Eocene

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Eocene
56.0 – 33.9 Ma
A map of Earth 45 million years ago during the Eocene Epoch, Lutetian Age
Chronology
Etymology
Name formalityFormal
Usage information
Celestial bodyEarth
Regional usageGlobal (ICS)
Time scale(s) usedICS Time Scale
Definition
Chronological unitEpoch
Stratigraphic unitSeries
Time span formalityFormal
Lower boundary definitionStrong negative anomaly in δ13C values at the PETM[3]
Lower boundary GSSPDababiya section, Luxor, Egypt[3]
25°30′00″N 32°31′52″E / 25.5000°N 32.5311°E / 25.5000; 32.5311
Lower GSSP ratified2003[3]
Upper boundary definitionLAD of Planktonic Foraminifers Hantkenina and Cribrohantkenina
Upper boundary GSSPMassignano quarry section, Massignano, Ancona, Italy
43°31′58″N 13°36′04″E / 43.5328°N 13.6011°E / 43.5328; 13.6011
Upper GSSP ratified1992[4]

The Eocene (IPA: /ˈiːəsiːn, ˈiːoʊ-/ EE-ə-seen, EE-oh-[5][6]) is a geological epoch that lasted from about 56 to 33.9 million years ago (Ma). It is the second epoch of the Paleogene Period in the modern Cenozoic Era. The name Eocene comes from the Ancient Greek Ἠώς (Ēṓs, "Dawn") and καινός (kainós, "new") and refers to the "dawn" of modern ('new') fauna that appeared during the epoch.[7][8]

The Eocene spans the time from the end of the Paleocene Epoch to the beginning of the Oligocene Epoch. The start of the Eocene is marked by a brief period in which the concentration of the carbon isotope 13C in the atmosphere was exceptionally low in comparison with the more common isotope 12C. The average temperature of Earth at the beginning of the Eocene was about 27 degrees Celsius.[9] The end is set at a major extinction event called the Grande Coupure (the "Great Break" in continuity) or the Eocene–Oligocene extinction event, which may be related to the impact of one or more large bolides in Siberia and in what is now Chesapeake Bay. As with other geologic periods, the strata that define the start and end of the epoch are well identified,[10] though their exact dates are slightly uncertain.

Etymology

The term "Eocene" is derived from Ancient Greek Ἠώς (Ēṓs) meaning "Dawn", and καινός kainos meaning "new" or "recent", as the epoch saw the dawn of recent, or modern, life.

Scottish geologist Charles Lyell (ignoring the Quaternary) divided the Tertiary Epoch into the Eocene, Miocene, Pliocene, and New Pliocene (Holocene) Periods in 1833.[11][n 1] British geologist John Phillips proposed the Cenozoic in 1840 in place of the Tertiary,[12] and Austrian paleontologist Moritz Hörnes introduced the Paleogene for the Eocene and Neogene for the Miocene and Pliocene in 1853.[13] After decades of inconsistent usage, the newly formed International Commission on Stratigraphy (ICS), in 1969, standardized stratigraphy based on the prevailing opinions in Europe: the Cenozoic Era subdivided into the Tertiary and Quaternary sub-eras, and the Tertiary subdivided into the Paleogene and Neogene periods.[14] In 1978, the Paleogene was officially defined as the Paleocene, Eocene, and Oligocene epochs; and the Neogene as the Miocene and Pliocene epochs.[15] In 1989, Tertiary and Quaternary were removed from the time scale due to the arbitrary nature of their boundary, but Quaternary was reinstated in 2009.[16]

Geology

Boundaries

The Eocene is a dynamic epoch that represents global climatic transitions between two climatic extremes, transitioning from the hot house to the cold house. The beginning of the Eocene is marked by the Paleocene–Eocene Thermal Maximum, a short period of intense warming and ocean acidification brought about by the release of carbon en masse into the atmosphere and ocean systems,[17] which led to a mass extinction of 30–50% of benthic foraminifera (single-celled species which are used as bioindicators of the health of a marine ecosystem)—one of the largest in the Cenozoic.[18][19] This event happened around 55.8 Ma, and was one of the most significant periods of global change during the Cenozoic.[17][20][21]

The middle Eocene was characterized by the shift towards a cooler climate at the end of the EECO, around 47.8 Ma, which was briefly interrupted by another warming event called the middle Eocene climatic optimum (MECO).[22] Lasting for about 400,000 years, the MECO was responsible for a globally uniform 4° to 6°C warming of both the surface and deep oceans, as inferred from foraminiferal stable oxygen isotope records. The resumption of a long-term gradual cooling trend resulted in a glacial maximum at the late Eocene/early Oligocene boundary.

The end of the Eocene was also marked by the Eocene–Oligocene extinction event, also known as the Grande Coupure.[23]

Stratigraphy

The Eocene is conventionally divided into early (56–47.8 Ma), middle (47.8–38 Ma), and late (38–33.9 Ma) subdivisions.[24] The corresponding rocks are referred to as lower, middle, and upper Eocene. The Ypresian Stage constitutes the lower, the Priabonian Stage the upper; and the Lutetian and Bartonian stages are united as the middle Eocene.[citation needed]

The Western North American floras of the Eocene were divided into four floral "stages" by Jack Wolfe (1968) based on work with the Puget Group fossils of King County, Washington. The four stages, Franklinian, Fultonian, Ravenian, and Kummerian covered the Early Eocene through early Oligocene, and three of the four were given informal early/late substages. Wolfe tentatively deemed the Franklinian as Early Eocene, the Fultonian as Middle Eocene, the Ravenian as Late, and the Kummerian as Early Oligocene.[25] The beginning of the Kummerian was refined by Gregory Retallack et al (2004) as 40 Mya, with a refined end at the Eocene-Oligocene boundary where the younger Angoonian floral stage starts.[26]

Palaeogeography and tectonics

A map of Earth in the early Eocene (50 Ma)

During the Eocene, the continents continued to drift toward their present positions.

At the beginning of the period, Australia and Antarctica remained connected, and warm equatorial currents may have mixed with colder Antarctic waters, distributing the heat around the planet and keeping global temperatures high. When Australia split from the southern continent around 45 Ma, the warm equatorial currents were routed away from Antarctica. An isolated cold water channel developed between the two continents.[27] However, modeling results call into question the thermal isolation model for late Eocene cooling,[28] and decreasing carbon dioxide levels in the atmosphere may have been more important. Once the Antarctic region began to cool down, the ocean surrounding Antarctica began to freeze, sending cold water and icefloes north and reinforcing the cooling.[29]

The northern supercontinent of Laurasia began to fragment, as Europe, Greenland and North America drifted apart.[30]

In western North America, the Laramide Orogeny came to an end in the Eocene, and compression was replaced with crustal extension that ultimately gave rise to the Basin and Range Province.[31][32] The Kishenehn Basin, around 1.5 km in elevation during the Lutetian, was uplifted to an altitude of 2.5 km by the Priabonian.[33] Huge lakes formed in the high flat basins among uplifts,[34] resulting in the deposition of the Green River Formation lagerstätte.[35]

At about 35 Ma, an asteroid impact on the eastern coast of North America formed the Chesapeake Bay impact crater.[36][37]

The Tethys Ocean finally closed with the collision of Africa and Eurasia,[38] while the uplift of the Alps isolated its final remnant, the Mediterranean, and created another shallow sea with island archipelagos to the north.[39] Planktonic foraminifera in the northwestern Peri-Tethys are very similar to those of the Tethys in the middle Lutetian but become completely disparate in the Bartonian, indicating biogeographic separation.[40] Though the North Atlantic was opening,[41] a land connection appears to have remained between North America and Europe since the faunas of the two regions are very similar.[42]

Eurasia was separated in three different landmasses 50 Ma; Western Europe, Balkanatolia and Asia. About 40 Ma, Balkanatolia and Asia were connected, while Europe was connected 34 Ma.[43][44] The Fushun Basin contained large, suboxic lakes known as the paleo-Jijuntun Lakes.[45]

India collided with Asia, folding to initiate formation of the Himalayas.[46] The incipient subcontinent collided with the Kohistan–Ladakh Arc around 50.2 Ma and with Karakoram around 40.4 Ma, with the final collision between Asia and India occurring ~40 Ma.[47][48]

Climate

The Eocene Epoch contained a wide variety of climate conditions that includes the warmest climate in the Cenozoic Era, and arguably the warmest time interval since the Permian-Triassic mass extinction and Early Triassic, and ends in an icehouse climate.[49] The evolution of the Eocene climate began with warming after the end of the Paleocene–Eocene Thermal Maximum (PETM) at 56 Ma to a maximum during the Eocene Optimum at around 49 Ma. During this period of time, little to no ice was present on Earth with a smaller difference in temperature from the equator to the poles.[50] Because of this the maximum sea level was 150 meters higher than current levels.[51] Following the maximum was a descent into an icehouse climate from the Eocene Optimum to the Eocene–Oligocene transition at 34 Ma. During this decrease, ice began to reappear at the poles, and the Eocene–Oligocene transition is the period of time when the Antarctic ice sheet began to rapidly expand.[52]

Early Eocene

Greenhouse gases, in particular carbon dioxide and methane, played a significant role during the Eocene in controlling the surface temperature. The end of the PETM was met with very large sequestration of carbon dioxide into the forms of methane clathrate, coal, and crude oil at the bottom of the Arctic Ocean, that reduced the atmospheric carbon dioxide.[53] This event was similar in magnitude to the massive release of greenhouse gasses at the beginning of the PETM, and it is hypothesized that the sequestration was mainly due to organic carbon burial and weathering of silicates. For the early Eocene there is much discussion on how much carbon dioxide was in the atmosphere. This is due to numerous proxies representing different atmospheric carbon dioxide content. For example, diverse geochemical and paleontological proxies indicate that at the maximum of global warmth the atmospheric carbon dioxide values were at 700–900 ppm,[54] while model simulations suggest a concentration of 1,680 ppm fits best with deep sea, sea surface, and near-surface air temperatures of the time.[55] Other proxies such as pedogenic (soil building) carbonate and marine boron isotopes indicate large changes of carbon dioxide of over 2,000 ppm over periods of time of less than 1 million years.[56] This large influx of carbon dioxide could be attributed to volcanic out-gassing due to North Atlantic rifting or oxidation of methane stored in large reservoirs deposited from the PETM event in the sea floor or wetland environments.[54] For contrast, today the carbon dioxide levels are at 400 ppm or 0.04%.

