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Libros sobre el tema "Pleistocene Climate Changes"

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Publicado: 4 de junio de 2021
Última modificación: 20 de febrero de 2023

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1

Avian community, climate, and sea-level changes in the Plio-Pleistocene of the Florida peninsula. Washington, DC: American Ornithologists' Union, 1998.

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2

Little, Martin Lewis. Pollen and grain size records in abyssal sediments of the northwest Pacific Ocean as proxies of Plio-Pleistocene climate change. St. Catharines, Ont: Brock University, Dept. of Earth Sciences, 2005.

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3

Muller, R. Ice ages and astronomical causes: Data, spectral analysis, and mechanisms. London: Springer, 2000.

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4

1929-, MacDonald Gordon J., ed. Ice ages and astronomical causes: Data, spectral analysis, and mechanisms. London: Springer, 2002.

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5

Lurcock, Pontus y Fabio Florindo. Antarctic Climate History and Global Climate Changes. Oxford University Press, 2017. http://dx.doi.org/10.1093/oxfordhb/9780190676889.013.18.

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Antarctic climate changes have been reconstructed from ice and sediment cores and numerical models (which also predict future changes). Major ice sheets first appeared 34 million years ago (Ma) and fluctuated throughout the Oligocene, with an overall cooling trend. Ice volume more than doubled at the Oligocene-Miocene boundary. Fluctuating Miocene temperatures peaked at 17–14 Ma, followed by dramatic cooling. Cooling continued through the Pliocene and Pleistocene, with another major glacial expansion at 3–2 Ma. Several interacting drivers control Antarctic climate. On timescales of 10,000–100,000 years, insolation varies with orbital cycles, causing periodic climate variations. Opening of Southern Ocean gateways produced a circumpolar current that thermally isolated Antarctica. Declining atmospheric CO2 triggered Cenozoic glaciation. Antarctic glaciations affect global climate by lowering sea level, intensifying atmospheric circulation, and increasing planetary albedo. Ice sheets interact with ocean water, forming water masses that play a key role in global ocean circulation.
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6

Lurcock, Pontus y Fabio Florindo. Antarctic Climate History and Global Climate Changes. Oxford University Press, 2017. http://dx.doi.org/10.1093/oxfordhb/9780190699420.013.18.

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Antarctic climate changes have been reconstructed from ice and sediment cores and numerical models (which also predict future changes). Major ice sheets first appeared 34 million years ago (Ma) and fluctuated throughout the Oligocene, with an overall cooling trend. Ice volume more than doubled at the Oligocene-Miocene boundary. Fluctuating Miocene temperatures peaked at 17–14 Ma, followed by dramatic cooling. Cooling continued through the Pliocene and Pleistocene, with another major glacial expansion at 3–2 Ma. Several interacting drivers control Antarctic climate. On timescales of 10,000–100,000 years, insolation varies with orbital cycles, causing periodic climate variations. Opening of Southern Ocean gateways produced a circumpolar current that thermally isolated Antarctica. Declining atmospheric CO2 triggered Cenozoic glaciation. Antarctic glaciations affect global climate by lowering sea level, intensifying atmospheric circulation, and increasing planetary albedo. Ice sheets interact with ocean water, forming water masses that play a key role in global ocean circulation.
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7

Lund, David Charles. Millennial-scale surface and deep water oscillations in the N.E. Pacific: Implications for late pleistocene climate change. 1997.

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8

Lund, David Charles. Millennial-scale surface and deep water oscillations in the N.E. Pacific: Implications for late pleistocene climate change. 1997.

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9

Biodiversity response to climate change in the middle Pleistocene: The Porcupine Cave fauna from Colorado. Berkeley: University of California Press, 2004.

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10

Barnosky, Anthony D. Biodiversity Response to Climate Change in the Middle Pleistocene: The Porcupine Cave Fauna from Colorado. University of California Press, 2004.

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11

Late Pleistocene and Holocene environmental changes in Fish Lake Valley, Nevada-California: Geomorphic response of alluvial fans to climate change. [Denver, Colo.]: U.S. Dept. of the Interior, U.S. Geological Survey, 1993.

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12

C, Reheis Marith y Geological Survey (U.S.), eds. Late Pleistocene and Holocene environmental changes in Fish Lake Valley, Nevada-California: Geomorphic response of alluvial fans to climate change. [Denver, Colo.]: U.S. Dept. of the Interior, U.S. Geological Survey, 1993.

