Precipitation in Dhofar and southwestern Arabia is brought by the African monsoon,^[447] and a change to a wetter climate resembling Africa has been noted in southern Arabia^[448] and Socotra from cave and river deposits.^[449] It possibly reached as far as Qatar.^[450] Holocene paleolakes are recorded at Tayma, Jubbah,^[451] in the Wahiba Sands of Oman^[452][453] and at Mundafan.^[454][455] In the Rub al-Khali lakes formed between 9,000 and 7,000 years ago^[456] and dunes were stabilized by vegetation,^[121] although the formation of lakes there was less pronounced than in the Pleistocene.^[457] The Wadi ad-Dawasir river system in central Saudi Arabia became active again^[454][455] with increased river runoff into the Persian Gulf.^[458] Wadis in Oman eroded across LGM dunes^[459] and formed accumulation terraces.^[460] Episodes of increased river discharge occurred in Yemen^[461] and increased precipitation is recorded in the caves of Hoti, Qunf in Oman, Mukalla in Yemen and Hoq Cave in Socotra.^[462] Increased precipitation resulted in increased groundwater flow, generating groundwater-fed lakes and carbonate deposits.^[463]

Forests and wildfire activity expanded across parts of Arabia.^[464] Freshwater sources in Arabia during the AHP became focus points of human activity^[465] and herding activity between mountains and lowlands occurred.^[121] In addition, karstic activity took place on exposed coral reefs in the Red Sea and traces of it are still recognizable today.^[466] Increased precipitation has been also invoked to explain decreased salinities in the Red Sea,^[467] increased sedimentation^[468] and increased river inflow, while dust input decreased.^[469] Rock art depicts wildlife that existed in Arabia during the humid period.^[470] Archaeological sites such as cairns appeared with the beginning of the humid period.^[471]

The humid period in Arabia did not last as long as in Africa,^[472] deserts did not retreat as much^[233] and precipitation may not have reached the central^[473] and northern part of the peninsula^[474] past Oman^[463] and the Yemen Highlands;^[475] northern Arabia remained somewhat drier than southern Arabia,^[476] droughts were still common^[477] and the land and still produced dust.^[478] One study has estimated that the amount of rainfall in the Red Sea did increase to no more than 1 metre per year (39 in/year).^[479] Whether some former lakes in Arabia were actually marshes is contentious.^[480]

East Africa

Nile discharge was higher than today^[241] and during the early African humid period, the Nile in Egypt flooded up to 3–5 metres (9.8–16.4 ft)^[241] higher than it did recently before flood control.^[111] The increased flooding may have turned the Nile Valley marshy and inhospitable^[366] and could explain why many archaeological sites along the Nile were abandoned during the AHP, with violent conflicts reconstructed from the Jebel Sahaba archaeological site.^[94][128] Early after the Younger Dryas, the Blue Nile would have been the major source of waters for the Nile.^[481] Waters from the Nile^[q] filled depressions like the Fayum Depression^[358] to form a deep lake with anoxic bottom waters^[482] and reaching 20 metres (66 ft) above sea level,^[483] probably once a geomorphic barrier was breached.^[484] Wetlands and anastomosing channels developed in the Nile Delta^[485] as sediment supply increased.^[486] In addition, Nile tributaries in northwestern Sudan^[487] such as Wadi Al-Malik,^[241] Wadi Howar^[r][489] and Valley of the Queens became active during the AHP^[490] and contributed sediments to the Nile.^[491] Wadi Howar was active until 4,500 years ago,^[489] and at the time often contained dune-dammed lakes, swamps and wetlands;^[492][222] it was the largest Saharan tributary of the Nile^[493] and constituted an important pathway into sub-Saharian Africa.^[241] Conversely it appears that Lake Victoria and Lake Albert were not overflowing into the White Nile for all of the AHP,^[494] and the White Nile would have been sustained by overflow from Lake Turkana.^[489] There appears to be a tendency over the course of the AHP for the discharge of the Blue Nile to decrease relative to that of the White Nile.^[495] The Blue Nile built an alluvial fan at its confluence with the White Nile, and incision by the Nile reduced flooding risk in some areas which thus became available for human use.^[241]

Closed lakes in East Africa rose, sometimes by hundreds of metres.^[496] Lake Suguta developed in the Suguta Valley, accompanied by the formation of river deltas where rivers such as the Baragoi River entered the lake.^[497] In turn, Lake Suguta overflowed into the Kerio River, this adding water to Lake Turkana^[498] where increased discharge by the Turkwel River led to the formation of a large river delta.^[499] The Omo River remained its principal inflow but the relative role of other water sources increased compared to present-day conditions.^[500][501] A 45 metres (148 ft) deep lake filled the Chew Bahir basin^[502] and together with Lakes Chamo and Abaya formed a river system flowing into Lake Turkana,^[503] which itself overflowed on its northwestern side through the Lotikipi Swamp into the White Nile.^[504][505] Deposits from this lake highstand form the Galana Boi Formation.^[381] The increased water depth reduced water mixing in Lake Turkana, allowing organic material to build up.^[506] This overflowing large lake was filled with freshwater and was populated by humans,^[507] typically in bays, along capes and protected shorelines;^[508] the societies there engaged in fishery^[507] but could probably also fall back on other resources in the region.^[509]