During the early Eocene, methane was another greenhouse gas that had a drastic effect on the climate. Methane has 30 times more of a warming effect than carbon dioxide on a 100-year scale (i.e., methane has a global warming potential of 29.8±11).[57] Most of the methane released to the atmosphere during this period of time would have been from wetlands, swamps, and forests.[58] The atmospheric methane concentration today is 0.000179% or 1.79 ppmv. As a result of the warmer climate and the sea level rise associated with the early Eocene, more wetlands, more forests, and more coal deposits would have been available for methane release. If we compare the early Eocene production of methane to current levels of atmospheric methane, the early Eocene would have produced triple the amount of methane. The warm temperatures during the early Eocene could have increased methane production rates, and methane that is released into the atmosphere would in turn warm the troposphere, cool the stratosphere, and produce water vapor and carbon dioxide through oxidation. Biogenic production of methane produces carbon dioxide and water vapor along with the methane, as well as yielding infrared radiation. The breakdown of methane in an atmosphere containing oxygen produces carbon monoxide, water vapor and infrared radiation. The carbon monoxide is not stable, so it eventually becomes carbon dioxide and in doing so releases yet more infrared radiation. Water vapor traps more infrared than does carbon dioxide. At about the beginning of the Eocene Epoch (55.8–33.9 Ma) the amount of oxygen in the Earth's atmosphere more or less doubled.[59]

During the warming in the early Eocene between 55 and 52 Ma, there were a series of short-term changes of carbon isotope composition in the ocean.[60][61] These isotope changes occurred due to the release of carbon from the ocean into the atmosphere that led to a temperature increase of 4–8 °C (7.2–14.4 °F) at the surface of the ocean. Recent analysis of and research into these hyperthermals in the early Eocene has led to hypotheses that the hyperthermals are based on orbital parameters, in particular eccentricity and obliquity. The hyperthermals in the early Eocene, notably the Palaeocene–Eocene Thermal Maximum (PETM), the Eocene Thermal Maximum 2 (ETM2), and the Eocene Thermal Maximum 3 (ETM3), were analyzed and found that orbital control may have had a role in triggering the ETM2 and ETM3.[62][63][64] An enhancement of the biological pump proved effective at sequestering excess carbon during the recovery phases of these hyperthermals.[65] These hyperthermals led to increased perturbations in planktonic and benthic foraminifera,[66][67] with a higher rate of fluvial sedimentation as a consequence of the warmer temperatures.[68] Unlike the PETM, the lesser hyperthermals of the Early Eocene had negligible consequences for terrestrial mammals.[69] These Early Eocene hyperthermals produced a sustained period of extremely hot climate known as the Early Eocene Climatic Optimum (EECO).[70] During the early and middle EECO, the superabundance of the euryhaline dinocyst Homotryblium in New Zealand indicates elevated ocean salinity in the region.[71]

Equable climate problem

One of the unique features of the Eocene's climate as mentioned before was the equable and homogeneous climate that existed in the early parts of the Eocene. A multitude of proxies support the presence of a warmer equable climate being present during this period of time. A few of these proxies include the presence of fossils native to warm climates, such as crocodiles, located in the higher latitudes,[72][73] the presence in the high latitudes of frost-intolerant flora such as palm trees which cannot survive during sustained freezes,[73][74] and fossils of snakes found in the tropics that would require much higher average temperatures to sustain them.[73] TEX86 BAYSPAR measurements indicate extremely high sea surface temperatures of 40 °C (104 °F) to 45 °C (113 °F) at low latitudes,[75] although clumped isotope analyses point to a maximum low latitude sea surface temperature of 36.3 °C (97.3 °F) ± 1.9 °C (35.4 °F) during the EECO.[76] Relative to present-day values, bottom water temperatures are 10 °C (18 °F) higher according to isotope proxies.[74] With these bottom water temperatures, temperatures in areas where deep water forms near the poles are unable to be much cooler than the bottom water temperatures.[citation needed]

An issue arises, however, when trying to model the Eocene and reproduce the results that are found with the proxy data.[77] Using all different ranges of greenhouse gasses that occurred during the early Eocene, models were unable to produce the warming that was found at the poles and the reduced seasonality that occurs with winters at the poles being substantially warmer. The models, while accurately predicting the tropics, tend to produce significantly cooler temperatures of up to 20 °C (36 °F) colder than the actual determined temperature at the poles.[74] This error has been classified as the "equable climate problem". To solve this problem, the solution would involve finding a process to warm the poles without warming the tropics. Some hypotheses and tests which attempt to find the process are listed below.[citation needed]

Large lakes

Due to the nature of water as opposed to land, less temperature variability would be present if a large body of water is also present. In an attempt to try to mitigate the cooling polar temperatures, large lakes were proposed to mitigate seasonal climate changes.[78] To replicate this case, a lake was inserted into North America and a climate model was run using varying carbon dioxide levels. The model runs concluded that while the lake did reduce the seasonality of the region greater than just an increase in carbon dioxide, the addition of a large lake was unable to reduce the seasonality to the levels shown by the floral and faunal data.[citation needed]

Ocean heat transport

The transport of heat from the tropics to the poles, much like how ocean heat transport functions in modern times, was considered a possibility for the increased temperature and reduced seasonality for the poles.[79] With the increased sea surface temperatures and the increased temperature of the deep ocean water during the early Eocene, one common hypothesis was that due to these increases there would be a greater transport of heat from the tropics to the poles. Simulating these differences, the models produced lower heat transport due to the lower temperature gradients and were unsuccessful in producing an equable climate from only ocean heat transport.[citation needed]

Orbital parameters

While typically seen as a control on ice growth and seasonality, the orbital parameters were theorized as a possible control on continental temperatures and seasonality. Simulating the Eocene by using an ice free planet, eccentricity, obliquity, and precession were modified in different model runs to determine all the possible different scenarios that could occur and their effects on temperature. One particular case led to warmer winters and cooler summer by up to 30% in the North American continent, and it reduced the seasonal variation of temperature by up to 75%. While orbital parameters did not produce the warming at the poles, the parameters did show a great effect on seasonality and needed to be considered.[80]

Polar stratospheric clouds

Another method considered for producing the warm polar temperatures were polar stratospheric clouds.[81] Polar stratospheric clouds are clouds that occur in the lower stratosphere at very low temperatures. Polar stratospheric clouds have a great impact on radiative forcing. Due to their minimal albedo properties and their optical thickness, polar stratospheric clouds act similar to a greenhouse gas and trap outgoing longwave radiation. Different types of polar stratospheric clouds occur in the atmosphere: polar stratospheric clouds that are created due to interactions with nitric or sulfuric acid and water (Type I) or polar stratospheric clouds that are created with only water ice (Type II).[citation needed]

Methane is an important factor in the creation of the primary Type II polar stratospheric clouds that were created in the early Eocene.[58] Since water vapor is the only supporting substance used in Type II polar stratospheric clouds, the presence of water vapor in the lower stratosphere is necessary where in most situations the presence of water vapor in the lower stratosphere is rare. When methane is oxidized, a significant amount of water vapor is released. Another requirement for polar stratospheric clouds is cold temperatures to ensure condensation and cloud production. Polar stratospheric cloud production, since it requires the cold temperatures, is usually limited to nighttime and winter conditions. With this combination of wetter and colder conditions in the lower stratosphere, polar stratospheric clouds could have formed over wide areas in Polar Regions.[citation needed]

To test the polar stratospheric clouds effects on the Eocene climate, models were run comparing the effects of polar stratospheric clouds at the poles to an increase in atmospheric carbon dioxide.[81] The polar stratospheric clouds had a warming effect on the poles, increasing temperatures by up to 20 °C in the winter months. A multitude of feedbacks also occurred in the models due to the polar stratospheric clouds' presence. Any ice growth was slowed immensely and would lead to any present ice melting. Only the poles were affected with the change in temperature and the tropics were unaffected, which with an increase in atmospheric carbon dioxide would also cause the tropics to increase in temperature. Due to the warming of the troposphere from the increased greenhouse effect of the polar stratospheric clouds, the stratosphere would cool and would potentially increase the amount of polar stratospheric clouds.

While the polar stratospheric clouds could explain the reduction of the equator to pole temperature gradient and the increased temperatures at the poles during the early Eocene, there are a few drawbacks to maintaining polar stratospheric clouds for an extended period of time. Separate model runs were used to determine the sustainability of the polar stratospheric clouds.[82] It was determined that in order to maintain the lower stratospheric water vapor, methane would need to be continually released and sustained. In addition, the amounts of ice and condensation nuclei would need to be high in order for the polar stratospheric cloud to sustain itself and eventually expand.[citation needed]

Middle Eocene

The Eocene is not only known for containing the warmest period during the Cenozoic; it also marked the decline into an icehouse climate and the rapid expansion of the Antarctic ice sheet. The transition from a warming climate into a cooling climate began at around 49 Ma. Isotopes of carbon and oxygen indicate a shift to a global cooling climate.[83] The cause of the cooling has been attributed to a significant decrease of >2,000 ppm in atmospheric carbon dioxide concentrations.[54] One proposed cause of the reduction in carbon dioxide during the warming to cooling transition was the azolla event. With the equable climate during the early Eocene, warm temperatures in the arctic allowed for the growth of azolla, which is a floating aquatic fern, on the Arctic Ocean. The significantly high amounts of carbon dioxide also acted to facilitate azolla blooms across the Arctic Ocean. Compared to current carbon dioxide levels, these azolla grew rapidly in the enhanced carbon dioxide levels found in the early Eocene.[83] The isolation of the Arctic Ocean, evidenced by euxinia that occurred at this time,[84] led to stagnant waters and as the azolla sank to the sea floor, they became part of the sediments on the seabed and effectively sequestered the carbon by locking it out of the atmosphere for good. The ability for the azolla to sequester carbon is exceptional, and the enhanced burial of azolla could have had a significant effect on the world atmospheric carbon content and may have been the event to begin the transition into an ice house climate.[83] The azolla event could have led to a draw down of atmospheric carbon dioxide of up to 470 ppm. Assuming the carbon dioxide concentrations were at 900 ppmv prior to the Azolla Event they would have dropped to 430 ppmv, or 30 ppmv more than they are today, after the Azolla Event.[83] This cooling trend at the end of the EECO has also been proposed to have been caused by increased siliceous plankton productivity and marine carbon burial, which also helped draw carbon dioxide out of the atmosphere.[54] Cooling after this event, part of a trend known as the Middle-Late Eocene Cooling (MLEC),[85] continued due to continual decrease in atmospheric carbon dioxide from organic productivity and weathering from mountain building.[86] Many regions of the world became more arid and cold over the course of the stage, such as the Fushun Basin.[45] In East Asia, lake level changes were in sync with global sea level changes over the course of the MLEC.[87]

