Characterisation and palaeoclimate of a loess-like permafrost palaeosol sequence in NE Siberia

An integrated rock-magnetic and geochemical approach to loess/paleosol sequences from Bohemia and Moravia (Czech Republic): Implications for the Upper Pleistocene paleoenvironment in central Europe

“…This behavior indicates secondary clay enrichment, because Rb substitutes for K in K-feldspars and mica and becomes enriched during weathering, whereas K is more mobile and preferentially leached under moderate/strong chemical weathering (Nesbitt et al, 1980;Zech et al, 2008). The variability of K in the investigated profiles is in agreement with the various correlations between CEC and the elemental signatures that are discussed below.…”

Paleoclimate and weathering of the Tokaj (Hungary) loess–paleosol sequence

“…Sheldon and Tabor, 2009). Despite the debate about the reliability of these indices Li and Yang, 2010;Xiao et al, 2010), many applications can be found in the literature, mainly, but not limited to, Quaternary loess and/or paleosols in Europe Kovács, 2007;Kühn et al, 2013;Újvári et al, 2008;Újvári et al, 2014;Vancampenhout et al, 2013), North and South America (Goldberg and Humayun, 2010;Hall and Penner, 2013;Meier et al, 2014), China (Baumann et al, 2014;Chen et al, 1999;Xiong et al, 2010), Southern Arabia (Pietsch and Kühn, 2012) and Siberia (Zech et al, 2008). However, despite the large number of published A C C E P T E D M A N U S C R I P T…”

Improved compound‐specific δ13C analysis of n‐alkanes for application in palaeoenvironmental studies

“…3 Accordingly, many authors have used d 13 C variations in soils, sediments and loess palaeosol sequences to reconstruct C3-C4 vegetation changes in the past. [4][5][6][7][8] However, when interpreting smaller d 13 C variations, changing palaeoclimatic conditions [9][10][11] and isotope fractionation processes during soil organic matter (SOM) decomposition [12][13][14][15][16] may also have to be considered. Recently, Chen et al 17 and Krull et al 18 even attributed d 13 C enrichments of several per mil in tropical and subtropical soils to SOM decomposition instead of to C3-C4 changes and ascribed this to intense weathering and high organic matter turnover rates.…”