scholarly journals Krzywopłoty – Late Glacial and Holocene Mire in the Bydlin Area (Częstochowa Upland)

2011 ◽  
Vol 4 (1) ◽  
pp. 89-102 ◽  
Author(s):  
Sławomir Żurek ◽  
Małgorzata Nita ◽  
Katarzyna Imioł
Keyword(s):  
Water Level ◽  
Laboratory Tests ◽  
Younger Dryas ◽  
Late Glacial ◽  
Pine Forests ◽  
Pollen Data ◽  
Continuous Transformation ◽  
Pollen Assemblage ◽  
Late Glacial And Holocene ◽  
Organic Deposits

Abstract Macroscopic and laboratory tests of over 4-metre-thick organic deposits of Krzywopłoty profile (gyttjas and peat) allowed the authors to identify the development of the peatland as having four phases, each transition being associated with fluctuations in water level. Sediments from a depth of 3.75-0.65 m were also included in palynological testing. Seven local pollen assemblage zones show a continuous transformation in the plant landscape and surroundings of the site between the end of the Vistulian and the Holocene. Pollen data indicates a change of vegetation, from open communities of herbaceous plants and loose pine-birch communities in the Younger Dryas, then dense pine forests in the Preboreal chronozone, and finally multispecies forests in the Atlantic and Subboreal chronozones.

Late-Glacial-Holocene Climate of the Lake District of Chile

1984 ◽  
Vol 22 (1) ◽  
pp. 77-90 ◽  
Author(s):  
Calvin J. Heusser
Keyword(s):  
Late Glacial ◽  
Cold Climate ◽  
Time Range ◽  
Lake District ◽  
Pollen Assemblage ◽  
Holocene Climate ◽  
Nothofagus Obliqua ◽  
Summer Temperatures ◽  
Cooling Trend ◽  
Late Glacial And Holocene

Pollen evidence from a 350-cm section of a fen in a moraine belt at Rucañancu (39°33′S, 72°18′W) bears on the controversy regarding interpretation of late-glacial and Holocene climate in midlatitude Chile. Earlier pollen studies, indicating a cooling trend between approximately 11,000 and 10,000 yr B.P., disagreed with observations of glacier fluctuations which show continuous glacier wastage and, by inference, warming after 12,500 yr B.P. and possibly earlier, up until Neoglaciation, beginning after 6850 yr B.P. Fossil beetle assemblage data in this time range support the interpretation of climate made from the observed glacier behavior. At Rucañancu, a pollen assemblage containing upper montane podocarp (Podocarpus andinus) in quantities reaching 34% and dating between 10,440 and 10,000 yr B.P. implies a cold climate with summer temperatures possibly 5–8°C lower than today's. Holocene warming began afterward, later than the glacier and beetle records indicate, and continued until at least 8350 yr B.P., as suggested by the sequence of assemblages dominated by Myrtaceae, by Aextoxicon punctatum, and by Gramineae. A subsequent assemblage of Nothofagus obliqua type implies an increase of moisture until 6960 yr B.P., following which N. dombeyi type, under a cool and humid Neoglacial climate, became dominant.

scholarly journals Reconstruction of vegetation in the foothills of the Carpathian Mountains, Gorgany region, in the late glacial (based on pollen data of peat-bog Pidluzhia)

2015 ◽  
pp. 333-340
Author(s):  
Natalia Chumak
Keyword(s):  
Key Words ◽  
Radiocarbon Dating ◽  
Environmental Changes ◽  
Younger Dryas ◽  
Late Glacial ◽  
Peat Bog ◽  
Pollen Data ◽  
Carpathian Mountains ◽  
The Holocene ◽  
Short Period