Global cooling continued until there was a major reversal from cooling to warming in the Bartonian. This warming event, signifying a sudden and temporary reversal of the cooling conditions, is known as the Middle Eocene Climatic Optimum (MECO).[88][89] At around 41.5 Ma, stable isotopic analysis of samples from Southern Ocean drilling sites indicated a warming event for 600,000 years.[86] A similar shift in carbon isotopes is known from the Northern Hemisphere in the Scaglia Limestones of Italy.[88] Oxygen isotope analysis showed a large negative change in the proportion of heavier oxygen isotopes to lighter oxygen isotopes, which indicates an increase in global temperatures.[90] The warming is considered to be primarily due to carbon dioxide increases, because carbon isotope signatures rule out major methane release during this short-term warming.[86] A sharp increase in atmospheric carbon dioxide was observed with a maximum of 4,000 ppm: the highest amount of atmospheric carbon dioxide detected during the Eocene.[91] Other studies suggest a more modest rise in carbon dioxide levels.[92] The increase in atmospheric carbon dioxide has also been hypothesised to have been driven by increased seafloor spreading rates and metamorphic decarbonation reactions between Australia and Antarctica and increased amounts of volcanism in the region. One possible cause of atmospheric carbon dioxide increase could have been a sudden increase due to metamorphic release due to continental drift and collision of India with Asia and the resulting formation of the Himalayas; however, data on the exact timing of metamorphic release of atmospheric carbon dioxide is not well resolved in the data.[86] Recent studies have mentioned, however, that the removal of the ocean between Asia and India could have released significant amounts of carbon dioxide.[91] Another hypothesis still implicates a diminished negative feedback of silicate weathering as a result of continental rocks having become less weatherable during the warm Early and Middle Eocene, allowing volcanically released carbon dioxide to persist in the atmosphere for longer.[93] Yet another explanation hypothesises that MECO warming was caused by the simultaneous occurrence of minima in both the 400 kyr and 2.4 Myr eccentricity cycles.[94] During the MECO, sea surface temperatures in the Tethys Ocean jumped to 32–36 °C,[95] and Tethyan seawater became more dysoxic.[96] A decline in carbonate accumulation at ocean depths of greater than three kilometres took place synchronously with the peak of the MECO, signifying ocean acidification took place in the deep ocean.[97] On top of that, MECO warming caused an increase in the respiration rates of pelagic heterotrophs, leading to a decreased proportion of primary productivity making its way down to the seafloor and causing a corresponding decline in populations of benthic foraminifera.[98] An abrupt decrease in lakewater salinity in western North America occurred during this warming interval.[99] This warming is short lived, as benthic oxygen isotope records indicate a return to cooling at ~40 Ma.[100]


Late Eocene

At the end of the MECO, the MLEC resumed.[85] Cooling and the carbon dioxide drawdown continued through the late Eocene and into the Eocene–Oligocene transition around 34 Ma.[101] The post-MECO cooling brought with it a major aridification trend in Asia,[102] enhanced by retreating seas.[103] A monsoonal climate remained predominant in East Asia.[104] The cooling during the initial stages of the opening of the Drake Passage ~38.5 Ma was not global, as evidenced by an absence of cooling in the North Atlantic.[105] During the cooling period, benthic oxygen isotopes show the possibility of ice creation and ice increase during this later cooling.[54] The end of the Eocene and beginning of the Oligocene is marked with the massive expansion of area of the Antarctic ice sheet that was a major step into the icehouse climate.[106] Multiple proxies, such as oxygen isotopes and alkenones, indicate that at the Eocene–Oligocene transition, the atmospheric carbon dioxide concentration had decreased to around 750–800 ppm, approximately twice that of present levels.[100][106] Along with the decrease of atmospheric carbon dioxide reducing the global temperature, orbital factors in ice creation can be seen with 100,000-year and 400,000-year fluctuations in benthic oxygen isotope records.[107] Another major contribution to the expansion of the ice sheet was the creation of the Antarctic Circumpolar Current.[108] The creation of the Antarctic circumpolar current would isolate the cold water around the Antarctic, which would reduce heat transport to the Antarctic[109] along with creating ocean gyres that result in the upwelling of colder bottom waters.[108] The issue with this hypothesis of the consideration of this being a factor for the Eocene-Oligocene transition is the timing of the creation of the circulation is uncertain.[110] For Drake Passage, sediments indicate the opening occurred ~41 Ma while tectonics indicate that this occurred ~32 Ma.[citation needed] Solar activity did not change significantly during the greenhouse-icehouse transition across the Eocene-Oligocene boundary.[111]

Flora

Eocene vegetation of the Clarno Nut Beds in John Day Fossil Beds National Monument was humid subtropical forest vegetation of high diversity dominated by angiosperms.
Heinrich Harder's reconstruction of Arsinoitherium shows it in an open landscape dominated by Poales

During the early-middle Eocene, forests covered most of the Earth including the poles. Tropical forests extended across much of modern Africa, South America, Central America, India, South-east Asia and China.  Paratropical forests grew over North America, Europe and Russia, with broad-leafed evergreen and broad-leafed deciduous forests at higher latitudes.[112]

Polar forests were quite extensive. Fossils and even preserved remains of trees such as swamp cypress and dawn redwood from the Eocene have been found on Ellesmere Island in the Arctic. Even at that time, Ellesmere Island was only a few degrees in latitude further south than it is today. Fossils of subtropical and even tropical trees and plants from the Eocene also have been found in Greenland and Alaska. Tropical rainforests grew as far north as northern North America and Europe.[citation needed]

Palm trees were growing as far north as Alaska and northern Europe during the early Eocene, although they became less abundant as the climate cooled.[113] Dawn redwoods were far more extensive as well.[114]

The earliest definitive Eucalyptus fossils were dated from 51.9 Ma, and were found in the Laguna del Hunco deposit in Chubut province in Argentina.[115]

Cooling began mid-period, and by the end of the Eocene continental interiors had begun to dry, with forests thinning considerably in some areas. The newly evolved grasses were still confined to river banks and lake shores, and had not yet expanded into plains and savannas.[citation needed]

The cooling also brought seasonal changes. Deciduous trees, better able to cope with large temperature changes, began to overtake evergreen tropical species.[116] By the end of the period, deciduous forests covered large parts of the northern continents, including North America, Eurasia and the Arctic, and rainforests held on only in equatorial South America, Africa, India and Australia.[citation needed]

Antarctica began the Eocene fringed with a warm temperate to sub-tropical rainforest. Pollen found in Prydz Bay from the Eocene suggest taiga forest existed there.[117] It became much colder as the period progressed; the heat-loving tropical flora was wiped out, and by the beginning of the Oligocene, the continent hosted deciduous forests and vast stretches of tundra.[citation needed]

Fauna

During the Eocene, plants and marine faunas became quite modern. Many modern bird orders first appeared in the Eocene. The Eocene oceans were warm and teeming with fish and other sea life.

Mammals

Cast of Uintatherium anceps skull, French National Museum of Natural History, Paris

The oldest known fossils of most of the modern mammal orders appear within a brief period during the early Eocene. At the beginning of the Eocene, several new mammal groups arrived in North America. These modern mammals, like artiodactyls, perissodactyls, and primates, had features like long, thin legs, feet, and hands capable of grasping, as well as differentiated teeth adapted for chewing. Dwarf forms reigned. All the members of the new mammal orders were small, under 10 kg; based on comparisons of tooth size, Eocene mammals were only 60% of the size of the primitive Palaeocene mammals that preceded them. They were also smaller than the mammals that followed them. It is assumed that the hot Eocene temperatures favored smaller animals that were better able to manage the heat.[118][119]

Rodents were widespread. East Asian rodent faunas declined in diversity when they shifted from ctenodactyloid-dominant to cricetid–dipodid-dominant after the MECO.[120]

Both groups of modern ungulates (hoofed animals) became prevalent because of a major radiation between Europe and North America, along with carnivorous ungulates like Mesonyx. Early forms of many other modern mammalian orders appeared, including horses (most notably the Eohippus), bats, proboscidians (elephants), primates, and rodents. Older primitive forms of mammals declined in variety and importance. Important Eocene land fauna fossil remains have been found in western North America, Europe, Patagonia, Egypt, and southeast Asia. Marine fauna are best known from South Asia and the southeast United States.[citation needed]

After the Paleocene–Eocene Thermal Maximum, members of the Equoidea arose in North America and Europe, giving rise to some of the earliest equids such as Sifrhippus and basal European equoids such as the palaeothere Hyracotherium.[121][122] Some of the later equoids were especially species-rich; Palaeotherium, ranging from small to very large in size, is known from as many as 16 species.[123][124]

Established large-sized mammals of the Eocene include the Uintatherium, Arsinoitherium, and brontotheres, in which the former two, unlike the latter, did not belong to ungulates but groups that became extinct shortly after their establishments.

Reconstruction of Andrewsarchus, Dinosaurier Museum Altmühltal, Germany

Large terrestrial mammalian predators had already existed since the Paleocene, but new forms now arose like Hyaenodon and Daphoenus (the earliest lineage of a once-successful predatory family known as bear dogs). Entelodonts meanwhile established themselves as some of the largest omnivores. The first nimravids, including Dinictis, established themselves as amongst the first feliforms to appear. Their groups became highly successful and continued to live past the Eocene.

Basilosaurus is a very well-known Eocene whale, but whales as a group had become very diverse during the Eocene, which is when the major transitions from being terrestrial to fully aquatic in cetaceans occurred. The first sirenians were evolving at this time, and would eventually evolve into the extant manatees and dugongs.

It is thought that millions of years after the Cretaceous-Paleogene extinction event, brain sizes of mammals now started to increase, "likely driven by a need for greater cognition in increasingly complex environments".[125][126][clarification needed]

Birds

Primobucco, an early relative of the roller

Eocene birds include some enigmatic groups with resemblances to modern forms, some of which continued from the Paleocene. Bird taxa of the Eocene include carnivorous psittaciforms, such as Messelasturidae, Halcyornithidae, large flightless forms such as Gastornis and Eleutherornis,[127] long legged falcon Masillaraptor, ancient galliforms such as Gallinuloides, putative rail relatives of the family Songziidae, various pseudotooth birds such as Gigantornis, the ibis relative Rhynchaeites, primitive swifts of the genus Aegialornis, and primitive penguins such as Archaeospheniscus and Inkayacu.[citation needed]

Many Eocene birds in Central Europe evolved tuberculate vertebrae as an adaptation against predation, with flightless birds facing low predation pressure during this time as a result.[128]

Reptiles

Reptile fossils from this time, such as fossils of pythons and turtles, are abundant.[129]

Arthropods

Several rich fossil insect faunas are known from the Eocene, notably the Baltic amber found mainly along the south coast of the Baltic Sea,[130] amber from the Paris Basin, France, the Fur Formation, Denmark, and the Bembridge Marls from the Isle of Wight, England. Insects found in Eocene deposits mostly belong to genera that exist today, though their range has often shifted since the Eocene. For instance the bibionid genus Plecia is common in fossil faunas from presently temperate areas, but only lives in the tropics and subtropics today.[citation needed] Platypleurin cicadas diversified during the Eocene.[131] Ostracods flourished in the oceans.[132]

Microbes

Calcareous nannoplankton were a prominent feature of Eocene marine ecosystems.[133]

See also

Notes

  1. ^ In Lyell's time, epochs were divided into periods. In modern geology, periods are divided into epochs.