The Ethiopian^[510] Lake Abhe expanded to cover an area of 6,000 square kilometres (2,300 sq mi), much larger than the present-day lake, in the "Abhe IV"-"Abhe V" lake cycle.^[511] The enlarged lake covered a large area west of the present-day lake, present-day lakes Afambo, Gamari and Tendaho, reducing Borawli, Dama Ale and Kurub to islands.^[512] The maximum water level was reached during the early Holocene as river discharge increased, but was later limited by partial overflow and did not rise above 380 metres (1,250 ft) again.^[513] Deep thermal groundwater recharge occurred in the region.^[514] About 9,000 years of human occupation are documented at the lake.^[515] Archaeological sites indicate that people obtained resources from the lake and followed its rise^[513] and decline.^[516] The cultural traditions at Lake Abhe appear to be unusual by AHP/African standards.^[517]

Lake Zway and Lake Shala in Ethiopia joined with Lake Abiyata and Lake Langano to form a large waterbody^[518] which began overflowing into the Awash River.^[519] Other lakes that expanded include Lake Ashenge^[520] and Lake Hayq also in Ethiopia,^[521] Lake Bogoria, Lake Naivasha^[209] and Lake Nakuru/Lake Elmenteita all in Kenya,^[522] and Lake Masoko in Tanzania.^[520] Lakes formed in the caldera of the Menengai volcano^[523][524] and in the Chalbi region east of Lake Turkana; the lake covered an area of about 10,000 square kilometres (3,900 sq mi).^[525] A 1,600 square kilometres (620 sq mi) large and 50 metres (160 ft) deep Lake Magadi formed in the early Holocene,^[152] generating the "High Magadi Beds" sediments.^[526] This lake was fed by now-dry waterfalls and possibly from the neighbouring lake Koora.^[527] In the Danakil Depression of Ethiopia freshwater conditions became established.^[209] Lakes formed in depressions on the mountains around Lake Kivu.^[528] Some of these lakes became connected through overflow: Lake Nakuru-Elmenteita drained northward through the Menengai caldera,^[524] Baringo-Bogoria^[s], Suguta into Lake Turkana and from there into the Nile, carving gorges along the way. Lake Naivasha drained south through Lake Siriata^[532] into Lake Magadi-Natron.^[533] Overflow of several of these lakes allowed animals including Nile crocodiles and fish to propagate to the individual lake basins,^[534] but at the same time hindered the propagation of many land-based mammals.^[524] River systems in the southern Kenya Rift region became active.^[535]

Glaciers stopped retreating or briefly expanded in East Africa at the beginning of the AHP before continuing retreat.^[536] On Mount Kilimanjaro they may have expanded during the AHP^[537] after a phase during the Younger Dryas where the mountain was ice free,^[538] but the tree line also rose at that time, accompanied by soil formation.^[539] The wetter climate may have destabilized the neighbouring Mount Meru volcano, causing a giant landslide that removed its summit.^[540]

Erosion in catchments of East Africa increased with the beginning of the humid period but then decreased even before its end,^[541] as the increased weathering led to the formation of soils, these in turn to the establishment of a vegetation cover that subsequently reduced additional erosion.^[542][543] Increased weathering resulted in the increased consumption of atmospheric CO
₂ during the AHP.^[544]

Surprisingly, and contrary to the patterns expected from precessional changes, the East African Rift also experienced a wetter climates during the AHP,^[147] reaching as far south as Lake Rukwa and Lake Cheshi into the Southern Hemisphere.^[545][546] In the region of the African Great Lakes, pollen evidence points to the occurrence of forests including rainforest vegetation^[547] due to the increased precipitation,^[548] while today they occur only in limited areas there.^[547] Denser vegetation also occurred at Lake Turkana,^[549] with wooden vegetation covering almost half of the dry land^[550] although grasslands remained dominant.^[267] Development of forest vegetation around the African Great Lakes created an interconnected environment where species spread, increasing biodiversity with effects on the future when the environment became fragmented.^[551] Vegetation cover also increased in the Afar region^[552] and Ericaceae plants spread at high elevations.^[553] Forests and moisture-requiring vegetation expanded in the Bale Mountains.^[554] Different types of vegetation, including dryland vegetation, existed at Lake Malawi and Lake Tanganyika however,^[555] and vegetation did not change much.^[556] The wetter climate led to the formation of the Halalee paleosoil in the Afar region.^[557]

In East Africa, the AHP led to improved environmental conditions in terms of food and water supply from large lakes, allowing early human populations to survive and grow in size without requiring major changes in food gathering strategies.^[558] Pottery techniques such as the "dotted wavy line" and "Kanysore" are associated with fishing and foraging communities.^[410] In Somalia, the "Bardaale" lithic industry is linked to the AHP.^[559] Earlier wet and dry periods in East Africa may have influenced the evolution of humans^[560] and allowed their spread across the Sahara^[561] and into Europe.^[562]

Other parts of Africa and the rainforest realm

Lake Bosumtwi in Ghana rose during the AHP.^[563][t] Evidence there also suggests a decrease in wildfire activity took place.^[565] Tropical forests expanded in Cameroon Highlands^[566] and the Adamawa Plateau of Cameroon^[567][568] and moved upward at Lake Bambili also in Cameroon,^[569] causing an upward shift of afromontane vegetation.^[570] The core of the rainforest was probably unaltered by the African humid period, perhaps with some changes in species^[571][572] and an expansion of their area.^[69] There is some evidence that an "Equatorial humid period", mechanistically linked to equatorial insolation and extending into the Amazon, may have taken place in the eastern Congo region at the same time as the AHP^[573] or around its beginning and end.^[574] The peatlands of Central Congo started developing during the African humid period and peat continues to accumulate there to this day,^[575] albeit with a slowdown in the Cuvette Centrale after the end of the African humid period.^[576] In the Gulf of Guinea, increased sedimentation and changed sedimentation patterns from increased river runoff decreased the activity of submarine cold seeps offshore present-day Nigeria.^[577]

