Environmental preferences of brachiopods and bivalves across major climatic changes during the Late Palaeozoic ice age (Pennsylvanian, western Argentina)

Palaeontology ◽  
2016 ◽  
Vol 59 (6) ◽  
pp. 803-816 ◽  
Author(s):  
Diego Balseiro ◽  
Karen Halpern
Keyword(s):  
Climatic Changes ◽  
Ice Age ◽  
Environmental Preferences ◽  
Late Palaeozoic

Ice-Core Pollen Record of Climatic Changes in the Central Andes during the last 400 yr

2005 ◽  
Vol 64 (2) ◽  
pp. 272-278 ◽  
Author(s):  
Kam-biu Liu ◽  
Carl A. Reese ◽  
Lonnie G. Thompson
Keyword(s):  
Little Ice Age ◽  
Ice Core ◽  
Climatic Changes ◽  
Ice Age ◽  
Striking Similarity ◽  
Pollen Record ◽  
Dry Period ◽  
Proxy Records ◽  
Ice Cap ◽  
Ice Accumulation

AbstractThis paper presents a high-resolution ice-core pollen record from the Sajama Ice Cap, Bolivia, that spans the last 400 yr. The pollen record corroborates the oxygen isotopic and ice accumulation records from the Quelccaya Ice Cap and supports the scenario that the Little Ice Age (LIA) consisted of two distinct phases�"a wet period from AD 1500 to 1700, and a dry period from AD 1700 to 1880. During the dry period xerophytic shrubs expanded to replace puna grasses on the Altiplano, as suggested by a dramatic drop in the Poaceae/Asteraceae (P/A) pollen ratio. The environment around Sajama was probably similar to the desert-like shrublands of the Southern Bolivian Highlands and western Andean slopes today. The striking similarity between the Sajama and Quelccaya proxy records suggests that climatic changes during the Little Ice Age occurred synchronously across the Altiplano.

II.—Pleistocene Climatic Changes

1894 ◽  
Vol 1 (8) ◽  
pp. 340-349 ◽  
Author(s):  
Warren Upham
Keyword(s):  
Climatic Changes ◽  
Ice Age ◽  
Temperate Climate ◽  
Northern Latitudes ◽  
Fossil Floras ◽  
Geologic Record

The most interesting and difficult climatic problem presented in all the geologic record is that of its latest period, immediately preceding the present, to discover the causes, first, of the accumulation, and later, of the rapid final melting of its vast sheets of land-ice. The fossil floras of Greenland and Spitzbergen indicate that those far northern latitudes enjoyed a temperate climate in the Miocene period; and, from the absence of glacial drift through the great series of Tertiary and Mesozoic formations, we infer that climates as mild as those of the present day had prevailed during long eras before the Ice-age.

Climatic Changes in the Qinghai-Xizang (Tibetan) Region of China during the Holocene

1987 ◽  
Vol 28 (1) ◽  
pp. 50-60 ◽  
Author(s):  
Wang Fu-Bao ◽  
C. Y. Fan
Keyword(s):  
Cross Sections ◽  
Little Ice Age ◽  
Climatic Changes ◽  
Northern Region ◽  
Ice Age ◽  
Southern Slope ◽  
The Holocene ◽  
Northeastern Part ◽  
Xizang Plateau ◽  
Sand And Gravel

AbstractClimatic changes in the Qinghai-Xizang Plateau of China were studied by analyzing the composition of peat and layers of sand and gravel distributed along the southern slopes of Nianqing-Tanggula and Gangdise Mountains, cross sections of deposits near a number of interior lakes in Xizang, past glacial variations on the southern slope of Nianqing-Tanggula Mountain, and landform changes south of the Yaluzangbu River. Such geologic evidence suggests a division of five climatic periods since the beginning of the Holocene: (1) The Wumadung interval, 10,000–7500 yr B.P., slightly cold and dry; (2) Qilongduo interval, 7500-3000 yr B.P., warm and moist; (3) the mid-Neoglacial period, 3000-1500 yr B.P., cold, except between 2500 and 200 yr B.P. when it was warmer; (4) the Dawelong interval, 1500-300 yr B.P., mild; and (5) the Little Ice Age, 300-0 yr B.P., cold. These changes progressed in a similar but not identical pattern as those in the northeastern part of China and in the northern region of Europe.