References

  1. ^ Zachos, J. C.; Kump, L. R. (2005). "Carbon cycle feedbacks and the initiation of Antarctic glaciation in the earliest Oligocene". Global and Planetary Change. 47 (1): 51–66. Bibcode:2005GPC....47...51Z. doi:10.1016/j.gloplacha.2005.01.001.
  2. ^ "International Chronostratigraphic Chart" (PDF). International Commission on Stratigraphy. September 2023. Retrieved December 16, 2024.
  3. ^ a b c Aubry, Marie-Pierre; Ouda, Khaled; Dupuis, Christian; William A. Berggren; John A. Van Couvering; Working Group on the Paleocene/Eocene Boundary (2007). "The Global Standard Stratotype-section and Point (GSSP) for the base of the Eocene Series in the Dababiya section (Egypt)" (PDF). Episodes. 30 (4): 271–286. doi:10.18814/epiiugs/2007/v30i4/003.
  4. ^ Silva, Isabella; Jenkins, D. (September 1993). "Decision on the Eocene-Oligocene boundary stratotype" (PDF). Episodes. 16 (3): 379–382. doi:10.18814/epiiugs/1993/v16i3/002. Retrieved 13 December 2020.
  5. ^ Jones, Daniel (2003) [1917], Peter Roach; James Hartmann; Jane Setter (eds.), English Pronouncing Dictionary, Cambridge: Cambridge University Press, ISBN 3-12-539683-2
  6. ^ "Eocene". Merriam-Webster.com Dictionary. Merriam-Webster.
  7. ^ See:
  8. ^ "Eocene". Online Etymology Dictionary.
  9. ^ Burke, K. D.; Williams, J. W.; Chandler, M. A.; Haywood, A. M.; Lunt, D. J.; Otto-Bliesner, B. L. (2018). "Pliocene and Eocene provide best analogs for near-future climates". Proceedings of the National Academy of Sciences. 115 (52): 13288–13293. Bibcode:2018PNAS..11513288B. doi:10.1073/pnas.1809600115. PMC 6310841. PMID 30530685.
  10. ^ The extinction of the Hantkeninidae, a planktonic family of foraminifera became generally accepted as marking the Eocene-Oligocene boundary; in 1998 Massignano in Umbria, central Italy, was designated the Global Boundary Stratotype Section and Point (GSSP).
  11. ^ Lyell, C. (1833). Principles of Geology. Vol. 3. Geological Society of London. p. 378.
  12. ^ Phillips, J. (1840). "Palæozoic series". Penny Cyclopaedia of the Society for the Diffusion of Useful Knowledge. Vol. 17. London, England: Charles Knight and Co. pp. 153–154.
  13. ^ Hörnes, M. (1853). "Mittheilungen an Professor Bronn gerichtet" [Reports addressed to Professor Bronn]. Neues Jahrbuch für Mineralogie, Geognosie, Geologie und Petrefaktenkunde (in German): 806–810. hdl:2027/hvd.32044106271273.
  14. ^ George, T. N.; Harland, W. B. (1969). "Recommendations on stratigraphical usage". Proceedings of the Geological Society of London. 156 (1, 656): 139–166.
  15. ^ Odin, G. S.; Curry, D.; Hunziker, J. Z. (1978). "Radiometric dates from NW European glauconites and the Palaeogene time-scale". Journal of the Geological Society. 135 (5): 481–497. Bibcode:1978JGSoc.135..481O. doi:10.1144/gsjgs.135.5.0481. S2CID 129095948.
  16. ^ Knox, R. W. O.'B.; Pearson, P. N.; Barry, T. L. (2012). "Examining the case for the use of the Tertiary as a formal period or informal unit" (PDF). Proceedings of the Geologists' Association. 123 (3): 390–393. Bibcode:2012PrGA..123..390K. doi:10.1016/j.pgeola.2012.05.004.
  17. ^ a b Turner, S. K.; Hull, P. M.; Ridgwell, A. (2017). "A probabilistic assessment of the rapidity of PETM onset". Nature Communications. 8 (353): 353. Bibcode:2017NatCo...8..353K. doi:10.1038/s41467-017-00292-2. PMC 5572461. PMID 28842564.
  18. ^ Zhang, Q.; Willems, H.; Ding, L.; Xu, X. (2019). "Response of larger benthic foraminifera to the Paleocene–Eocene thermal maximum and the position of the Paleocene/Eocene boundary in the Tethyan shallow benthic zones: Evidence from south Tibet". Geological Society of America Bulletin. 131 (1–2): 84–98. Bibcode:2019GSAB..131...84Z. doi:10.1130/B31813.1. S2CID 134560025.
  19. ^ Kennet, J. P.; Stott, L. D. (1995). "Terminal Paleocene Mass Extinction in the Deep Sea: Association with Global Warming". Effects of Past Global Change on Life: Studies in Geophysics. National Academy of Sciences.
  20. ^ Winguth, C.; Thomas, E. (2012). "Global decline in ocean ventilation, oxygenation, and productivity during the Paleocene–Eocene Thermal Maximum: Implications for the benthic extinction". Geology. 40 (3): 263–266. Bibcode:2012Geo....40..263W. doi:10.1130/G32529.1.
  21. ^ Schmidt, G. A.; Shindell, D. T. (2003). "Atmospheric composition, radiative forcing, and climate change as a consequence of a massive methane release from gas hydrates". Paleoceanography and Paleoclimatology. 18 (1): n/a. Bibcode:2003PalOc..18.1004S. doi:10.1029/2002PA000757.
  22. ^ Bijl, Peter K.; Houben, Alexander J. P.; Schouten, Stefan; Bohaty, Steven M.; Sluijs, Appy; Reichart, Gert-Jan; Sinninghe Damsté, Jaap S.; Brinkhuis, Henk (2010-11-05). "Transient Middle Eocene Atmospheric CO 2 and Temperature Variations". Science. 330 (6005): 819–821. Bibcode:2010Sci...330..819B. doi:10.1126/science.1193654. hdl:1874/385803. ISSN 0036-8075. PMID 21051636. S2CID 206528256.
  23. ^ Hooker, J.J.; Collinson, M.E.; Sille, N.P. (2004). "Eocene-Oligocene mammalian faunal turnover in the Hampshire Basin, UK: calibration to the global time scale and the major cooling event" (PDF). Journal of the Geological Society. 161 (2): 161–172. Bibcode:2004JGSoc.161..161H. doi:10.1144/0016-764903-091. S2CID 140576090.
  24. ^ Rafferty, John P.; et al., eds. (2013). "Eocene Epoch". Britannica.
  25. ^ Wolfe, J.A. (1968). Paleogene Biostratigraphy of nonmarine rocks in King County, Washington (Report). Professional Paper. Vol. 571. United States Geological Survey. pp. 1–29. doi:10.3133/pp571.
  26. ^ Retallack, G.J.; Orr, W.N.; Prothero, D.R.; Duncan, R.A.; Kester, P.R.; Ambers, C.P. (2004). "Eocene–Oligocene extinction and paleoclimatic change near Eugene, Oregon". Geological Society of America Bulletin. 116 (7–8): 817–839. Bibcode:2004GSAB..116..817R. doi:10.1130/B25281.1.
  27. ^ Bijl, P. K.; Bendle, J. A. P.; Bohaty, S. M.; Pross, J.; Schouten, S.; Tauxe, L.; Stickley, C. E.; McKay, R. M.; Rohl, U.; Olney, M.; Sluijs, A.; Escutia, C.; Brinkhuis, H.; Klaus, A.; Fehr, A.; Williams, T.; Carr, S. A.; Dunbar, R. B.; Gonzalez, J. J.; Hayden, T. G.; Iwai, M.; Jimenez-Espejo, F. J.; Katsuki, K.; Kong, G. S.; Nakai, M.; Passchier, S.; Pekar, S. F.; Riesselman, C.; Sakai, T.; Shrivastava, P. K.; Sugisaki, S.; Tuo, S.; van de Flierdt, T.; Welsh, K.; Yamane, M. (2013-06-11). "Eocene cooling linked to early flow across the Tasmanian Gateway". Proceedings of the National Academy of Sciences of the United States of America. 110 (24): 9645–9650. Bibcode:2013PNAS..110.9645B. doi:10.1073/pnas.1220872110. PMC 3683727. PMID 23720311.
  28. ^ Huber, Matthew; Brinkhuis, Henk; Stickley, Catherine E.; Döös, Kristofer; Sluijs, Appy; Warnaar, Jeroen; Schellenberg, Stephen A.; Williams, Graham L. (December 2004). "Eocene circulation of the Southern Ocean: Was Antarctica kept warm by subtropical waters?: Did the East Australian Current Warm Antarctica?". Paleoceanography and Paleoclimatology. 19 (4). doi:10.1029/2004PA001014. hdl:1874/385798. S2CID 15123861.
  29. ^ Francis, J.E.; Marenssi, S.; Levy, R.; Hambrey, M.; Thorn, V.C.; Mohr, B.; Brinkhuis, H.; Warnaar, J.; Zachos, J.; Bohaty, S.; DeConto, R. (2008). "Chapter 8 From Greenhouse to Icehouse – The Eocene/Oligocene in Antarctica". Developments in Earth and Environmental Sciences. 8: 309–368. doi:10.1016/S1571-9197(08)00008-6. ISBN 9780444528476.
  30. ^ Torsvik, Trond H.; Cocks, L. Robin M. (2017). Earth history and palaeogeography. Cambridge, United Kingdom: Cambridge University Press. pp. 242, 251. ISBN 9781107105324.
  31. ^ English, Joseph M.; Johnston, Stephen T. (September 2004). "The Laramide Orogeny: What Were the Driving Forces?". International Geology Review. 46 (9): 833–838. Bibcode:2004IGRv...46..833E. doi:10.2747/0020-6814.46.9.833. S2CID 129901811.
  32. ^ Bird, Peter (October 1998). "Kinematic history of the Laramide orogeny in latitudes 35°-49°N, western United States". Tectonics. 17 (5): 780–801. Bibcode:1998Tecto..17..780B. doi:10.1029/98TC02698.