The environmental changes on short-period stages of the Late Glacial were reconstructed based on pollen data of peat-bog Pidluzhia deposits and their radiocarbon dating. There are the Older and Younger Dryas, the Allerod (three phases) are allocated on palynological data in the Late Glacial. Vegetation had evolved from cold meadows to pine forest during this time. The transition from the Late Glacial to the Holocene was identified by the emergence of broad-leaved trees (elm, oak and linden), the spreading of spruce and disappearance of xerophytic elements. Key words: paleovegetation, paleoclimate, palinology, the Late Glacial, the foothills of the Carpathian Mountains.

scholarly journals Interdisciplinary studies of spring mire deposits from Radzików (South Podlasie Lowland, East Poland) and their significance for palaeoenvironmental reconstructions

2012 ◽  
Vol 39 (1) ◽  
pp. 10-29 ◽  
Author(s):  
Radosław Dobrowolski ◽  
Irena Pidek ◽  
Witold Alexandrowicz ◽  
Stanisław Hałas ◽  
Anna Pazdur ◽  
...  
Keyword(s):  
Radiocarbon Dating ◽  
Environmental Changes ◽  
Younger Dryas ◽  
Late Glacial ◽  
Plant Macrofossils ◽  
Interdisciplinary Studies ◽  
Carbon Stable Isotopes ◽  
Calcareous Tufa ◽  
Palaeoenvironmental Reconstructions ◽  
Late Glacial And Holocene

Abstract The paper presents the results of interdisciplinary (multiproxy) palaeoenvironmental studies of peat — calcareous tufa depositional sequences of spring mire from Radzików site (east Poland). Analyses of three biotic proxies (plant macrofossils, pollen, molluscs) were supplemented with sedimentological, geochemical, oxygen and carbon stable isotopes analyses and radiocarbon dating and used for reconstruction of environmental changes in Late Glacial and Holocene. The obtained results enable us to (1) reconstruct main phases of mire development and (2) determine environmental factors influencing changes of water supply. The object started to develop in Allerød. The Late Glacial and Early Holocene deposit sequence is relatively thick (about 1.0 m), with good palaeoecological record. The boundary between Younger Dryas and Preboreal is especially well confirmed by palynological and malacological analyses as well as radiocarbon dating. The Mesoholocene deposits are considerably worse preserved. Mire development was evaluated in terms of general mire ecology.

Fluctuations of Outlet and Valley Glaciers in the Southern Andes (Argentina) during the Past 13,000 Years

1999 ◽  
Vol 51 (3) ◽  
pp. 238-247 ◽  
Author(s):  
Gerd Wenzens
Keyword(s):  
Younger Dryas ◽  
Late Glacial ◽  
The South ◽  
Southern Andes ◽  
Outlet Glacier ◽  
The Holocene ◽  
The Past ◽  
Late Glacial And Holocene ◽  
Glacial Time

AbstractIn the southern Argentine Andes, ten advances of valley glaciers were used to reconstruct the late-glacial and Holocene glacier history. The accumulation areas of these glaciers lie in the Precordillera and are thus independent of fluctuations of the South Patagonian Icefield. Like the Viedma outlet glacier, the valley glaciers advanced three times during late-glacial time (14,000–10,000 yr B.P.). The youngest advance correlates with the Younger Dryas Stade, based on two minimum AMS14C dates of 9588 and 9482 yr B.P. The second oldest advance occurred before 11,800 yr B.P. During the first half of the Holocene, (ca. 10,000–5000 yr B.P.), advances culminated about 8500, 8000–7500, and 5800–5500 yr B.P. During the second half of the Holocene, advances occurred between ca. 4500 and 4200 yr B.P., as well as between 3600 and 3300 yr B.P. In the Rı́o Cóndor valley three subsequent advances have been identified.