On São Nicolau and Brava in the Cape Verde Islands, precipitation and erosion increased.^[578] In the Canary Islands, there is evidence of a moister climate on Fuerteventura,^[579] the laurel forests changed perhaps as a consequence of the AHP.^[120] Recharge of groundwater levels have been inferred from Gran Canaria also in the Canary Islands, followed by a decrease after the end of the AHP.^[580] Choughs may have reached the Canary Islands from North Africa when the latter was wetter.^[581]

Levant and Mediterranean

High latitude Africa has not undergone large scale changes in the past 11,700 years;^[135] the Atlas Mountains may have blocked the monsoon from expanding further north.^[582] However, river valley^[583] and cave deposits showing a moister climate in southern Morocco,^[161] increased precipitation in the Algerian highlands,^[584] vegetation changes in the Middle Atlas,^[585] several floods in Tunisian rivers^[586] and ecosystem changes which impacted steppe-dependent rodents of Northern Africa have been linked to the AHP.^[587]

In the Pleistocene and Holocene humidity in the Mediterranean is often correlated to humidity in the Sahara,^[588][589] and the early-mid Holocene climate of Iberia, Italy, Negev and Northern Africa was wetter than today;^[590] in Sicily wettening correlates with ITCZ changes in Northern Africa.^[591] Mediterranean precipitation is brought by Mediterranean cyclones and the westerlies;^[588] either increased precipitation from the westerlies,^[592] northward moisture transport from Africa^[593] or monsoonal precipitation extending into the Mediterranean may have rendered it wetter.^[594] The connection between the African Monsoon and Mediterranean precipitation is unclear^[595][588] and it was winter rainfall that increased predominantly,^[596][597] although separating monsoonal and non-monsoonal precipitation can be difficult.^[598]

The Mediterranean Sea became less saline during the AHP, in part due to increased precipitation from the westerlies^[592] but also from increased river discharge in Africa, leading to the formation of sapropel layers when the increased runoff led to the Mediterranean becoming more stratified^{[u][600][601]} and eutrophied,^[602] with changes in the main water masses of the sea.^[603] The S1 sapropel layer is specifically associated with the AHP^[244] and with increased discharge of the Nile and other African rivers.^[349] These processes together with decreased dust transport by wind led to changes in the sediment patterns of the Mediterranean,^[604] and increased marine nutrient availability^[602] and food web productivity in the Mediterranean,^[605] which impacted the development of deep-sea corals.^[606]

In the Levant, wetter conditions during the AHP are recorded from Jeita Cave in Lebanon and Soreq Cave in Israel,^[607] while the Dead Sea has variously been reported to have grown^[597] or shrunk during the AHP. Such a decline, if it took place, and a decline of other southern European lakes were low during this period. This is unlike some earlier wet periods in the Sahara; possibly the stronger winter-summer insolation gradient in these earlier wet periods created a different moisture pattern than during the Holocene.^[608] The northern Mediterranean may have been drier, with more wildfire activity, during the AHP.^[609]

Southern Africa

The effects, if any, of the African humid period on Southern Africa have been unclear. Originally it was proposed that the orbitally driven changes would imply a dry period in Southern Africa which would have given way to moister conditions as the northern AHP ended,^[610][611] as the ITCZ should shift its average position between the two hemispheres.^[135] However, the lack of paleoclimatology data with sufficient time resolution from Southern Africa has made it difficult to assess the climate there during the AHP.^[611] More recently obtained paleoclimate data have suggested however that southern Africa was actually wetter during the AHP rather than drier,^[612][613] reaching as far as north-northwest Madagascar^[614][615] 23° south^[177] and as far as the catchment of the Orange River.^[616] The area between Lake Tanganyika and Lake Malawi has been interpreted as the limit of the AHP's influence.^[617]

Conversely, and consistent with the opposite reaction pattern of the Southern Hemisphere, the Zambezi River reached its lowest discharge during the AHP,^[618] and precipitation in the Central African Plateau and Zambia decreases in computer simulations of a Green Sahara.^[619] Thus, the AHP may not have reach southern^[620] or southeastern Africa.^[621] There may have been opposite changes in precipitation between southeast Africa and tropical East Africa,^[622] separated by a "hinge zone".^[176] Particular changes occurred in central southern Africa, where a dry period co-occurred with an expansion of Lake Makgadikgadi; presumably the lake during this dry interval was nourished by increased wetness over the Okavango River catchment in the Angolan Highlands due to the AHP;^[623] peatlands formed in Angola during the AHP.^[624] In general there is little consistency between Northern and Southern Africa in terms of hydrological changes during the Holocene,^[625] and nowhere are both the start and end of the AHP apparent.^[248] Orbitally-mediated changes in Northern Hemisphere climate affected the Southern Hemisphere through oceanic pathways involving sea surface temperatures.^[626] Additionally, wetter periods unrelated to the AHP may have occurred after deglaciation in Southern Africa.^[627]