  33. ^ Fan, Majie; Constenius, Kurt N.; Phillips, Rachel F.; Dettman, David L. (17 March 2021). "Late Paleogene paleotopographic evolution of the northern Cordilleran orogenic front: Implications for demise of the orogen". Geological Society of America Bulletin. 133 (11–12): 2549–2566. doi:10.1130/B35919.1. ISSN 0016-7606. Retrieved 11 September 2023.
  34. ^ Bradley, W. H. (1930). "The varves and climate of the Green River epoch". U.S. Geological Survey Professional Paper. Professional Paper. 158-E. doi:10.3133/pp158E.
  35. ^ Grande, Lance (2001). "An Updated Review of the Fish Faunas from the Green River Formation, the World's Most Productive Freshwater Lagerstätten". Eocene Biodiversity. Topics in Geobiology. Vol. 18. pp. 1–38. doi:10.1007/978-1-4615-1271-4_1. ISBN 978-1-4613-5471-0.
  36. ^ Gohn, G. S.; Koeberl, C.; Miller, K. G.; Reimold, W. U.; Browning, J. V.; Cockell, C. S.; Horton, J. W.; Kenkmann, T.; Kulpecz, A. A.; Powars, D. S.; Sanford, W. E.; Voytek, M. A. (2008-06-27). "Deep Drilling into the Chesapeake Bay Impact Structure". Science. 320 (5884): 1740–1745. Bibcode:2008Sci...320.1740G. doi:10.1126/science.1158708. PMID 18583604. S2CID 27071176.
  37. ^ Poag, C. Wylie (2004). The Chesapeake Bay Crater : Geology and Geophysics of a Late Eocene Submarine Impact Structure. Berlin, Heidelberg: Springer Berlin Heidelberg. ISBN 9783642189005.
  38. ^ Frizon de Lamotte, Dominique; Raulin, Camille; Mouchot, Nicolas; Wrobel-Daveau, Jean-Christophe; Blanpied, Christian; Ringenbach, Jean-Claude (17 May 2011). "The southernmost margin of the Tethys realm during the Mesozoic and Cenozoic: Initial geometry and timing of the inversion processes". Tectonics. 30 (3): 1–22. Bibcode:2011Tecto..30.3002F. doi:10.1029/2010TC002691. ISSN 0278-7407. Retrieved 15 December 2023 – via Wiley Online Library.
  39. ^ Torsvik & Cocks 2017, pp. 242–245.
  40. ^ Benyamovskiy, Vladimir Naumovich (January 2012). "A high resolution lutetian-Bartonian planktonic foraminiferal zonation in the Crimean-Caucasus region of the northeastern Peri-Tethys". Austrian Journal of Earth Sciences. 105 (1): 117–128. Retrieved 24 September 2023.
  41. ^ Torsvik & Cocks 2017, pp. 251.
  42. ^ Denk, Thomas; Grímsson, Friðgeir; Zetter, Reinhard; Símonarson, Leifur A. (2011). "The Biogeographic History of Iceland – the North Atlantic Land Bridge Revisited". Late Cainozoic Floras of Iceland. Topics in Geobiology. Vol. 35. pp. 647–668. doi:10.1007/978-94-007-0372-8_12. ISBN 978-94-007-0371-1.
  43. ^ Licht, Alexis; Métais, Grégoire; Coster, Pauline; İbilioğlu, Deniz; Ocakoğlu, Faruk; Westerweel, Jan; Mueller, Megan; Campbell, Clay; Mattingly, Spencer; Wood, Melissa C.; Beard, K. Christopher (2022-03-01). "Balkanatolia: The insular mammalian biogeographic province that partly paved the way to the Grande Coupure". Earth-Science Reviews. 226: 103929. Bibcode:2022ESRv..22603929L. doi:10.1016/j.earscirev.2022.103929. ISSN 0012-8252.
  44. ^ CNRS (2022-03-01). "Balkanatolia: Forgotten Continent Discovered by Team of Paleontologists and Geologists". SciTechDaily. Retrieved 2023-02-06.
  45. ^ a b Xu, Sheng-Chuan; Liu, Zhao-Jun; Zhang, Pu; Boak, Jeremy M.; Liu, Rong; Meng, Qing-Tao (1 October 2016). "Characterization of depositional conditions for lacustrine oil shales in the Eocene Jijuntun Formation, Fushun Basin, NE China". International Journal of Coal Geology. 167: 10–30. Bibcode:2016IJCG..167...10X. doi:10.1016/j.coal.2016.09.004. Retrieved 24 September 2023.
  46. ^ Ding, Huixia; Zhang, Zeming; Dong, Xin; Tian, Zuolin; Xiang, Hua; Mu, Hongchen; Gou, Zhengbin; Shui, Xinfang; Li, Wangchao; Mao, Lingjuan (February 2016). "Early Eocene ( c . 50 Ma) collision of the Indian and Asian continents: Constraints from the North Himalayan metamorphic rocks, southeastern Tibet". Earth and Planetary Science Letters. 435: 64–73. Bibcode:2016E&PSL.435...64D. doi:10.1016/j.epsl.2015.12.006.
  47. ^ Bouilhol, Pierre; Jagoutz, Oliver; Hanchar, John M.; Dudas, Francis O. (15 March 2013). "Dating the India–Eurasia collision through arc magmatic records". Earth and Planetary Science Letters. 366: 163–175. Bibcode:2013E&PSL.366..163B. doi:10.1016/j.epsl.2013.01.023. Retrieved 25 December 2022.
  48. ^ Rennie, Victoria C. F.; Paris, Guillaume; Sessions, Alex L.; Abramovich, Sigal; Turchyn, Alexandra V.; Adkins, Jess F. (13 August 2018). "Cenozoic record of δ34S in foraminiferal calcite implies an early Eocene shift to deep-ocean sulfide burial". Nature Geoscience. 11 (10): 761–765. Bibcode:2018NatGe..11..761R. doi:10.1038/s41561-018-0200-y. S2CID 134126659. Retrieved 26 December 2022.
  49. ^ Cramwinckel, Margot J.; Huber, Matthew; Kocken, Ilja J.; Agnini, Claudia; Bijl, Peter K.; Bohaty, Steven M.; Frieling, Joost; Goldner, Aaron; Hilgen, Frederik J.; Kip, Elizabeth L.; Peterse, Francien; Van der Ploeg, Robin; Röhl, Ursula; Schouten, Stefan; Sluijs, Appy (2 July 2018). "Synchronous tropical and polar temperature evolution in the Eocene". Nature. 559 (7714): 382–386. Bibcode:2018Natur.559..382C. doi:10.1038/s41586-018-0272-2. hdl:1874/366626. PMID 29967546. S2CID 49556944. Retrieved 21 September 2022.
  50. ^ West, Christopher K.; Greenwood, David R.; Reichgelt, Tammo; Lowe, Alexander J.; Vachon, Janelle M.; Basinger, James F. (4 August 2020). "Paleobotanical proxies for early Eocene climates and ecosystems in northern North America from middle to high latitudes". Climate of the Past. 16 (4): 1387–1410. Bibcode:2020CliPa..16.1387W. doi:10.5194/cp-16-1387-2020. S2CID 236890548. Retrieved 8 January 2023.
  51. ^ Li, Fengyuan; Li, Shuqiang (2018-10-01). "Paleocene–Eocene and Plio–Pleistocene sea-level changes as "species pumps" in Southeast Asia: Evidence from Althepus spiders". Molecular Phylogenetics and Evolution. 127: 545–555. Bibcode:2018MolPE.127..545L. doi:10.1016/j.ympev.2018.05.014. ISSN 1055-7903. PMID 29778723. S2CID 29155499.
  52. ^ Galeotti, Simone; Deconto, Robert; Naish, Timothy; Stocchi, Paolo; Florindo, Fabio; Pagani, Mark; Barrett, Peter; Bohaty, Steven M.; Lanci, Luca; Pollard, David; Sandroni, Sonia; Talarico, Franco M.; Zachos, James C. (10 March 2016). "Antarctic Ice Sheet variability across the Eocene-Oligocene boundary climate transition". Science. 352 (6281): 76–80. Bibcode:2016Sci...352...76G. doi:10.1126/science.aab0669. PMID 27034370. S2CID 24154493. Retrieved 17 March 2023.
  53. ^ Bowen, J. G.; Zachos, J. C. (2010). "Rapid carbon sequestration at the termination of the Palaeocene-Eocene Thermal Maximum". Nature Geoscience. 3 (12): 866–869. Bibcode:2010NatGe...3..866B. doi:10.1038/ngeo1014.
  54. ^ a b c d e Pearson, P. N.; Palmer, M. R. (2000). "Atmospheric carbon dioxide concentrations over the past 60 million years". Nature. 406 (6797): 695–699. Bibcode:2000Natur.406..695P. doi:10.1038/35021000. PMID 10963587. S2CID 205008176.
  55. ^ Goudsmit-Harzevoort, Barbara; Lansu, Angelique; Baatsen, Michiel L. J.; von der Heydt, Anna S.; de Winter, Niels J.; Zhang, Yurui; Abe-Ouchi, Ayako; de Boer, Agatha; Chan, Wing-Le; Donnadieu, Yannick; Hutchinson, David K.; Knorr, Gregor; Ladant, Jean-Baptiste; Morozova, Polina; Niezgodzki, Igor (17 February 2023). "The Relationship Between the Global Mean Deep-Sea and Surface Temperature During the Early Eocene". Paleoceanography and Paleoclimatology. 38 (3): 1–18. Bibcode:2023PaPa...38.4532G. doi:10.1029/2022PA004532. ISSN 2572-4517. Retrieved 24 September 2023.
  56. ^ Royer, Dana L.; Wing, Scott L.; Beerling, David J.; Jolley, David W.; Koch, Paul L.; Hickey1, Leo J.; Berner, Robert A. (22 June 2001). "Paleobotanical Evidence for Near Present-Day Levels of Atmospheric CO2 During Part of the Tertiary". Science. 292 (5525): 2310–2313. Bibcode:2001Sci...292.2310R. doi:10.1126/science.292.5525.2310. PMID 11423657.{{cite journal}}: CS1 maint: numeric names: authors list (link)
  57. ^ Forster, P.; Storelvmo, T.; Armour, K.; Collins, W. (2021). "Chapter 7: The Earth's energy budget, climate feedbacks, and climate sensitivity" (PDF). IPCC AR6 WG1 2021.
  58. ^ a b Sloan, L. C.; Walker, C. G.; Moore, T. C. Jr.; Rea, D. K.; Zachos, J. C. (1992). "Possible methane-induced polar warming in the early Eocene". Nature. 357 (6376): 1129–1131. Bibcode:1992Natur.357..320S. doi:10.1038/357320a0. hdl:2027.42/62963. PMID 11536496. S2CID 4348331.
