『Abstract
　Solute yields, laboratory dissolution data and both chemical and isotopic markers of rock weathering reactions are used to characterise the biogeochemistry of glacial meltwaters draining a maritime Antarctic glacier. We find that delayed flowpaths through ice-marginal talus and moraine sediments are critical for the acquisition of solute from rock minerals because delayed flowpaths through subglacial sediments are absent beneath this small, cold-based glacier. Here the mechanisms of weathering are similar to those reported in subglacial environments, and include sub-oxic conditions in the early summer and increasingly oxic conditions thereafter. Up to 85％ of the NO3^- and 65％ of the SO4^2- are most likely produced by bacterially mediated reactions in these ice marginal sediments. However, reactive pyrite phases are sparse in the host rocks, limiting the export of Fe, SO4^2- and cations that may be removed by weathering once pyrite oxidation has taken place. This means that dissolution of Ca²⁺ and Na⁺ from carbonate and silicate minerals dominate, producing moderate cationic denudation yields from Tuva Glacier (163 Σ^*meq⁺ m^-2 a^-1) compared to a global range of values (94-4,200 Σ^*meq⁺ m^-2 a^-1). Overall, crustally derived cations represent 42％ of the total cationic flux, the rest being accounted for by snowpack sources.

Keywords: Antarctica; Chemical denudation; Glacial meltwater; Rock-water interaction』

Introduction
Field site
Methods
　Hydrochemical sampling
　Stable isotope sampling
　Hydrological monitoring
　Dissolution experiments
　Analytical methods
　Stable isotope analysis
　Correction of δ¹⁸ONO3 for organic matter
　Correction for marine salts
Results
　Non-snowpack solute transfer
　Cation composition
　Major anion composition and CO2 partial pressures
　Nitrogen biogeochemistry
　Chemistry and stable isotopes of C,N,O and S
Discussion
　Seasonal melting, flowpaths and the concentrations of non-snowpack ions
　Carbonate weathering and its coupling to pyrite oxidation
　Fe and ^*SO4^2- liberation: fingerprints of microbial weathering?
　Microbial processes and the provision of non-snowpack N
　Rock weathering yields
Conclusions
Acknowledgments
References