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Jie Li, Tao Tao, Zhonghe Pang, Ming Tan, Yanlong Kong, Wuhui Duan, and Yuwei Zhang

, respectively. The samples were transported to the laboratory and stored in refrigeration at 4°C before analysis. Fig . 3. The 24-h accumulated rainfall (mm), ending at 0800 LT 22 Jul 2012 [modified after Zhang et al. (2013) ]. The black box represents Shihua Cave, our sampling site. Stable isotopes were analyzed with a Picarro L2130-i laser absorption water isotope spectrometer in the Key Laboratory of Tibetan Environment Changes and Land Surface Processes, Institute of Tibetan Plateau Research, Chinese

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Catherine L. Muller, Andy Baker, Ian J. Fairchild, Chris Kidd, and Ian Boomer

to tropical rainfall, the multiscale influences on the isotopic composition of midlatitude precipitation do not lend themselves well to univariate regression analysis because different processes can dominate the isotope signature at different spatiotemporal scales; for example, the air mass may have an opposing influence compared to within-event and life cycle effects ( Berkelhammer et al. 2012 ; Sturm et al. 2010 ). This has resulted in difficulties in calibrating isotopic records. Studies of

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Youjie Wu, Taisheng Du, Risheng Ding, Ling Tong, Sien Li, and Lixin Wang

Occasional Publication 3, University of Rhode Island, 277–374 . Dirmeyer, P. A. , and Brubaker K. L. , 2007 : Characterization of the global hydrologic cycle from a back-trajectory analysis of atmospheric water vapor . J. Hydrometeor. , 8 , 20 – 37 , doi: 10.1175/JHM557.1 . Dubbert, M. , Cuntz M. , Piayda A. , Maguás C. , and Werner C. , 2013 : Partitioning evapotranspiration—Testing the Craig and Gordon model with field measurements of oxygen isotope ratios of evaporative fluxes . J

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Tim Kerr, M. S. Srinivasan, and Jeremy Rutherford

characterization efforts have been carried out in the glacierized regions of the Southern Alps ( Anderton 1976 ; Purdie et al. 2010 ; Ruddell and Budd 1990 ). Anderton (1976) found seasonal variations of 18 O concentrations in snow, precipitation, stream water, and spring water in a glacier-dominated Southern Alps catchment with winter water more depleted in 18 O than summer water. A more extensive analysis of alpine isotope concentrations was carried out by Ruddell and Budd (1990) to assess the value

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Heather Guy, Anton Seimon, L. Baker Perry, Bronwen L. Konecky, Maxwell Rado, Marcos Andrade, Mariusz Potocki, and Paul A. Mayewski

essential to understand the controls on modern-day subseasonal spatiotemporal variability of precipitation isotopes, and whether or not these signals are preserved in the ice. In response to these current limitations and opportunities in the analysis of tropical Andean ice cores, the goals of this study are to 1) to identify subseasonal signals of isotopes in precipitation on the northeastern flank of the Altiplano, and their spatiotemporal characteristics, 2) to determine the dominant meteorological

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Huancui Hu and Francina Dominguez

. In the southwestern United States, measurements of δ D in water vapor during one premonsoon period show that most of the isotopic variability can be associated with changes in the advection of atmospheric moisture from different source regions ( Strong et al. 2007 ). In their study, Strong et al. (2007) show that periods of high δ D are linked to precipitation originating from the Gulf of Mexico, while low δ D values originate from the Pacific. Similarly, in an analysis of isotopic

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G. W. K. Moore, Robert D. Field, and Carl S. Benson

Gedzelman and Lawrence (1990) using an isotopically equipped regional climate model to interpret a similarly large isotopic shift in precipitation over the eastern United States. Given the magnitude of the observed isotopic shift during the event, the 1980 case study for Mount Wrangell considered here is another strong candidate for more detailed analysis, given the importance of the region for reconstructing North Pacific climate variability using isotopic proxies. In that context, this case study

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Shengjie Wang, Mingjun Zhang, Yanjun Che, Xiaofan Zhu, and Xuemei Liu

Normal University. Every sample and isotopic standard was injected sequentially six times, with the first two injections discarded because of memory effects, and the results were expressed as δ values relative to Vienna Standard Mean Ocean Water (VSMOW). The measurement precision is ±0.6‰ for δ D and ±0.2‰ for δ 18 O. More information on sampling and sample analysis is given in Wang et al. (2016) . b. Method Influenced by below-cloud evaporation of raindrops, the stable isotopic ratios in

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Huancui Hu, L. Ruby Leung, and Zhe Feng

only viable approach for quantifying how MCS and non-MCS rainfall influence the surface water budget components. This is because stable water isotope tracers are sparsely observed in space and time, so they are incapable of providing event-scale water transit characteristics over a large area to be climatologically relevant ( McGuire and McDonnell 2007 ). In this study, the water tracer enabled version of the Noah land surface model with multiparameterization options (WT-Noah-MP; Niu et al. 2011

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Wenyi Xie, Xiankui Zeng, Dongwei Gui, Jichun Wu, and Dong Wang

, literature, or an optimization procedure ( Panday et al. 2014 ; J. L. Zhang et al. 2016 ; Zhang et al. 2007 ). However, it is difficult to accurately define or calibrate these parameters for high-dimensional and complex hydrological models, particularly when limited observation data are available. Therefore, the routing results will inevitably be uncertain when using an optimized parameter set solely. To resolve this problem, we calibrated these parameters through Bayesian uncertainty analysis, that is

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