  59. ^ O'Neil, Dennis (2012). "The First Primates". anthro.palomar.edu. Archived from the original on 2015-12-25. Retrieved 2014-05-13.
  60. ^ Galeotti, S.; Krishnan, Srinath; Pagani, Mark; Lanci, Luca; Gaudio, Alberto; Zachos, James C.; Monechi, Simonetta; Morelli, Guia; Lourens, Lucas (2010). "Orbital chronology of Early Eocene hyperthermals from the Contessa Road section, central Italy". Earth and Planetary Science Letters. 290 (1–2): 192–200. Bibcode:2010E&PSL.290..192G. doi:10.1016/j.epsl.2009.12.021.
  61. ^ Slotnick, Benjamin S.; Cickens, Gerald R.; Nicolo, Micah J.; Hollis, Christopher J.; Crampton, James S.; Zachos, James C.; Sluijs, Appy (11 May 2012). "Large-Amplitude Variations in Carbon Cycling and Terrestrial Weathering during the Latest Paleocene and Earliest Eocene: The Record at Mead Stream, New Zealand". The Journal of Geology. 120 (5): 487–505. Bibcode:2012JG....120..487S. doi:10.1086/666743. hdl:1911/88269. S2CID 55327247. Retrieved 23 June 2023.
  62. ^ Zachos, James C.; McCarren, Heather; Murphy, Brandon; Röhl, Ursula; Westerhold, Thomas (15 October 2010). "Tempo and scale of late Paleocene and early Eocene carbon isotope cycles: Implications for the origin of hyperthermals". Earth and Planetary Science Letters. 299 (1–2): 242–249. Bibcode:2010E&PSL.299..242Z. doi:10.1016/j.epsl.2010.09.004. Retrieved 23 June 2023.
  63. ^ Turner, Sandra Kirtland; Sexton, Philip D.; Charles, Christopher D.; Norris, Richard D. (7 September 2014). "Persistence of carbon release events through the peak of early Eocene global warmth". Nature Geoscience. 7 (1): 748–751. Bibcode:2014NatGe...7..748K. doi:10.1038/ngeo2240. Retrieved 22 June 2023.
  64. ^ Sexton, Philip F.; Norris, Richard D.; Wilson, Paul A.; Pälike, Heiko; Westerhold, Thomas; Röhl, Ursula; Bolton, Clara T.; Gibbs, Samantha (16 March 2011). "Eocene global warming events driven by ventilation of oceanic dissolved organic carbon". Nature. 471 (7338): 349–352. Bibcode:2011Natur.471..349S. doi:10.1038/nature09826. PMID 21412336. S2CID 26081460. Retrieved 22 June 2023.
  65. ^ Yasukawa, Kazutaka; Nakamura, Kentaro; Fujinaga, Koijiro; Ikehara, Minoru; Kato, Yasuhiro (12 September 2017). "Earth system feedback statistically extracted from the Indian Ocean deep-sea sediments recording Eocene hyperthermals". Scientific Reports. 7 (1): 11304. Bibcode:2017NatSR...711304Y. doi:10.1038/s41598-017-11470-z. PMC 5595800. PMID 28900142.
  66. ^ Khanolkar, Sonal; Saraswati, Pratul Kumar (1 July 2015). "Ecological Response of Shallow-Marine Foraminifera to Early Eocene Warming in Equatorial India". Journal of Foraminiferal Research. 45 (3): 293–304. Bibcode:2015JForR..45..293K. doi:10.2113/gsjfr.45.3.293. Retrieved 23 June 2023.
  67. ^ Stassen, Peter; Steurbaut, Etienne; Morsi, Abdel-Mohsen; Schulte, Peter; Speijer, Robert (1 May 2021). "Biotic impact of Eocene thermal maximum 2 in a shelf setting (Dababiya, Egypt)". Austrian Journal of Earth Sciences. 109: 154–160. Retrieved 23 June 2023.
  68. ^ Reinhardt, Lutz; Von Gosen, Werner; Lückge, Andreas; Blumenberg, Martin; Galloway, Jennifer M.; West, Christopher K.; Sudermann, Markus; Dolezych, Martina (7 January 2022). "Geochemical indications for the Paleocene-Eocene Thermal Maximum (PETM) and Eocene Thermal Maximum 2 (ETM-2) hyperthermals in terrestrial sediments of the Canadian Arctic". Geosphere. 18 (1): 327–349. Bibcode:2022Geosp..18..327R. doi:10.1130/GES02398.1. Retrieved 23 June 2023.
  69. ^ Abels, Hemmo A.; Clyde, William C.; Gingerich, Philip D.; Hilgen, Frederik J.; Fricke, Henry C.; Bowen, Gabriel J.; Lourens, Lucas J. (1 April 2012). "Terrestrial carbon isotope excursions and biotic change during Palaeogene hyperthermals". Nature Geoscience. 5 (5): 326–329. Bibcode:2012NatGe...5..326A. doi:10.1038/ngeo1427. Retrieved 22 June 2023.
  70. ^ Slotnick, B. S.; Dickens, G. R.; Hollis, C. J.; Crampton, J. S.; Strong, C. Percy; Phillips, A. (17 Sep 2015). "The onset of the Early Eocene Climatic Optimum at Branch Stream, Clarence River valley, New Zealand". New Zealand Journal of Geology and Geophysics. 58 (3): 262–280. Bibcode:2015NZJGG..58..262S. doi:10.1080/00288306.2015.1063514. S2CID 130982094.
  71. ^ Crouch, E. M.; Shepherd, C. L.; Morgans, H. E. G.; Naafs, B. D. A.; Dallanave, E.; Phillips, A.; Hollis, C. J.; Pancost, R. D. (1 January 2020). "Climatic and environmental changes across the early Eocene climatic optimum at mid-Waipara River, Canterbury Basin, New Zealand". Earth-Science Reviews. 200: 102961. Bibcode:2020ESRv..20002961C. doi:10.1016/j.earscirev.2019.102961. hdl:1983/aedc04cc-bba8-44c6-8f9d-ba398bb24607. ISSN 0012-8252. Retrieved 11 September 2023.
  72. ^ Sloan, L. C.; Rea, D. K. (1995). "Atmospheric carbon dioxide and early Eocene climate: a general circulation modeling sensitivity study". Palaeogeography, Palaeoclimatology, Palaeoecology. 119 (3–4): 275–292. doi:10.1016/0031-0182(95)00012-7.
  73. ^ a b c Huber, M. (2009). "Snakes tell a torrid tale". Nature. 457 (7230): 669–671. doi:10.1038/457669a. PMID 19194439. S2CID 205044111.
  74. ^ a b c Huber, M.; Caballero, R. (2011). "The early Eocene equable climate problem revisited". Climate of the Past. 7 (2): 603–633. Bibcode:2011CliPa...7..603H. doi:10.5194/cp-7-603-2011.
  75. ^ Grossman, Ethan L.; Joachimski, Michael M. (27 May 2022). "Ocean temperatures through the Phanerozoic reassessed". Scientific Reports. 12 (1): 8938. Bibcode:2022NatSR..12.8938G. doi:10.1038/s41598-022-11493-1. PMC 9142518. PMID 35624298. S2CID 249128273.
  76. ^ Evans, David; Sagoo, Navjit; Renema, Willem; Cotton, Laura J.; Müller, Wolfgang; Todd, Jonathan A.; Saraswati, Pratul Kumar; Stassen, Peter; Ziegler, Martin; Pearson, Paul N.; Valdes, Paul J.; Affek, Hagit P. (22 January 2018). "Eocene greenhouse climate revealed by coupled clumped isotope-Mg/Ca thermometry". Proceedings of the National Academy of Sciences of the United States of America. 115 (6): 1174–1179. Bibcode:2018PNAS..115.1174E. doi:10.1073/pnas.1714744115. PMC 5819407. PMID 29358374.
  77. ^ Sloan, L. C.; Barron, E. J. (1990). ""Equable" climates during Earth history?". Geology. 18 (6): 489–492. Bibcode:1990Geo....18..489C. doi:10.1130/0091-7613(1990)018<0489:ecdeh>2.3.co;2.
  78. ^ Sloan, L. C. (1994). "Equable climates during the early Eocene: Significance of regional paleogeography for North American climate". Geology. 22 (10): 881–884. Bibcode:1994Geo....22..881C. doi:10.1130/0091-7613(1994)022<0881:ecdtee>2.3.co;2.
  79. ^ Huber, M.; Sloan, L. C. (2001). "Heat transport, deeps waters, and thermal gradients: Coupled simulation of an Eocene Greenhouse Climate". Geophysical Research Letters. 28 (18): 3481–3484. Bibcode:2001GeoRL..28.3481H. doi:10.1029/2001GL012943.
  80. ^ Sloan, L. C.; Morrill, C. (1998). "Orbital forcing and Eocene continental temperatures". Palaeogeography, Palaeoclimatology, Palaeoecology. 144 (1–2): 21–35. Bibcode:1998PPP...144...21S. doi:10.1016/s0031-0182(98)00091-1.
  81. ^ a b Sloan, L. C.; Pollard, D. (1998). "Polar stratospheric clouds: A high latitude warming mechanism in an ancient greenhouse world". Geophysical Research Letters. 25 (18): 3517–3520. Bibcode:1998GeoRL..25.3517S. doi:10.1029/98gl02492. S2CID 128392518.
  82. ^ Kirk-Davidoff, D. B.; Lamarque, J. F. (2008). "Maintenance of polar stratospheric clouds in a moist stratosphere". Climate of the Past. 4 (1): 69–78. Bibcode:2008CliPa...4...69K. doi:10.5194/cp-4-69-2008.
  83. ^ a b c d Speelman, E. N.; Van Kempen, M. M. L.; Barke, J.; Brinkhuis, H.; Reichart, G. J.; Smolders, A. J. P.; Roelofs, J. G. M.; Sangiorgi, F.; De Leeuw, J. W.; Lotter, A. F.; Sinninghe Damsté, J. S. (27 March 2009). "The Eocene Arctic Azolla bloom: environmental conditions, productivity, and carbon drawdown". Geobiology. 7 (2): 155–170. Bibcode:2009Gbio....7..155S. doi:10.1111/j.1472-4669.2009.00195.x. PMID 19323694. S2CID 13206343.