Numerical estimates

Estimates of the exact amount of increased precipitation vary widely.^[628] During the African humid period, Saharan rainfall increased to 300–400 millimetres per year (12–16 in/year),^[629] and values exceeding 400 millimetres per year (16 in/year) may have spread to 19–21° northern latitude.^[630] In the eastern Sahara, a gradient from 200 millimetres per year (7.9 in/year) increment in the north to 500 millimetres per year (20 in/year) in the south has been identified.^[338] An area with less than 100 millimetres per year (3.9 in/year) may have remained in the Eastern Sahara however,^[631][632] although its driest parts may have received 20-fold more precipitation than today.^[435] Precipitation in the Sahara probably reached no more than 500 millimetres per year (20 in/year),^[633] with large uncertainty.^[223]

Other reconstructed values of the precipitation increase indicate an annual increase of about 150–320 millimetres (5.9–12.6 in) in Africa,^[634] with strong regional variation.^[635] From lake levels and other proxies, precipitation increases of 20–33%,^[636] 25-40%^[168] or 50–100%^[209]/40-150% have been inferred for East Africa,^[544] with an increase of 40% reconstructed for Northern Africa.^[637] In the early Holocene, there appears to have been an eastward- and northward-decreasing trend of humidity.^[638] Additionally, at Tayma in Arabia a threefold increase appears to have occurred^[639] and precipitation in the Wahiba Sands of Oman may have reached 250–500 millimetres per year (9.8–19.7 in/year).^[640]

Effect on other climate modesedit

The El Niño–Southern Oscillation is a major climate variability mode. Paleoclimatology records from Ecuador and the Pacific Ocean indicate that during the early and middle Holocene ENSO variability was suppressed by about 30–60%, which can be only partially explained through orbital forcing.^[641][642] The Green Sahara may have suppressed ENSO activity, forcing a La Niña–like climate state,^[643][642] in a climate model this is accompanied by decreased upwelling and deepening of the thermocline in the Eastern Pacific as the Walker circulation shifts westward.^[644][645] Easterly winds in the western Pacific Ocean increase, while they decrease in the eastern.^[646] In addition, Atlantic Niño sea surface temperature patterns develop in the Atlantic Ocean.^[647][648]

Remote effects of the AHP on climate have also been studied,^[649] although many changes are model-dependent and may also be inaccurate due to incorrect depictions of atmospheric dust distribution.^[650] Whether the reduced albedo of the Sahara during the AHP contributed to, or increased cloud cover counteracted, the warming of the Holocene thermal maximum is model-dependent;^[651] dust changes did not have a major effect.^[652] The AHP would also influence SSTs in the Indian Ocean, although there is not much evidence about the mid-Holocene sea temperatures there.^[650]

The AMOC transports heat from the Southern into the Northern Hemisphere^[165] and is implicated in starting the Holocene AHP an earlier AHPs after the end of an ice age.^[653] Various studies have been conducted to determine which effects reduced dust supply and the greening of the Sahara would have had on its intensity,^[654] with conflicting results on which effects would predominate.^[165] Increased heat transport either through the atmosphere or the ocean would result in warming in the Arctic.^[655]

Remote precipitation and the AHPedit

The Sahara greening intensified the Indian and Asian monsoons,^[650] warming^[656] and increased precipitation across most of the Tibetan Plateau^[657] especially late in the monsoon season, and climate simulations including a green Sahara reproduce the reconstructed palaeoclimates there better than these without.^[646] In a climate model, there is a shift in precipitation from snow to rain.^[658] The strengthened and expanding monsoons of Africa and Asia alter the atmospheric circulation of the planet, inducing a wetter East Asian Monsoon and drying across tropical South America and central-eastern North America.^{[659][660][661]} In East Asia, a strengthened anticyclone over the West Pacific delivers more moisture to northeastern China and Indochina, and less to central and south-eastern China.^[662] The reduced dust emission warms the North Atlantic and increases westerly flow into the North American Monsoon, strengthening it.^[663] The far-field precipitation changes reach as far as Europe and Australia.^[664] Discrepancies between modelled and reconstructed northward extension^[665][660] and precipitation in the Asian monsoon regions and the North American Monsoon area may be explained through these remote effects.^[666]

Sun et al. 2020 proposed that the greening of the Sahara during the AHP can increase precipitation over the Middle East even if neither the African nor the Indian monsoons reach it.^[667] During spring, the increased vegetation forces anomalous atmospheric circulations that direct moisture transport from the Mediterranean, the Red Sea and eastern tropical Africa into the Middle East, increasing precipitation^[668] and agricultural productivity there.^[669] This could explain increased precipitation in the Middle East during the AHP:^[670] A wet climate occurred in the Middle East during the early Holocene, leading to the Ubaid period of settlement in Mesopotamia, followed by dry phases around 5,500 years ago^[671] and a concomitant reduction in simulated wheat yield.^[672]