Early Holocene hydrology and environments of the Ner River (Poland)

2016 ◽  
Vol 85 (2) ◽  
pp. 187-203 ◽  
Author(s):  
Piotr Kittel ◽  
Mateusz Płociennik ◽  
Ryszard K. Borόwka ◽  
Daniel Okupny ◽  
Dominik Pawłowski ◽  
...  
Keyword(s):  
Climate Changes ◽  
Late Glacial ◽  
Reference Points ◽  
Early Holocene ◽  
Oxbow Lake ◽  
Pollen Data ◽  
Overbank Sediments ◽  
Winter Temperatures ◽  
Organic Deposits ◽  
Boreal Period

The Ner River valley (central Poland) underwent substantial transformation during the Weichselian–Holocene transition as a result of fluvial processes and climate changes, resulting in the establishment of its present shape in the Holocene. A multiproxy study based on organic deposits from a palaeochannel fill (Lutomiersk–Koziówki) shows that after the channel was cut off during the late glacial termination, it became a shallow oxbow, fed by local springs. In the Boreal period, the oxbow lake was also fed by precipitation and became a telmatic environment overgrown by rush and swamp vegetation. Finally, it was covered by overbank deposits. The first flooding phase (9900–9600 cal. BP) was followed by the accumulation of overbank sediments (after 9500 cal. BP) and flooding increased after ca. 9300–9000 cal. BP. Pollen data provide information on the regional vegetation context for local and regional changes. In the Atlantic period, an increase in both summer and winter temperatures is inferred from the pollen data, corresponding to an expansion of thermophilous deciduous forests. While in general, flooding phases of the Early Holocene are poorly recognised in Eastern Europe, the Lutomiersk–Koziówki site may be considered as one of the reference points for this phenomenon in the region.

A Younger Dryas Icecap in the Equatorial Andes

1997 ◽  
Vol 47 (1) ◽  
pp. 13-28 ◽  
Author(s):  
Chalmers M. Clapperton ◽  
Minard Hall ◽  
Patricia Mothes ◽  
Malcolm J. Hole ◽  
John W. Still ◽  
...  
Keyword(s):  
Younger Dryas ◽  
Late Glacial ◽  
Tropical Andes ◽  
Outlet Glacier ◽  
Radiocarbon Dates ◽  
Glacial Ice ◽  
Ice Cap ◽  
North Atlantic Climate ◽  
Organic Deposits ◽  
Younger Dryas Event

AbstractMorphologic and stratigraphic evidence shows that a late-glacial ice cap existed on part of the Eastern Cordillera of Ecuador (Lat. 0° 20′ S) on ground with a mean elevation of 4200 m where none exists now. An outlet glacier from an ca. 800 km2ice cap terminated at 3850 m altitude in the Papallacta valley on the eastern side of the plateau. Radiocarbon dates show that moraines formed by this advance were ice-free by 13,20014C yr B.P. Tephras and the age of organic deposits at the plateau edge indicate ice-free conditions before 11,80014C yr B.P. This interval was followed by the expansion of an ca. 140 km2ice cap that discharged glaciers into adjacent valleys where terminal moraines were built at 3950 m altitude. AMS and conventional radiocarbon dates from macrofossils, peat, and gyttja above and below till of the readvance indicate that the ice cap formed between ca. 11,000 and 10,00014C yr B.P. and was thus coeval with the European Younger Dryas event. The ice cap developed in response to a surface temperature cooling of at least 3°C in the tropical Andes, a finding that is consistent with a coupled equatorial/high latitude North Atlantic climate system operating at the late-glacial/Holocene transition. These results are further evidence that Younger Dryas cooling may have been a global event.

scholarly journals A reindeer track from a drill core, and lake basin development of the Late Glacial Lille Slotseng kettle-hole basin, South-East Jylland, Denmark

2007 ◽  
Vol 55 ◽  
pp. 85-95
Author(s):  
Nanna Noe Nygaard ◽  
Jesper Milán ◽  
Mikkel Ulfeldt Hede ◽  
Jørgen Holm
Keyword(s):  
Younger Dryas ◽  
Late Glacial ◽  
Maximum Diameter ◽  
Lake Basin ◽  
Drill Core ◽  
Soft Sediment ◽  
Southeastern Part ◽  
Kettle Hole ◽  
Time Period ◽  
Late Glacial And Holocene

