The geochemical and pedogenic signatures of Shantisagara lake sediments, southern India: Implications for weathering, terrigenous influx, and provenance during the Holocene

2022 ◽  
Author(s):  
Kizhur Sandeep ◽  
Rajasekhariah Shankar ◽  
Anish Kumar Warrier ◽  
Geetha Hariendranath Aravind
Keyword(s):  
Lake Sediments ◽  
Southern India ◽  
The Holocene

scholarly journals A late Quaternary record of eolian silt deposition in a maar lake, St. Michael Island, western Alaska

2003 ◽  
Vol 60 (1) ◽  
pp. 110-122 ◽  
Author(s):  
Daniel R. Muhs ◽  
Thomas A. Ager ◽  
Josh Been ◽  
J. Platt Bradbury ◽  
Walter E. Dean
Keyword(s):  
Lake Sediments ◽  
Late Quaternary ◽  
Geochemical Data ◽  
Unexpected Finding ◽  
The Holocene ◽  
Tundra Vegetation ◽  
Shrub Tundra ◽  
Loess Deposition ◽  
Maar Lake ◽  
Glacial Time

AbstractRecent stratigraphic studies in central Alaska have yielded the unexpected finding that there is little evidence for full-glacial (late Wisconsin) loess deposition. Because the loess record of western Alaska is poorly exposed and not well known, we analyzed a core from Zagoskin Lake, a maar lake on St. Michael Island, to determine if a full-glacial eolian record could be found in that region. Particle size and geochemical data indicate that the mineral fraction of the lake sediments is not derived from the local basalt and is probably eolian. Silt deposition took place from at least the latter part of the mid-Wisconsin interstadial period through the Holocene, based on radiocarbon dating. Based on the locations of likely loess sources, eolian silt in western Alaska was probably deflated by northeasterly winds from glaciofluvial sediments. If last-glacial winds that deposited loess were indeed from the northeast, this reconstruction is in conflict with a model-derived reconstruction of paleowinds in Alaska. Mass accumulation rates in Zagoskin Lake were higher during the Pleistocene than during the Holocene. In addition, more eolian sediment is recorded in the lake sediments than as loess on the adjacent landscape. The thinner loess record on land may be due to the sparse, herb tundra vegetation that dominated the landscape in full-glacial time. Herb tundra would have been an inefficient loess trap compared to forest or even shrub tundra due to its low roughness height. The lack of abundant, full-glacial, eolian silt deposition in the loess stratigraphic record of central Alaska may be due, therefore, to a mimimal ability of the landscape to trap loess, rather than a lack of available eolian sediment.

Environmental changes of the Okhotsk-Kolyma divide from glacial lake sediments during the Holocene

2014 ◽  
Vol 8 (6) ◽  
pp. 464-474 ◽  
Author(s):  
P. M. Anderson ◽  
A. V. Lozhkin ◽  
P. S. Minuyk ◽  
A. Yu. Pakhomov
Keyword(s):  
Lake Sediments ◽  
Environmental Changes ◽  
Glacial Lake ◽  
The Holocene

Alpine climate during the Holocene: a comparison between records of glaciers, lake sediments and solar activity

2011 ◽  
Vol 26 (7) ◽  
pp. 703-713 ◽  
Author(s):  
Samuel U. Nussbaumer ◽  
Friedhelm Steinhilber ◽  
Mathias Trachsel ◽  
Petra Breitenmoser ◽  
Jürg Beer ◽  
...  
Keyword(s):  
Solar Activity ◽  
Lake Sediments ◽  
The Holocene

Phytoliths as indicators of grassland dynamics during the Holocene from lake sediments in the Ubari sand sea, Fazzan Basin, Libya

2008 ◽  
Vol 39 ◽  
pp. 29-40 ◽  
Author(s):  
Adrian Parker ◽  
Belinda Harris ◽  
Kevin White ◽  
Nick Drake
Keyword(s):  
Lake Sediments ◽  
Growing Season ◽  
Summer Season ◽  
Tree Cover ◽  
C4 Grasses ◽  
The Holocene ◽  
Phytolith Analysis ◽  
Grassland Community ◽  
C3 Grasses

AbstractThis paper presents the first study of phytoliths from the Saharan region. Phytolith analysis shows the potential of reconstructing grassland dynamics during the Holocene, refining our knowledge of palaeoecosystems in the Ubari sand sea, Libya. The lake sediments studied range in age between 3,273–9,440 cal. BP. Tree cover was very low around 3,273–3,436 cal. BP and 6,678–6,796 cal. BP, and the landscape was dominated by C4 grasslands around 6,678–6,796 cal. BP, shifting to a more mixed C3-C4 grassland community around 3,273–3,436 cal. BP. These differences may be caused by the older sample being deposited during the onset of a brief arid period, but a similar phytolith assemblage could arise due to a more pronounced seasonality in the climate, with C3 grasses dominating late and early in the growing season when the climate is cooler and less arid, and C4 grasses becoming dominant in the hot, dry summer season.

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