Hurricanes and the AHPedit

One climate model has indicated that a greener Sahara and reduced dust output would have increased tropical cyclone activity, especially over the Atlantic but also in most other tropical cyclone basins^[v]. Changes in the intensity of the storms, decreases in wind shear, changes in atmospheric circulation and less dust in the atmosphere, which results in warmer oceans, are responsible for this phenomenon,^[674] while tropical wave activity may have increased^[226] or decreased.^[675] The net effect could be a global increase in tropical cyclone activity, a westward shift within the ocean basins^[676] and in the Atlantic Ocean a shift towards later dates.^[677] While there are no good paleotempestology data for the time of the African humid period that could confirm or refute this theory^[678][679] and many of these records are specific for particular locations,^[680] hurricane activity^[681] including past strikes in Puerto Rico^[643] and in Vieques appear to correlate with the strength of the West African Monsoon^[682] and increased precipitation on the northern Yucatan Peninsula during the middle Holocene could be explained by increased hurricane activity during the AHP.^[683] On the other hand, at Grand Bahama Bank and the Dry Tortugas of South Florida a decrease of hurricane activity took place during the AHP^[684] and dust emission is not always anti-correlated to hurricane activity.^[685] Finally, the northward movement of the ITCZ during the AHP may have caused a corresponding northward movement of tropical cyclogenesis areas and storm tracks in the Atlantic Ocean,^[686][677] which could also explain decreased hurricane activity in the Bahamas and Dry Tortugas.^[684]

Fluctuationsedit

Climate variability during the AHP is poorly documented,^[687] but some gaps with less precipitation took place during the late glacial and the Holocene.^[249] During the Younger Dryas 12,500–11,500 years ago, the North Atlantic and Europe became much colder again and there was a phase of drought in the area of the African humid period,^[688][689] extending over both East Africa,^[w][691] where lake levels dropped in many places,^[692][693] southern Africa^[694] and West Africa. The dry interval extended to India^[691] and the Mediterranean^[695] where dune activity occurred in the Negev.^[696] At the end of the Younger Dryas, precipitation, lake levels and river runoff increased again, although south of the equator the return of humid conditions was slower than the relatively abrupt change to its north.^[697][639]

Another dry phase took place about 8,200 years ago, spanning East Africa^[186][698] and Northern Africa^[x] as documented by various lines of evidence^[701] such as decreased water levels in lakes.^[702] It coincided with cooling in the Northern Atlantic,^[703] in surrounding landmasses such as Greenland^[704] and around the world;^[392] the drought may be related to the 8.2 kiloyear event^[688] which separates the Greenlandian and Northgrippian stages of the Holocene^[705] and lasted for about one millennium.^[248] The 8,200 year event has also been noted in the Maghreb, where it is associated with a transition of the Capsian culture^[706] as well as with cultural changes both in the Sahara and the Mediterranean;^[377] at the Gobero cemetery a population change occurred after this dry interruption^[707] but the occurrence of widespread cultural changes appears to be questionable.^[27] This episode appears to have been caused by the draining of ice-dammed lakes in North America ^[708] although a low latitude origin has also been suggested.^[709]

Cooling of the Northern Atlantic during Heinrich event 1 and the Younger Dryas associated with a weaker Atlantic meridional overturning circulation leads to atmospheric pressure anomalies that shift the Tropical Easterly Jet and precipitation belts south, making Northern Africa drier. ^{[191][219][710]} Storm tracks shift north away from the Mediterranean.^[711] Earlier Heinrich events were also accompanied by drought in North Africa.^[60] Likewise, a weakening of moisture transport and a less eastward position of the Congo Air Boundary contributed to reducing precipitation in East Africa^[691] although some parts of southern Africa at Lake Malawi were wetter during the Younger Dryas.^[712]

Many humidity fluctuations in the early Holocene appear to be caused by the discharge of meltwater from the Laurentide Ice Sheet into the Atlantic, which weakens the Atlantic meridional overturning circulation.^[711] Some dry periods in marine cores in the Gulf of Guinea appear to coincide with events recorded in Greenland ice cores.^[713] Other variations in precipitation observed in records have been attributed to solar activity changes,^[15] water levels of Lake Turkana for example appear to reflect the 11-year solar cycle.^[714]

In Lake Turkana, water level fluctuations took place between 8,500 and 4,500 years before present, with highstands before 8,400, around 7,000 and between 5,500 and 5,000^[715] and lowstands around 8,000, 10,000 and 12,000 years before present.^[716] In total, five separate highstands are recorded in desert varnish around the lake.^[717] The highstands appear to be controlled by sea surface temperature patterns in the Atlantic and Indian Oceans, but also by overflow of water from Lake Suguta^[715] and Chew Bahir and upstream lakes into Lake Turkana.^[505] Volcanic and tectonic phenomena occur at Lake Turkana, but do not have the magnitude required to explain large changes in lake level.^[718] Water level fluctuations have also been inferred for Lake Chad on the basis of pollen data, especially towards the end of the AHP.^[719] In the Taoudenni lake fluctuations of about a quarter-millennium have been recorded^[720] and frequent droughts occurred in the Eastern Sahara.^[721]

Other variations appear to have occurred 9,500–9,000 and 7,400–6,800^[309] as well as 10,200, 8,200, 6,600 and 6,000 years before present; they were accompanied by decreased population density in parts of the Sahara,^[711] and other dry interludes in Egypt have been noted 9,400–9,300, 8,800–8,600, 7,100–6,900 and 6,100–5,900 years ago.^[722] The duration and severity of dry events is difficult to reconstruct^[392] and the impact of events like the Younger Dryas is heterogeneous even between neighbouring areas.^[723] During dry episodes, humans might have headed to waterbodies which still had resources,^[381] and cultural changes in the central Sahara have been linked to some dry episodes.^[724] Aside from fluctuations, a southward retreat of the humid period may have been underway after 8,000 years ago^[725] with a major drought around 7,800 years ago.^[726]