IA subfossil reindeer track is found in lake shore sediments in a drill core through the Late Glacial and Holocene lacustrine succession from the Lille Slotseng kettle-hole basin, located in the southeastern part of Jylland. The track is dated to 11,795 ± 80 14C yr BP or 13,635 cal. yr BP. This is the first vertebrate track recognized from a soft sediment drill core. Hitherto, convincing vertebrate trace fossils have only been described from boreholes through lithified Triassic sediments. During a previous excavation at the site, skeletal remains of at least ten reindeer were recovered from the Bølling succession and a vertebra was dated to approximately 14,100 cal. yr BP. The Lille Slotseng basin is semicircular with a maximum diameter of 23 m and the overall transgressive–regressive succession covers the time period from 16,000 to around 8,000 cal. yr BP. The oldest basin-fill sediments are melt-water deposits. They are overlain by a succession belonging to the Bølling Interstadial (GI 1-e), older Dryas (GI 1-d), Allerød, (GI 1-c, 1-b, 1-a), and Younger Dryas (GS 1), which terminates the Late Glacial succession. Then follows Preboreal algal gyttja and nearshore woody peat from the Boreal and Early Atlantic times, filling the basin.

Late-glacial and Holocene sedimentation and fluctuations of river water level in the Caquetá River area (Colombian Amazonia)

1992 ◽  
Vol 7 (1) ◽  
pp. 57-67 ◽  
Author(s):  
Thomas Van Der Hammen ◽  
Ligia E. Urrego ◽  
Nohora Espejo ◽  
Joost F. Duivenvoorden ◽  
Johanna M. Lips
Keyword(s):  
Water Level ◽  
River Water ◽  
Late Glacial ◽  
Late Glacial And Holocene

Palaeoenvironments in the Vale of Pickering. Part I: Stratigraphy and Palaeogeography of Seamer Carr, Star Carr and Flixton Carr

1988 ◽  
Vol 54 ◽  
pp. 1-19 ◽  
Author(s):  
E. W. Cloutman
Keyword(s):  
Water Level ◽  
Open Water ◽  
Late Glacial ◽  
Pictorial Representation ◽  
Large Area ◽  
Dry Land ◽  
Pollen Zone ◽  
Pollen Diagrams ◽  
Mesolithic Period ◽  
Organic Deposits

A contour map of part of the basin of the glacial Lake Pickering was constructed from surface and sub-surface levels. This map (figs 2, 3 and 4) gives a pictorial representation of the microtopography of the area and is amplified by an additional map (fig. 13) in which the margin of the organic deposits is given for the early Mesolithic period, based on evidence outlined below. A stratigraphical survey of the basin deposits shows that the infilling of the lake in the Devensian Late-glacial began largely with the deposition of calcareous muds. In the early Flandrian there followed a natural hydroseral development from open water to reedswamp and fen carr. Towards the end of the Boreal period and during the early Atlantic, a rise in water level was responsible for the replacement of fen carr by reedswamp. The rate of hydroseral development was affected by a progressive rise of water level. This has been determined (estimated) by radio-carbon dating the basal organic muds on the 23, 24 and 25 m OD sub-surface contours at eight sites within the study area. During the early Mesolithic (Godwin's pollen Zone IV, c.9600 BP)the water level in the basin was likely to have been in the range of 23–24.5 m OD. By reference to the dating evidence, including published pollen diagrams (Walker and Godwin 1954) and new data presented in Parts 2 and 3, the stratigraphical evidence is interpreted to show that there was considerable variation in the vegetation of the lake margin during the early Mesolithic period (pollen Zone IV). At Seamer Carr there was a large area of fen carr woodland with reedswamp fringing the open water. Star Carr had a much larger area of reedswamp, with open water close to the dry land in places, but with a narrow fringe of carr. The bed of the ancient River Hertford, which drained the basin, probably in the late Mesolithic, has been identified in two of the sections which traverse the basin.

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