  84. ^ Ogawa, Yusuke; Takahashi, Kozo; Yamanaka, Toshiro; Onodera, Jonaotaro (30 July 2009). "Significance of euxinic condition in the middle Eocene paleo-Arctic basin: A geochemical study on the IODP Arctic Coring Expedition 302 sediments". Earth and Planetary Science Letters. 285 (1–2): 190–197. Bibcode:2009E&PSL.285..190O. doi:10.1016/j.epsl.2009.06.011. Retrieved 6 April 2023.
  85. ^ a b Scotese, Christopher Robert; Song, Haijun; Mills, Benjamin J.W.; van der Meer, Douwe G. (April 2021). "Phanerozoic paleotemperatures: The earth's changing climate during the last 540 million years". Earth-Science Reviews. 215: 103503. Bibcode:2021ESRv..21503503S. doi:10.1016/j.earscirev.2021.103503. Retrieved 24 September 2023.
  86. ^ a b c d Bohaty, S. M.; Zachos, J. C. (2003). "Significant Southern Ocean warming event in the late middle Eocene". Geology. 31 (11): 1017–1020. Bibcode:2003Geo....31.1017B. doi:10.1130/g19800.1.
  87. ^ Ma, Yiquan; Fan, Majie; Li, Mingsong; Ogg, James G.; Zhang, Chen; Feng, Jun; Zhou, Chunhua; Liu, Xiaofeng; Lu, Yongchao; Liu, Huimin; Eldrett, James S.; Ma, Chao (15 January 2023). "East Asian lake hydrology modulated by global sea-level variations in the Eocene warmhouse". Earth and Planetary Science Letters. 602: 117925. Bibcode:2023E&PSL.60217925M. doi:10.1016/j.epsl.2022.117925. ISSN 0012-821X. Retrieved 24 September 2023.
  88. ^ a b Jovane, Luigi; Florindo, Fabio; Coccioni, Rodolfo; Marsili, Andrea; Monechi, Simonetta; Roberts, Andrew P.; Sprovieri, Mario (1 March 2007). "The middle Eocene climatic optimum event in the Contessa Highway section, Umbrian Apennines, Italy". Geological Society of America Bulletin. 119 (3–4): 413–427. Bibcode:2007GSAB..119..413J. doi:10.1130/B25917.1. Retrieved 18 May 2023.
  89. ^ Shi, Juye; Jin, Zhijun; Liu, Quanyou; Zhang, Rui; Huang, Zhenkai (March 2019). "Cyclostratigraphy and astronomical tuning of the middle eocene terrestrial successions in the Bohai Bay Basin, Eastern China". Global and Planetary Change. 174: 115–126. Bibcode:2019GPC...174..115S. doi:10.1016/j.gloplacha.2019.01.001. S2CID 135265513. Retrieved 3 January 2023.
  90. ^ Edgar, Kirsty M.; Wilson, P. A.; Sexton, P. F.; Gibbs, S. J.; Roberts, Andrew P.; Norris, R. D. (20 November 2010). "New biostratigraphic, magnetostratigraphic and isotopic insights into the Middle Eocene Climatic Optimum in low latitudes". Palaeogeography, Palaeoclimatology, Palaeoecology. 297 (3–4): 670–682. Bibcode:2010PPP...297..670E. doi:10.1016/j.palaeo.2010.09.016. Retrieved 18 May 2023.
  91. ^ a b Pearson, P. N. (2010). "Increased Atmospheric CO2 During the Middle Eocene". Science. 330 (6005): 763–764. Bibcode:2010Sci...330..763P. doi:10.1126/science.1197894. PMID 21051620. S2CID 20253252.
  92. ^ Henehan, Michael J.; Edgar, Kirsty M.; Foster, Gavin L.; Penman, Donald E.; Hull, Pincelli M.; Greenop, Rosanna; Anagnostou, Eleni; Pearson, Paul N. (9 March 2020). "Revisiting the Middle Eocene Climatic Optimum "Carbon Cycle Conundrum" With New Estimates of Atmospheric pCO2 From Boron Isotopes". Paleoceanography and Paleoclimatology. 35 (6). Bibcode:2020PaPa...35.3713H. doi:10.1029/2019PA003713. S2CID 216309293. Retrieved 18 May 2023.
  93. ^ Van der Ploeg, Robin; Selby, David; Cramwinckel, Margot J.; Li, Yang; Bohaty, Steven M.; Middelburg, Jack J.; Sluijs, Appy (23 July 2018). "Middle Eocene greenhouse warming facilitated by diminished weathering feedback". Nature Communications. 9 (1): 2877. Bibcode:2018NatCo...9.2877V. doi:10.1038/s41467-018-05104-9. PMC 6056486. PMID 30038400.
  94. ^ Giorgioni, Martino; Jovane, Luigi; Rego, Eric S.; Rodelli, Daniel; Frontalini, Fabrizio; Coccioni, Rodolfo; Catanzariti, Rita; Özcan, Ercan (27 June 2019). "Carbon cycle instability and orbital forcing during the Middle Eocene Climatic Optimum". Scientific Reports. 9 (1): 9357. Bibcode:2019NatSR...9.9357G. doi:10.1038/s41598-019-45763-2. PMC 6597698. PMID 31249387.
  95. ^ Cramwinckel, Margot J.; Van der Ploeg, Robin; Van Helmond, Niels A. G. M.; Waarlo, Niels; Agnini, Claudia; Bijl, Peter K.; Van der Boon, Annique; Brinkhuis, Henk; Frieling, Joost; Krijgsman, Wout; Mather, Tamsin A.; Middelburg, Jack J.; Peterse, Francien; Slomp, Caroline P.; Sluijs, Appy (1 September 2022). "Deoxygenation and organic carbon sequestration in the Tethyan realm associated with the middle Eocene climatic optimum". Geological Society of America Bulletin. 135 (5–6): 1280–1296. doi:10.1130/B36280.1. S2CID 252033074. Retrieved 18 May 2023.
  96. ^ Spofforth, D. J. A.; Agnini, C.; Pälike, H.; Rio, D.; Fornaciari, E.; Giusberi, L.; Luciani, V.; Lanci, L.; Muttoni, G. (24 August 2010). "Organic carbon burial following the middle Eocene climatic optimum in the central western Tethys". Paleoceanography and Paleoclimatology. 25 (3): 1–11. Bibcode:2010PalOc..25.3210S. doi:10.1029/2009PA001738. Retrieved 18 May 2023.
  97. ^ Bohaty, Steven M.; Zachos, James C.; Florindo, Fabio; Delaney, Margaret L. (9 May 2009). "Coupled greenhouse warming and deep-sea acidification in the middle Eocene". Paleoceanography and Paleoclimatology. 24 (2): 1–16. Bibcode:2009PalOc..24.2207B. doi:10.1029/2008PA001676. Retrieved 20 May 2023.
  98. ^ Boscolo Galazzo, Flavia; Thomas, Ellen; Giusberti, Luca (1 January 2015). "Benthic foraminiferal response to the Middle Eocene Climatic Optimum (MECO) in the South-Eastern Atlantic (ODP Site 1263)". Palaeogeography, Palaeoclimatology, Palaeoecology. 417: 432–444. Bibcode:2015PPP...417..432B. doi:10.1016/j.palaeo.2014.10.004. Retrieved 19 November 2023.
  99. ^ Mulch, Andreas; Chamberlain, C. P.; Cosca, Michael A.; Teyssier, Christian; Methner, Katharina; Hren, Michael T.; Graham, Stephan A. (April 2015). "Rapid change in high-elevation precipitation patterns of western North America during the Middle Eocene Climatic Optimum (MECO)". American Journal of Science. 315 (4): 317–336. Bibcode:2015AmJS..315..317M. doi:10.2475/04.2015.02. S2CID 129918182. Archived from the original on 19 May 2023. Retrieved 18 May 2023.
  100. ^ a b Pagani, M.; Zachos, J. C.; Freeman, Katherine H.; Tipple, Brett; Bohaty, Stephen (2005). "Marked Decline in Atmospheric Carbon Dioxide Concentrations During the Paleogene". Science. 309 (5734): 600–603. Bibcode:2005Sci...309..600P. doi:10.1126/science.1110063. PMID 15961630. S2CID 20277445.
  101. ^ Cappelli, C.; Bown, P. R.; Westerhold, T.; Bohaty, S. M.; De Riu, M.; Loba, V.; Yamamoto, Y.; Agnini, C. (15 November 2019). "The Early to Middle Eocene Transition: An Integrated Calcareous Nannofossil and Stable Isotope Record From the Northwest Atlantic Ocean (Integrated Ocean Drilling Program Site U1410)". Paleoceanography and Paleoclimatology. 34 (12): 1913–1930. Bibcode:2019PaPa...34.1913C. doi:10.1029/2019PA003686. S2CID 210245165. Retrieved 17 March 2023.
  102. ^ Bosboom, Roderic E.; Abels, Hemmo A.; Hoorn, Carina; Van den Berg, Bas C. J.; Guo, Zhaojie; Dupont-Nivet, Guillaume (1 March 2014). "Aridification in continental Asia after the Middle Eocene Climatic Optimum (MECO)". Earth and Planetary Science Letters. 389: 34–42. Bibcode:2014E&PSL.389...34B. doi:10.1016/j.epsl.2013.12.014. Retrieved 18 May 2023.
  103. ^ Bosboom, Roderic; Dupont-Nivet, Guillaume; Grothe, Arjen; Brinkhuis, Henk; Villa, Giuliana; Mandic, Oleg; Stoica, Marius; Kouwenhoven, Tanja; Huang, Wentao; Yang, Wei; Guo, ZhaoJie (1 June 2014). "Timing, cause and impact of the late Eocene stepwise sea retreat from the Tarim Basin (west China)". Palaeogeography, Palaeoclimatology, Palaeoecology. 403: 101–118. Bibcode:2014PPP...403..101B. doi:10.1016/j.palaeo.2014.03.035. ISSN 0031-0182. Retrieved 26 December 2023 – via Elsevier Science Direct.
  104. ^ Li, Qijia; Utescher, Torsten; Liu, Yusheng (Christopher); Ferguson, David; Jia, Hui; Quan, Cheng (1 September 2022). "Monsoonal climate of East Asia in Eocene times inferred from an analysis of plant functional types". Palaeogeography, Palaeoclimatology, Palaeoecology. 601: 111138. Bibcode:2022PPP...60111138L. doi:10.1016/j.palaeo.2022.111138. Retrieved 20 July 2024 – via Elsevier Science Direct.