Endedit

The African humid period ended about 6,000–5,000 years ago;^[19][727] an ending date of 5,500 years before present is often used.^[728] After vegetation declined,^[73] the Sahara became barren and was claimed by sand.^[144] Wind erosion increased in northern Africa,^[729] and dust export from the now-desert^[711] and from dried up lakes^[730] such as the Bodélé Basin grew; Bodélé today is the largest single source of dust on Earth.^[731] The lakes dried up, mesic vegetation disappeared, and sedentary human populations were replaced by more mobile cultures.^[19] The transition from the "green Sahara" to the present-day dry Sahara is considered to be the greatest environmental transition of the Holocene in northern Africa;^[732] today almost no precipitation falls in the region.^[48] The end of the AHP but also its beginning could be considered a "climate crisis" given the strong and extended impact.^[703] Drying extended as far as the Canary Islands^[733][734] and southeastern Iran,^[735] and there is evidence of climate change on São Nicolau, Cape Verde.^[736]

The Piora Oscillation cold period in the Alps^[737] coincides with the end of the AHP;^[420][738] the period 5,600–5,000 years ago was characterized by widespread cooling and more variable precipitation changes around the world^[738] and was possibly forced by changes in solar activity and orbital parameters.^[739] It has also been named "Mid-Holocene Transition".^[740] Some changes in climate possibly extended into southeastern Australia,^[741] Central America^[742] and into South America.^[743] The neoglacial began.^[744]

A major pan-tropical environmental change took place about 4,000 years ago.^[745] This change was accompanied by the collapse of ancient civilizations, severe drought in Africa, Asia and the Middle East and the retreat of glaciers on Mount Kilimanjaro^[746] and Mount Kenya.^[747]

Chronologyedit

Whether the drying happened everywhere at the same time and whether it took place in centuries or millennia is unclear^{[281][50][144]} in part due to disagreeing records^[271]and has led to controversy,^[57][748] and such a disagreement on timing also exists with respect to the expected vegetation changes.^[180][230] Marine cores usually indicate an abrupt change^[749][141] but not without exceptions^[57] while pollen data do not, perhaps due to regional and local differences in vegetation.^[750] Africa is a diverse landscape^[751] and groundwater and local vegetation can modify local conditions;^[368] groundwater-fed water bodies for example persisted longer than those nourished by rain.^[284] The debate on how quickly the Sahara formed goes back to 1849, when the Prussian naturalist Alexander von Humboldt suggested that only a quick drying could form the desert.^[752]

Most recently, the idea has taken hold that the end of the African humid period occurred from north to south in a stepwise fashion.^{[753][754][368]} In northeastern Asia,^[755] the western Sahara and east Africa it ended within 500 years^[756] with a one-step drying 6,000 – 5,000 years ago north of the present-day monsoon belt. Farther south, precipitation decrease was more protracted^{[16][118][757][758]} and closer to the equator the AHP ended between 4,000 and 2,500 years ago.^[118][16] In East Africa, pronounced drying occurred between 4,500 and 3,500 years ago, centered on 4,000 years ago;^[248] Egypt during the Old Kingdom was still wetter than today.^[759] A later end in northeast Africa about 4,000 years ago may reflect the different configuration of landmasses and thus monsoon behaviour,^[760] while other research has found a westward propagating drying trend.^[117]

Some evidence points to a two-phase change in climate with two distinct dry transitions^[761] caused by the existence of two different steps of insolation decrease at which climate changes.^[762] Distinct environmental changes may have occurred in Central Africa, Western Africa and East Africa.^[748] Finally, sometimes the 4.2 kiloyear event - the transition from the Northgrippian to the Meghalayan stage of the Holocene -^[705] is considered to be the true end of the AHP,^[709] especially in central Africa.^[763]

Increased variability in precipitation may have preceded the end of the AHP; this is commonly observed before a sudden change in climate.^[764] In Gilf Kebir, between 6,300 and 5,200 years ago apparently a winter rainfall regime became established as the AHP ended.^[202] Later fluctuations in climate that produced brief humid spells also took place,^[765] such as a moister period between 500 BCE – 300 CE in Roman Northern Africa and along the Dead Sea^[766] and an earlier one 2,100 years before present in the western Sahel.^[120] By 2,700 years ago the central Sahara had become a desert and remained one until the present-day.^[767]

Sahara and Saheledit

After a first brief lake level drop between 5,700 and 4,700 calibrated years ago that might reflect climate variability towards the end of the African humid period,^[768][769] water levels in Lake Megachad decreased quickly after 5,200 years before present.^[770] It shrank to about 5% of its former size,^[296] with the deeper northern Bodele basin drying up entirely about 2,000^[303]-1,000 years ago^[771] as it was disconnected from the southern basin where its major tributary, the Chari River, enters Lake Chad.^[296] The dried out basin was now exposed to the Harmattan winds, which blow dust out of the dry lake bed,^[772] making it the single largest source of dust in the world.^[773] Dunes formed in the dried-up Sahara^[774] and Sahel^[775] or began moving again after stabilizing during the AHP.^[776]

The tropical vegetation was replaced by desert vegetation, in some places suddenly and in others more gradually.^[777] Along the Atlantic coast, the vegetation retreat was slowed by a stage of sea level rise that increased soil moisture levels, delaying the retreat by about two millennia.^[778][779] A gradual decline has been noted in the Tibesti.^[780] In Libya at Wadi Tanezzuft the end of the humid period was also delayed by leftover water in dune systems and in the Tassili mountains until 2,700 years ago, when river activity finally ceased.^[83][781] A brief moist pulse between 5,000 – 4,000 years ago in the Tibesti led to the development of the so-called "Lower Terrace".^[782] The Egyptian Sahara might still have been vegetated until 4,200 years ago, based on depictions of savanna environments in Fifth Dynasty tombs in Egypt.^[783]

