Tracing Sr isotopic composition in space and time across the Yangtze River basin

Chemical weathering controls on variations in the molybdenum isotopic composition of river water: Evidence from large rivers in China

“…The HHR river basin is located mainly in an aridsemiarid climate zone in northern China, where the annual precipitation ranges from 500 to 600 mm, which is less than half of the annual evaporation (Wang et al, 2012;Yang et al, 2004;Zhang et al, 1995;Zhou et al, 2014). However, the CJR basin experiences a subtropical monsoon climate where the annual precipitation ranges from 600 to 900 mm (Luo et al, 2014;Xu et al, 2010;Yang et al, 2004;Zhou et al, 2014). The climate of the XJR basin is typical of the tropical/ subtropical monsoonal style, with mean annual temperatures ranging from 14-23°C, and annual precipitation ranging from 1000-2000 mm (Wei et al, 2013;Xu and Han, 2009).…”

“…1a). The CJR catchment is situated in a subtropical monsoon climate region where annual precipitation ranges from 600 to 900 mm (Luo et al, 2014;Xu et al, 2010;Yang et al, 2004;Zhou et al, 2014). No new sampling of the CJR was carried out as part of this study, and the Mo isotopic compositions used in the following discussion were all obtained from previous researches (Archer and Vance, 2008;Neubert et al, 2011).…”

Evaluating natural and anthropogenic trace element inputs along an alpine to urban gradient in the Provo River, Utah, USA

“…Trace element concentrations (e.g., As, Cr, Mo, Pb, Sb, Se, Sr, Tl, and U)combined with 87 Sr/ 86 Sr ratios provide powerful discriminatory leverage for distinguishing among the variety of natural and anthropogenic solute sources to a river, including inputs from weathering, soil erosion, groundwater, mining, agriculture, and urban runoff (Barats et al, 2014;Christofaro and Leao, 2009;Fitzpatrick et al, 2007;Le Pape et al, 2012Luo et al, 2014;Ollivier et al, 2011;Potot et al, 2012;Xu and Han, 2009).For example, Sr is an important trace element for evaluating natural weathering processes in a watershed, and 87 Sr/ 86 Sr ratios can be used to distinguish between silicate and carbonate weathering (Bickle et al, 2005;Brennan et al, 2014;Chetelat et al, 2008;Jacobson et al, 2002;Voss et al, 2014;Wei et al, 2013). Furthermore, weathering of specific types of bedrock such as black shales may contribute other elements, including Se and U (Bates, 1957;Galindo et al, 2007;Lavergren et al, 2009a;Rawat et al, 2010;Stillings and Amacher, 2010;Tuttle et al, 2014aTuttle et al, , 2014bWen and Carignan, 2011).…”

Modeling the paleo-seawater radiogenic strontium isotope record: A case study of the Late Jurassic-Early Cretaceous

“…Challenges exist to constrain the concentration and 87 Sr/ 86 Sr ratio of the modern global dissolved riverine input due to the complexity of lithology, bedrock age, climate, and weathering history within individual drainage basins (Palmer and Edmond, 1989;Vance et al, 2009;Allegre et al, 2010;Krabbenhoft et al, 2010;Peucker-Ehrenbrink et al, 2010;Luo et al, 2014;Voss et al, 2014;Pearce et al, 2015). Riverine Sr concentrations can vary over three orders of magnitude from <0.1 µmol/L to >100 µmol/L (Palmer and Edmond, 1989;Krabbenhoft et al, 2010;Voss et al, 2014;Pearce et al, 2015).…”

“…Riverine Sr concentrations can vary over three orders of magnitude from <0.1 µmol/L to >100 µmol/L (Palmer and Edmond, 1989;Krabbenhoft et al, 2010;Voss et al, 2014;Pearce et al, 2015). Within a single river, Sr concentrations can vary seasonally from less than a factor of two up to an order of magnitude (Bagard et al, 2011;Luo et al, 2014;Voss et al, 2014;Chapman et al, 2015). The 87 Sr/ 86 Sr ratio of the global riverine input largely reflects three-component mixing between young mafic rocks (basalt), old felsic rocks (granites), and marine carbonates.…”