  105. ^ Borrelli, Chiara; Cramer, Benjamin S.; Katz, Miriam E. (27 March 2014). "Bipolar Atlantic deepwater circulation in the middle-late Eocene: Effects of Southern Ocean gateway openings". Paleoceanography and Paleoclimatology. 29 (4): 308–327. Bibcode:2014PalOc..29..308B. doi:10.1002/2012PA002444. Retrieved 7 April 2023.
  106. ^ a b Lear, C. H.; Bailey, T. R.; Pearson, P.N.; Coxall, H. K.; Rosenthal, Y. (2008). "Cooling and ice growth across the Eocene-Oligocene transition". Geology. 36 (3): 251–254. Bibcode:2008Geo....36..251L. doi:10.1130/g24584a.1.
  107. ^ Diester-Haass, L.; Zahn, R. (1996). "Eocene-Oligocene transition in the Southern Ocean: History of water mass circulation and biological productivity". Geology. 24 (2): 163–166. Bibcode:1996Geo....24..163D. doi:10.1130/0091-7613(1996)024<0163:eotits>2.3.co;2.
  108. ^ a b Barker, P. F.; Thomas, E. (2004). "Origin, signature and palaeoclimatic influence of the Antarctic Circumpolar Current". Earth-Science Reviews. 66 (1–2): 143–162. Bibcode:2004ESRv...66..143B. doi:10.1016/j.earscirev.2003.10.003.
  109. ^ Huber, M.; Nof, D. (2006). "The ocean circulation in the southern hemisphere and its climatic impacts in the Eocene". Palaeogeography, Palaeoclimatology, Palaeoecology. 231 (1–2): 9–28. Bibcode:2006PPP...231....9H. doi:10.1016/j.palaeo.2005.07.037.
  110. ^ Barker, P. F.; Filippelli, Gabriel M.; Florindo, Fabio; Martin, Ellen E.; Scher, Howard D. (2007). "Onset and Role of the Antarctic Circumpolar Current" (PDF). Topical Studies in Oceanography. 54 (21–22): 2388–2398. Bibcode:2007DSRII..54.2388B. doi:10.1016/j.dsr2.2007.07.028.
  111. ^ Shi, Juye; Jin, Zhijun; Liu, Quanyou; Fan, Tailiang; Gao, Zhiqian (1 October 2021). "Sunspot cycles recorded in Eocene lacustrine fine-grained sedimentary rocks in the Bohai Bay Basin, eastern China". Global and Planetary Change. 205: 103614. Bibcode:2021GPC...20503614S. doi:10.1016/j.gloplacha.2021.103614. ISSN 0921-8181. Retrieved 26 December 2023 – via Elsevier Science Direct.
  112. ^ Briggs, John (1995). Global Biogeography. Elsevier. p116 Fig 40. ISBN 0-444-88297-9.
  113. ^ Wing, Scott L.; Greenwood, David R. (28 August 1993). "Fossils and fossil climate: the case for equable continental interiors in the Eocene". Philosophical Transactions of the Royal Society of London. Series B: Biological Sciences. 341 (1297): 243–252. doi:10.1098/rstb.1993.0109.
  114. ^ Jahren, A. Hope (28 August 1993). "Fossils and fossil climate: the case for equable continental interiors in the Eocene". Philosophical Transactions of the Royal Society of London. Series B: Biological Sciences. 341 (1297): 243–252. doi:10.1098/rstb.1993.0109.
  115. ^ Gandolfo, MA; Hermsen, EJ; Zamaloa, MC; Nixon, KC; González, CC (2011). "Oldest Known Eucalyptus Macrofossils Are from South America". PLOS ONE. 6 (6): e21084. Bibcode:2011PLoSO...621084G. doi:10.1371/journal.pone.0021084. PMC 3125177. PMID 21738605.
  116. ^ Briggs 1995, p. 118.
  117. ^ Bender, Michael (2013). Paleoclimate. Princeton University Press. p. 108.
  118. ^ Abigail R. D’Ambrosia et al. (2017) Repetitive mammalian dwarfing during ancient greenhouse warming events.Sci. Adv.3,e1601430.DOI:10.1126/sciadv.1601430
  119. ^ Katherina B. Searing et al. (2023) Melting climates shrink North American small mammals. 120 (50) e2310855120 https://doi.org/10.1073/pnas.2310855120.
  120. ^ Li, Qian; Li, Qi; Xu, Rancheng; Wang, Yuanqing (7 September 2022). "Rodent faunas, their paleogeographic pattern, and responses to climate changes from the early Eocene to the early Oligocene in Asia". Frontiers in Ecology and Evolution. 10. doi:10.3389/fevo.2022.955779. ISSN 2296-701X.
  121. ^ Secord, Ross; BLoch, Jonathan I.; Chester, Stephen G. B.; Boter, Doug M.; Wood, Aaron R.; Wing, Scott L.; Kraus, Mary J.; McInerney, Francesca A.; Krigbaum, John (2012). "Evolution of the Earliest Horses Driven by Climate Change in the Paleocene-Eocene Thermal Maximum". Nature. 335 (6071): 959–962. doi:10.1126/science.1213859.
  122. ^ Bronnert, Constance; Métais, Grégoire (2023). "Early Eocene hippomorph perissodactyls (Mammalia) from the Paris Basin". Geodiversitas. 45 (9): 277–326. doi:10.5252/geodiversitas2023v45a9.
  123. ^ Remy, Jean-Albert (1992). "Observations sur l'anatomie cranienne du genre Palaeotherium (Perissodactyla, Mammalia): mise en évidence d'un nouveau sous-genre, Franzenitherium". Palaeovertebrata. 21 (3–4): 103–224.
  124. ^ Ruiz-Colmenares, Miguel Ángel Cuesta (1993). "Los Palaeotheriidae (Perissodactyla, Mammalia) del Eoceno de la Cuenca del Duero (Castilla y León, España)". Estudios Geológicos. 49 (1–2): 87–109. doi:10.3989/egeol.93491-2341.
  125. ^ "Mammals' bodies outpaced their brains right after the dinosaurs died". Science News. 31 March 2022. Retrieved 14 May 2022.
  126. ^ Bertrand, Ornella C.; Shelley, Sarah L.; Williamson, Thomas E.; Wible, John R.; Chester, Stephen G. B.; Flynn, John J.; Holbrook, Luke T.; Lyson, Tyler R.; Meng, Jin; Miller, Ian M.; Püschel, Hans P.; Smith, Thierry; Spaulding, Michelle; Tseng, Z. Jack; Brusatte, Stephen L. (April 2022). "Brawn before brains in placental mammals after the end-Cretaceous extinction". Science. 376 (6588): 80–85. Bibcode:2022Sci...376...80B. doi:10.1126/science.abl5584. ISSN 0036-8075. PMID 35357913. S2CID 247853831. Retrieved 19 November 2023.
  127. ^ Buffetaut, Eric; Angst, Delphine (November 2014). "Stratigraphic distribution of large flightless birds in the Palaeogene of Europe and its palaeobiological and palaeogeographical implications". Earth-Science Reviews. 138: 394–408. Bibcode:2014ESRv..138..394B. doi:10.1016/j.earscirev.2014.07.001. Retrieved 20 July 2024 – via Elsevier Science Direct.
  128. ^ Mayr, Gerald; Göhlich, Ursula B.; Roček, Zbyněk; Lemierre, Alfred; Winkler, Viola; Georgalis, Georgios L. (22 November 2023). "Reinterpretation of tuberculate cervical vertebrae of Eocene birds as an exceptional anti-predator adaptation against the mammalian craniocervical killing bite". Journal of Anatomy. 244 (3): 402–410. doi:10.1111/joa.13980. ISSN 0021-8782. PMC 10862156. PMID 37990985.
  129. ^ Georgalis, Georgios L.; Abdel Gawad, Mohamed K.; Hassan, Safiya M.; El-Barkooky, Ahmed N.; Hamdan, Mohamed A. (2020-05-22). "Oldest co-occurrence of Varanus and Python from Africa—first record of squamates from the early Miocene of Moghra Formation, Western Desert, Egypt". PeerJ. 8: e9092. doi:10.7717/peerj.9092. ISSN 2167-8359. PMC 7255343. PMID 32509449.
  130. ^ Wolfe, Alexander P.; Tappert, Ralf; Muehlenbachs, Karlis; Boudreau, Marc; McKellar, Ryan C.; Basinger, James F.; Garrett, Amber (1 July 2009). "A new proposal concerning the botanical origin of Baltic amber". Proceedings of the Royal Society B. 276 (1972): 3403–3412. doi:10.1098/rspb.2009.0806. PMC 2817186. PMID 19570786.
  131. ^ Price, Benjamin W.; Marshall, David C.; Barker, Nigel P.; Simon, Chris; Villet, Martin H. (29 March 2019). "Out of Africa? A dated molecular phylogeny of the cicada tribe Platypleurini Schmidt (Hemiptera: Cicadidae), with a focus on African genera and the genus Platypleura Amyot & Audinet-Serville". Systematic Entomology. 44 (4): 842–861. Bibcode:2019SysEn..44..842P. doi:10.1111/syen.12360. ISSN 0307-6970. Retrieved 20 July 2024 – via Wiley Online Library.
  132. ^ Shahin, Abdalla; El Khawagah, Samar; Shahin, Banan (May 2023). "Implication of middle Eocene to early Miocene ostracodes from the N. El Faras-1X Well, Qattara Depression, Egypt, for paleobathymetry and paleobiogeographic reconstruction". Marine Micropaleontology. 181: 102244. doi:10.1016/j.marmicro.2023.102244. Retrieved 20 July 2024 – via Elsevier Science Direct.
  133. ^ Arias-Villegas, Viviana; Bedoya Agudelo, Erika L.; Vallejo-Hincapié, Felipe; Aubry, Marie-Pierre; Pardo-Trujillo, Andrés (August 2023). "Late Eocene to Early Miocene calcareous nannofossil biostratigraphy from the ANH-San Jacinto- 1 well: Stratigraphic implications for the Sinú-San Jacinto basin in the Caribbean region of Colombia". Journal of South American Earth Sciences. 128: 104470. Bibcode:2023JSAES.12804470A. doi:10.1016/j.jsames.2023.104470. Retrieved 20 July 2024 – via Elsevier Science Direct.

Further reading

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