At Lake Yoa, which is groundwater-fed, vegetation decreased and became desert vegetation between 4,700–4,300 and 2,700 years ago, while the lake became hypersaline 4,000 years ago.^{[784][785][786]} Lake Teli dried out completely about 4,200 years ago.^[787] However, the climate of the Ounianga lakes may have been affected by the Tibesti Mountains and the end of the AHP thus delayed,^[770] and fossil groundwater left by the AHP nourishes the lake to this day.^[788] In the central Sahara, water resources in the mountains persisted longer.^[789]

East Africa and Arabiaedit

In northern East Africa, water levels dropped rapidly about 5,500 years ago^[213] while in Hoti cave in Arabia a southward retreat of the Indian Monsoon took place about 5,900 years ago.^[121] Drying is also documented from Oman,^[129] and rivers and lakes of Arabia became intermittent or entirely dry.^[790] The Blue Nile basin became less moist^[129] with a noticeable decrease of Nile discharge about 4,000 years ago.^[604] Decreased discharge of the Nile led to the cessation of sapropel deposition and turbidite activity off its delta,^[111] the abandonment of river channels in its delta and upstream^[791] and increased seawater influence in the delta.^[792]

Some data from Ethiopia and the Horn of Africa indicate that drying there may have begun already 7,000–8,000 years ago or earlier.^[693][449] Reconstructions from Lake Abiyata in Ethiopia suggest that the end of the African humid period took the form of severe droughts rather than a gradual decrease of precipitation.^[793] Drying in Arabia commenced about 7,000 calibrated years ago^[465] and there are large disparities in the timing between various parts of Arabia^[794] but a tendency towards an arid climate between 6,000 and 5,000 years ago has been observed^[795][796] which continued until 2,700 years ago.^[452] In the Bale Mountains and the Sanetti Plateau of Ethiopia vegetation changes signalling a drier climate took place around 4,600 years ago.^[797]

Forest cover in the area of the African Great Lakes decreased between 4,700 and 3,700 years ago,^[547] although drying at Lake Victoria had begun around 8,000 years ago,^[555] at Lake Rukwa 6,700 years ago,^[545] at Lake Tanganyika about 6,000 years ago^[555] and at Lake Edward major changes in lake chemistry consistent with drying are noted 5,200 years ago. There a minor recovery in vegetation took place between 2,500 and 2,000 years ago, followed by a much more rapid appearance of grasses accompanied also by substantial wildfire activity. This might have been the most severe drought of the Lake Edward region in the Holocene, with many lakes such as Lake George dropping significantly or drying up altogether.^[798] Other lakes such as Nakuru, Turkana, Lake Chew Bahir, Lake Abbe and Lake Zway also dropped between 5,400 and 4,200 years ago.^[799] Decreased vegetation cover in the catchment of the Blue Nile has been correlated with increased sediment transport in the river beginning 3,600 – 4,000 years ago.^[800]

The end of the AHP at Lake Turkana occurred about 5,000^[717]-5,300 years before present, accompanied by a lake level decline^[801] and the cessation of overflow from other lakes in its area into Lake Turkana.^[499] Between 5,000 and 4,200, Lake Turkana became more saline and its water levels decreased below the level of outflow to the Nile.^[802] Towards the end of the AHP water temperatures in the lake and in other regional lakes appear to have increased, followed by a drop after its end^[803] possibly resulting from the insolation seasonality pattern that was in force at the time of the end of the AHP.^[804] The decrease of water levels in Lake Turkana also impacted the Nile and the Predynastic societies dependent on it.^[805]

Mediterraneanedit

The southern Aegean,^[806] Libya and the Middle Atlas became gradually more dry,^[777] and drying in Morocco took place about 6,000 radiocarbon years ago,^[761] Drier conditions in Iberia accompanied the end of the African humid period between 6,000 and 4,000 years ago, perhaps as a consequence of increasingly frequent positive North Atlantic Oscillation episodes and the shift of the ITCZ.^{[807][808][809]} More complicated changes have been found for the northern margin of the Mediterranean,^[810] and winter rainfall increased in the Levant at the end of the AHP.^[811] A 4.2 kiloyear event is recorded in dust records from the Mediterranean^[812] and might have been caused by changes in the circulation of the Atlantic Ocean.^[193]

Tropical West Africaedit

In Lake Bosumtwi the African humid period ended about 3,000 years ago^[144] after a brief moistening between 5,410 ± 80 years ago that ended 3,170 ± 70 years ago. This, earlier but similar changes off western Senegal and later but similar changes in the Congo Fan appear to reflect a southward shift of the precipitation zone over time.^[710] Some drying occurred simultaneously between the Sahel and the Gulf of Guinea.^[219] Some lakes in the Guineo-Congolian region dried out, while others were relatively unaffected.^[778]