Distribution and ecology of early ferns

1985 ◽  
Vol 86 ◽  
pp. 141-149 ◽  
Author(s):  
Andrew C. Scott ◽  
Jean Galtier
Keyword(s):  
Current Knowledge ◽  
Climatic Changes ◽  
Lower Carboniferous ◽  
Late Palaeozoic ◽  
Distribution And Ecology ◽  
The Relationship ◽  
Volcanic Terrains

SynopsisA review of current knowledge of the distribution of Palaeozoic ferns and fern-like plants is presented. Whilst numerous putative ferns occur in the Devonian, it is not until the Lower Carboniferous that ferns belonging to the Filicales appear. The Namurian represents a major gap in our knowledge. The ecology of late Palaeozoic ferns is reviewed. The association of early fern assemblages with volcanic terrains is considered particularly significant in the relationship between evolution and environment. Extinction of more specialised groups may have been caused by climatic changes.

Paleoenvironmental records of water level and climatic changes from the middle to late holocene at a Lake Erie coastal wetland, Ontario, Canada

2006 ◽  
Vol 65 (1) ◽  
pp. 33-43 ◽  
Author(s):  
Sarah A. Finkelstein ◽  
Anthony M. Davis
Keyword(s):  
Water Level ◽  
Plant Communities ◽  
Little Ice Age ◽  
Lake Erie ◽  
Coastal Wetland ◽  
Climatic Changes ◽  
Ice Age ◽  
Climatic Forcing ◽  
Site Water ◽  
Northern Shore

AbstractPollen and diatom assemblages, and peat stratigraphies, from a coastal wetland on the northern shore of Lake Erie were used to analyze water level and climatic changes since the middle Holocene and their effects on wetland plant communities. Peat deposition began 4700 cal yr B.P. during the Nipissing II transgression, which was driven by isostatic rebound. At that time, a diatom-rich wild rice marsh existed at the site. Water level dropped at the end of the Nipissing rise at least 2 m within 200 yr, leading to the development of shallower-water plant communities and an environment too dry for most diatoms to persist. The sharp decline in water level was probably driven primarily by outlet incision, but climate likely played some role. The paleoecological records provide evidence for post-Nipissing century-scale transgressions occurring around 2300, 1160, 700 and 450 cal yr B.P. The chronology for these transgressions correlates with other studies from the region and implies climatic forcing. Peat inception in shallow sloughs across part of the study area around 700 cal yr B.P. coincides with the Little Ice Age. These records, considered alongside others from the region, suggest that the Little Ice Age may have resulted in a wetter climate across the eastern Great Lakes region.

Evidence from northwest European bogs shows ‘Little Ice Age’ climatic changes driven by variations in solar activity

The Holocene ◽  
2002 ◽  
Vol 12 (1) ◽  
pp. 1-6 ◽  
Author(s):  
Dmitri Mauquoy ◽  
Bas van Geel ◽  
Maarten Blaauw ◽  
Johannes van der Plicht
Keyword(s):  
Solar Activity ◽  
Little Ice Age ◽  
Climatic Changes ◽  
Ice Age

scholarly journals Temporal Change of Radiocarbon Reservoir Effect in Sugan Lake, Northwest China during the Late Holocene

Radiocarbon ◽  
2009 ◽  
Vol 51 (2) ◽  
pp. 529-535 ◽  
Author(s):  
Ai-feng Zhou ◽  
Fa-hu Chen ◽  
Zong-li Wang ◽  
Mei-lin Yang ◽  
Ming-rui Qiang ◽  
...  
Keyword(s):  
Little Ice Age ◽  
Late Holocene ◽  
Temporal Change ◽  
Northwest China ◽  
Climatic Changes ◽  
Lacustrine Sediment ◽  
Ice Age ◽  
Reservoir Effect ◽  
The Past ◽  
Reservoir Age