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13

C, Reheis Marith y Geological Survey (U.S.), eds. Late Pleistocene and Holocene environmental changes in Fish Lake Valley, Nevada-California: Geomorphic response of alluvial fans to climate change. [Denver, Colo.]: U.S. Dept. of the Interior, U.S. Geological Survey, 1993.

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14

Holmes, Jonathan y Philipp Hoelzmann. The Late Pleistocene-Holocene African Humid Period as Evident in Lakes. Oxford University Press, 2017. http://dx.doi.org/10.1093/acrefore/9780190228620.013.531.

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From the end of the last glacial stage until the mid-Holocene, large areas of arid and semi-arid North Africa were much wetter than present, during the interval that is known as the African Humid Period (AHP). During this time, large areas were characterized by a marked increase in precipitation, an expansion of lakes, river systems, and wetlands, and the spread of grassland, shrub land, and woodland vegetation into areas that are currently much drier. Simulations with climate models indicate that the AHP was the result of orbitally forced increase in northern hemisphere summer insolation, which caused the intensification and northward expansion of the boreal summer monsoon. However, feedbacks from ocean circulation, land-surface cover, and greenhouse gases were probably also important.Lake basins and their sediment archives have provided important information about climate during the AHP, including the overall increases in precipitation and in rates, trajectories, and spatial variations in change at the beginning and the end of the interval. The general pattern is one of apparently synchronous onset of the AHP at the start of the Bølling-Allerød interstadial around 14,700 years ago, although wet conditions were interrupted by aridity during the Younger Dryas stadial. Wetter conditions returned at the start of the Holocene around 11,700 years ago covering much of North Africa and extended into parts of the southern hemisphere, including southeastern Equatorial Africa. During this time, the expansion of lakes and of grassland or shrub land vegetation over the area that is now the Sahara desert, was especially marked. Increasing aridity through the mid-Holocene, associated with a reduction in northern hemisphere summer insolation, brought about the end of the AHP by around 5000–4000 years before present. The degree to which this end was abrupt or gradual and geographically synchronous or time transgressive, remains open to debate. Taken as a whole, the lake sediment records do not support rapid and synchronous declines in precipitation and vegetation across the whole of North Africa, as some model experiments and other palaeoclimate archives have suggested. Lake sediments from basins that desiccated during the mid-Holocene may have been deflated, thus providing a misleading picture of rapid change. Moreover, different proxies of climate or environment may respond in contrasting ways to the same changes in climate. Despite this, there is evidence of rapid (within a few hundred years) termination to the AHP in some regions, with clear signs of a time-transgressive response both north to south and east to west, pointing to complex controls over the mid-Holocene drying of North Africa.
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15

Barnosky, Anthony D., ed. Biodiversity Response to Climate Change in the Middle Pleistocene. University of California Press, 2004. http://dx.doi.org/10.1525/9780520930858.

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16

Barnosky, Anthony, ed. Biodiversity Response to Climate Change in the Middle Pleistocene. University of California Press, 2004. http://dx.doi.org/10.1525/california/9780520240827.001.0001.

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17

Gavin, Daniel G. y Linda B. Brubaker. Late Pleistocene and Holocene Environmental Change on the Olympic Peninsula, Washington. Springer, 2014.

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18

Gavin, Daniel G. y Linda B. Brubaker. Late Pleistocene and Holocene Environmental Change on the Olympic Peninsula, Washington. Springer International Publishing AG, 2016.

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19

Gavin, Daniel G. y Linda B. Brubaker. Late Pleistocene and Holocene Environmental Change on the Olympic Peninsula, Washington. Springer, 2014.

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20

Holman, J. Alan. Pleistocene Amphibians and Reptiles in Britain and Europe. Oxford University Press, 1998. http://dx.doi.org/10.1093/oso/9780195112320.001.0001.