A general tendency towards a drier climate is observed in West Africa at the end of the AHP.^[813] There, dense vegetation became progressively thinner between 5,000 and 3,000 years ago,^[798] and major perturbations of the vegetation took place around 4,200 and 3,000–2,500^[814][815] /2,400 calibrated years ago.^[816] A brief return of moister conditions took place 4,000 years ago^[703] while a substantial dry phase occurred between 3,500 and 1,700 years ago.^[813] Aridity became established between 5,200 and 3,600 years ago in the Sahara.^[817] In Senegal mangroves collapsed 2,500 years ago^[224] and modern-type vegetation arose about 2,000 years ago.^[818]

Central Africaedit

Farther south at the equator between 6,100 and 3,000 calibrated years before present savannah expanded at the expense of forests, with the transition possibly lasting until 2,500 calibrated years before present;^[745] a different time course estimate for the area between 4° southern and 7° northern latitude states that forest cover decreased between 4,500 and 1,300 years ago.^[778] In the Adamawa Plateau (Cameroon^[819]), the Ubangui Plateau (Central African Republic^[819]) and the Cameroon Volcanic Line montane forests disappeared at the end of the African humid period.^[820] In the Adamawa Plateau savanna has continuously expanded since 4,000 calibrated years ago.^[816] Such a change took also place in Benin and Nigeria between 4,500 and 3,400 calibrated years ago.^[778] Climate around the Gulf of Guinea became drier at the end of the AHP, although forests remained stable on Sao Tome.^[570] In the Congo Basin, there were changes in the composition and density of the forests rather than their extent,^[821] and along the equator precipitation may have increased around 4.2 ka.^[822] Many vegetation changes in the tropical regions were probably caused by a longer dry season^[823] and perhaps a smaller latitudinal range of the ITCZ.^[816]

Southern Hemisphere Africaedit

In the Southern Hemisphere at Lake Malawi drying began later – 1,000 years before present – as did the African humid period which there began only about 8,000 years ago.^[803] Contrarily, increased water levels in Etosha Pan (Namibia) appear to relate to a southward movement of the ITCZ at the end of the AHP^[824] although stalagmite growth data in Dante Cave also in Namibia has been interpreted as indicating a wetter climate during the AHP.^[612] Several records indicate that 5,500 years ago, precipitation changed in an east-west dipole-like way^[825] with drying in the west and moistening in the east.^[826] This pattern was probably driven by shifts in atmospheric moisture transport and of rain belt width.^[827]

Mechanismsedit

The end of the humid period appears to reflect the changes in insolation during the Holocene,^[118] as a progressive decrease of summer insolation caused the insolation gradients between Earth's hemispheres to decrease.^[828] However, the drying appears to have been much more abrupt than the insolation changes;^[141] it is not clear whether non-linear feedbacks led to abrupt changes in climate and it is also unclear whether the process, driven by orbital changes, was abrupt.^[144] Also, the Southern Hemisphere warmed and this resulted in a southward shift of the ITCZ;^[829] orbitally-driven insolation has increased over the Holocene in the Southern Hemisphere.^[133]

As precipitation decreased, so did vegetation, in turn increasing the albedo and further decreasing precipitation.^[148] Furthermore, vegetation may have responded to increased variations in precipitation towards the end of the AHP^[145] although this view has been challenged.^[830] This could have directed sudden changes in precipitation, although this view has been cast in doubt by the observation that in many places the end of the African humid period was gradual rather than sudden.^[831] Plants at higher and lower latitudes might respond differently to climate change; for example more diverse plant communities might have slowed down the end of the AHP.^[90]

Other proposed mechanisms:

• Decreases in polar insolation through altered cosmic ray fluxes might promote the growth of sea ice and cooling at high latitudes, which in turn result in stronger equator-to-pole temperature gradients, stronger subtropical anticyclones and more intense upwelling in for example the Benguela current.^[211]
• Changes in the circulation of high latitude oceans may have played a role,^[828] such as the potential occurrence of another meltwater/ice rafting pulse around 5,700 years before present.^[829] The decreased insolation during the mid-Holocene may have made the climate system more sensitive to changes, explaining why earlier comparable pulses did not terminate the humid period for good.^[832]
• There is evidence that glaciers in Tibet such as at Nanga Parbat expanded during the Holocene, especially towards the end of the AHP.^[833] In climate models, increased snow and ice on the Tibetan Plateau can lead to a weakening of the Indian and African monsoons, with the weakening of the former preceding that of the latter by 1,500–2,000 years.^[834]
• Decreases in sea surface temperatures of the Indian Ocean may be involved in the drying of East Africa, but there is no agreement on the temperature records from that ocean.^[182] Moreover, there is no evidence of temperature changes in the Gulf of Guinea at the critical time that might explain the end of the AHP.^[213]
• Additional feedback processes may have included the drying of soils and loss of vegetation after decreased rainfall,^[144] which would have led to wind-driven deflation of the soils.^[835]
• An expansion of sea ice around Greenland, Ellesmere Island 6,000^[836] and Antarctica about 5,000 calibrated years ago may have provided another positive feedback.^[837]
• The expanding dry belt of the Sahara pushed the regions of cyclogenesis in the Mediterranean northwest-northward, resulting in wind changes^[838] and precipitation regime changes in parts of Italy.^[839]
• Climate change at high latitudes has been proposed as a cause for the end of the AHP. Specifically, about 6,000–5,000 years ago the Arctic became colder, with sea ice expanding, temperatures in Europe and off Northern Africa decreasing and the Atlantic meridional overturning circulation weakening.^[213] This cooling tendency may have weakened the Tropical Easterly Jet and thus reduced the amount of precipitation falling over Africa.^[840]

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