Many lacustrine chronology records suffer from radiocarbon reservoir effects. A continuous, accurate varve chronology, in conjunction with accelerator mass spectrometry (AMS) 14C dating, was used to determine the age of lacustrine sediment and to quantify the past 14C reservoir effect in Sugan Lake (China). Reservoir age varied from 4340 to 2590 yr due to 14C-depleted water in the late Holocene. However, during the Little Ice Age (LIA), 14C reservoir age was relatively stable. According to this study, 14C reservoir age in the late Holocene may be driven by hydrological and climatic changes of this period. Therefore, special caution should be paid to the correction of the 14C reservoir effect by a unique 14C reservoir age in paleoclimatic and paleolimnological study of northwest China.

Sensitivity of Cool-Temperate Forests and their Fossil Pollen Record to Rapid Temperature Change

1985 ◽  
Vol 23 (3) ◽  
pp. 327-340 ◽  
Author(s):  
Margaret Bryan Davis ◽  
Daniel B. Botkin
Keyword(s):  
Sugar Maple ◽  
Climatic Changes ◽  
Forest Growth ◽  
Ice Age ◽  
Fossil Pollen ◽  
Mean Annual Temperature ◽  
Pollen Record ◽  
Adult Trees ◽  
Cool Temperate ◽  
Delayed Responses

Simulations of cool-temperate forest growth in response to climatic change using the JABOWA computer model show that a decrease of 600 growing degree-days (equivalent to a 2°C decrease in mean annual temperature) causes red spruce (Picea rubens) to replace sugar maple (Acer saccharum) as the dominant tree. These changes are delayed 100–200 yr after the climatic cooling, producing gradual forest changes in response to abrupt temperature changes, and reducing the amplitude of response to brief climatic events. Soils and disturbances affect the speed and magnitude of forest response. The delayed responses are caused by the difference in sensitivity of adult trees and younger stages. The length of the delay depends on the life history characteristics of the dominant species. Delayed responses imply that fossil pollen deposits, even if they faithfully record the abundances of trees in forests, may not be able to resolve climatic changes within 100–200 yr, or to record very brief climatic events. This explains why pollen deposits do not as yet show responses to climatic changes during the past 100 yr. Only the Little Ice Age, which lasted several centuries, caused sufficient forest change to be recorded in fossil pollen, and only at certain sites.

scholarly journals Trends and features of climatic changes in the past 5000 years recorded by the Dunde ice core

1992 ◽  
Vol 16 ◽  
pp. 21-24 ◽  
Author(s):  
Yao Tandong ◽  
L. G. Thompson
Keyword(s):  
Accumulation Rate ◽  
Ice Core ◽  
Climatic Changes ◽  
Ice Age ◽  
The Tibetan Plateau ◽  
Temperature Relation ◽  
The Core ◽  
The Past ◽  
Ice Cap ◽  
The Qilian Mountains

Α δ18O record from Dunde Ice Cap, located in the Qilian mountains on the northeastern margin of the Tibetan Plateau, has been analyzed and interpreted. With an ice temperature of –7.3°C at a depth of 10 m and –4.7°C at the bottom of the ice cap, and an accumulation rate of 400 mm a−1, the Dunde core has provided interesting results. The upper part of this core, core D-l, can be easily dated by a combination of δ18O, microparticle concentration and conductivity. It can also be dated as far back as 4550 BP by counting dust layers in ice. Based on the time scale established by the above methods and on the δ18O–temperature relation, the δ18O fluctuations in the upper 120 m of the core can be interpreted as mainly due to climatic changes during the past ~ 5000 years. The warmest periods in the past ~ 5000 years in the core were found to be centered on the present, 3000, and 4100 BP, and the colder periods center around 500, 1200, 4000, and 4500 BP. It is clear from the ice-core record that the Little Ice Age was only one of many cold periods in the past, although it was the coldest period in the past 500 years.

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