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The Pleistocene epoch or Ice Age, an extended period of advancing and retreating ice sheets, is characterized by striking climatic oscillations and sea level fluctuations. This age saw the rise and spread of humans and a great extinction of large mammals by the end of the epoch; in fact, the world today is essentially the product of dramatic changes that took place in the Pleistocene. This book, a companion to the author's Pleistocene Amphibians and Reptiles in North America, discusses the Pleistocene amphibians and reptiles in Britain and the European continent eastward through present-day Poland, the Czech Republic, Hungary, the Yugoslavian republics, and Greece. The book begins with a general discussion of the Pleistocene in Britain and Europe with an emphasis on regional terms used to define Pleistocene chronological events. Next, a look at the pre-Pleistocene herpetofauna of the study area sets the stage for a discussion of Pleistocene herpetofauna. A significant section of the book consists of a "bestiary," a series of annotated taxonomic accounts of Pleistocene herpetological taxa from the region. Following this is the interpretive section, beginning with a discussion of herpetological species as paleoenvironmental indicators and continuing with an analysis of herpetological population adjustments to Pleistocene events in Britain and Europe, and then with a discussion of extinction patterns in the region. Finally, the author compares Pleistocene herpetological events in Europe with those in North America. This volume and its companion together provide an up-to-date and comprehensive review of Pleistocene herpetofaunas across a significant portion of the Northern Hemisphere.
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21

Eren, Metin I. Hunter-Gatherer Behavior: Human Response During the Younger Dryas. Taylor & Francis Group, 2016.

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22

Eren, Metin I. Hunter-Gatherer Behavior: Human Response During the Younger Dryas. Taylor & Francis Group, 2013.

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23

Eren, Metin I. Hunter-Gatherer Behavior: Human Response During the Younger Dryas. Taylor & Francis Group, 2016.

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24

Barnosky, Anthony D. Biodiversity Response to Climate Change in the Middle Pleistocene: The Porcupine Cave Fauna from Colorado. University of California Press, 2004.

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25

D, Barnosky Dr Anthony y Barnosky Dr Anthony D. Biodiversity Response to Climate Change in the Middle Pleistocene: The Porcupine Cave Fauna from Colorado. University of California Press, 2004.

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26

In The Shadow Of The Sabertooth A Renegade Naturalist Considers Global Warming The First Americans And The Terrible Beasts Of The Pleistocene. AK Press, 2013.

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27

Sabin, Ann Louise. Holocene and latest Pleistocene paleoceanography of the northeast Pacific and its relationship to climate change in the Pacific Northwest. 1994.

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28

American Megafaunal Extinctions At The End Of The Pleistocene. Springer, 2009.

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29

Ice Sheets and Late Quaternary Environmental Change. Wiley, 2001.

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30

Ice Sheets and Late Quaternary Environmental Change. John Wiley & Sons, 2001.

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31

MacDonald, Gordon J. y Richard A. Muller. Ice Ages and Astronomical Causes (Springer Praxis Books / Environmental Sciences). Springer, 2002.

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32

Weiss, Harvey, ed. Megadrought and Collapse. Oxford University Press, 2017. http://dx.doi.org/10.1093/oso/9780199329199.001.0001.

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This is the first book to treat the major examples of megadrought and societal collapse, from the late Pleistocene end of hunter–gatherer culture and origins of cultivation to the 15th century AD fall of the Khmer Empire capital at Angkor, and ranging from the Near East to South America. Previous enquiries have stressed the possible multiple and internal causes of collapse, such overpopulation, overexploitation of resources, warfare, and poor leadership and decision-making. In contrast, Megadrought and Collapse presents case studies of nine major episodes of societal collapse in which megadrought was the major and independent cause of societal collapse. In each case the most recent paleoclimatic evidence for megadroughts, multiple decades to multiple centuries in duration, is presented alongside the archaeological records for synchronous societal collapse. The megadrought data are derived from paleoclimate proxy sources (lake, marine, and glacial cores; speleothems, or cave stalagmites; and tree-rings) and are explained by researchers directly engaged in their analysis. Researchers directly responsible for them discuss the relevant current archaeological records. Two arguments are developed through these case studies. The first is that societal collapse in different time periods and regions and at levels of social complexity ranging from simple foragers to complex empires would not have occurred without megadrought. The second is that similar responses to megadrought extend across these historical episodes: societal collapse in the face of insurmountable climate change, abandonment of settlements and regions, and habitat tracking to sustainable agricultural landscapes. As we confront megadrought today, and in the likely future, Megadrought and Collapse brings together the latest contributions to our understanding of past societal responses to the crisis on an equally global and diverse scale.
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33

E&G - Quaternary Science Journal Vol. 60 No 1: Loess in Europe. Geozon Science Media, 2011.

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