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all but a handful of sites. There is an outstanding need to better quantify the volume of contributions from all hydrologic components in this dynamic climate on the regional scale where humans utilize water resources, and where future management decisions must be made. Only initial attempts have been made to account for the regional flux of hydrologic components in the valleys of the tropical Andes, utilizing major simplifying assumptions for lack of empirical data. It has proven very challenging to maintain regular meteorological observations due to human disturbance and technical issues in the extreme environment (Georges and Kaser, 2002). Groundwater and evaporation have been assumed negligible in glacierized valleys, given high relief and steep slopes (Caballero et al., 2004; Kaser et al., 2003). The hydrological processes in these high tropical mountain valley deposits remain understudied, and there is a need for systematic research to better understand the impact of runoff down valley by different morphological zones (Caballero et al., 2002). The hydrologic balance of tropical glaciers at various time scales (Hastenrath and Ames, 1995; Kaser et al, 2003; Francou et al., 2000; Francou et al., 2003) has been the focus of recent research, but measurements and model simulations of the role of evapotranspiration (ET) in the pro-glacial valleys are lacking. The low barometric pressure in high elevations promotes ET, but incident solar radiation, wind, humidity, precipitation and temperature are primary regulating components of meteorological forcing. Studies of mid-latitude pro-glacial valleys suggest significant contributions of ET to the hydrologic balance. For example, Konzelmann et al. (1996) found that the type of vegetation and surface texture strongly control the rate of ET at different elevations in the Dischma valley, near Davos, Switzerland. Konzelmann et al. concluded that ET in this alpine valley was regulated by soil moisture and the physiological behavior of the vegetation. However, the influence of soil, vegetation, and local meteorological forcing on ET in tropical pro-glacial valleys is largely unverified and assumed negligible. Current ground-based meteorological observations in the Peruvian Andes, such as Hardy et al. (1998) and Vuille et al. (2003) do not extend to pro-glacial valleys, so it is necessary to develop and deploy a new measurement network. ET is largely controlled by a combination of available surface moisture, atmospheric vapor pressure, air temperature and wind speed. Vuille et al. (2003) report significant increases in near-surface air temperature throughout most of the tropical Andes. Interestingly, the temperature increase varies markedly between the eastern and western Andean slopes with a much larger temperature increase to the west. In this paper, we introduce a new network of monitoring instruments from the northeastsouthwest trending Llanganuco pro-glacial valley of the western Cordillera Blanca, and report on model estimations of ET. We present data for dry and wet periods from a full annual cycle (2004- 2005) and report on the sensor network design, including a transect of automatic temperature sensors ranging from about 3500 to 4700 m. We applied the Penman-Monteith FAO method of estimating hourly potential ET (ET0) during the wet and dry periods. We ran a process-based water balance model (Brook90: Federer, 2003) to examine the influence of meteorological forcing on ET rates and compare the contributing sources of ET, and made comparisons with the ET0 estimations. Unlike most research on processes affecting ET, which targets mid-latitude and subtropical sites, we present methods and results for a hydroclimatologically sensitive region at the tropical-sub-tropical interface, the outer tropics. Study area The Andean Cordillera Blanca is home to the greatest concentration of tropical glaciers on earth (Fig. 1). It is the largest and most northerly mountain range in Peru, trending NW-SE over 130 km between 8º–10º S latitude (Ames, 1998) along the Andean continental divide. Most of the glacierized area in the Cordillera Blanca discharges northwest via the Santa River, that has the least variable monthly runoff of all Pacific draining rivers. 264
Figure 1. Cordillera Blanca regional map. The Llanganuco is one of several pro-glacial valleys in the region. The Llanganuco valley is a classic U-shaped hanging valley tributary draining SW to the Santa River (Figs. 2 and 3). Its mouth is flanked by steep walls of the glacially sculpted granodiorite bedrock that comprises the Upper Miocene batholithic core of the range (McNulty et al., 1998). Summits that border the catchment include Huascarán (6768 m) to the south, highest in Peru, the Huandoy massif (6395 m) to the north, and Chacraraju (6113 m) at the NE valley head. The valley contains two lakes, and is a well-visited tourist attraction within the Huascarán National Park and International Biodiversity Reserve. The road along the long axis of the valley forms one of three principal transect routes over the Cordillera Blanca and reaches a high pass at the Portachuelo de Llanganuco (4767 m) and it continues down the east side. 265
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Proceedings of the 63rd ANNUAL EAST
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FOREWORD T his proceedings volume c
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CONTENTS Foreword..................
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STATEMENT OF PURPOSE The Eastern Sn
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EXECUTIVES FOR THE 63rd EASTERN SNO
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THE PRESIDENT’S PAGE The 63rd ann
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Weisnet Medal for Best Student Pape
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3 63 rd EASTERN SNOW CONFERENCE New
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Figure 1. Layer 1 represents the so
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Figure 4. The general layout of the
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lue color represented no convection
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Total Density of Water Profiles The
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Figure 11(a). Simulated snow grain
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Jordan R, 1991. A one-dimensional t
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Campbell Scientific Award for Best
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19 63 rd EASTERN SNOW CONFERENCE Ne
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R ∑i ∑ n 2 = 1 NS = − n i = 1
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Snow and Climate 37
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Spatial distributions of changes in
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Snow and Climate Posters 43
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Figure 2 presents correlation maps
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CONCLUSIONS Three regional-continen
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Discharge (mm) 20 18 16 14 12 10 8
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ABSTRACT 55 63 rd EASTERN SNOW CONF
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This paper analyzes the synoptic pa
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Cyclones that track west of the App
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The synoptic-scale atmospheric circ
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CONCLUSIONS The record snowfall in
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correlations between April-May snow
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Figure 3. Linear correlations betwe
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winter/early spring could contribut
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Snow Remote Sensing 73
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height averaged 11.4 m with an aver
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strings were buried 20 - 30 cm belo
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Although the λE/Rn fraction was on
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estimated snow depth based on the 2
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important to note that the average
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Schmidt, R. A., C. A. Troendle, and
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METHODS The IMS Product The IMS was
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Figure 1. Microwave spectral charac
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snow depth and SWE on a weekly basi
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Figure 4. Example of blended SWE pr
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Evaluation of the global distributi
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Figure 9. Inter-comparison plots of
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Helfrich, S.R., D. McNamara, B.H.Ra
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105 63 rd EASTERN SNOW CONFERENCE N
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and validated regionally so they ca
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109 Test Site Figure 2. Variation o
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Correlation Coe. Correlation Coe. C
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Figure 8. SSM/I scattering signatur
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Considering the facts mentioned abo
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Besides the temporal validation, th
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RMSE Non linear Azar Chang Goodison
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63 nd EASTERN SNOW CONFERENCE Newar
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http://www.ccin.ca); from simulatio
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over the period 1988-2000. With the
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Figure 3: Explained variance (R 2 )
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correspondence between simulated an
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values. Continued development of ne
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National Climatic Data Center (2005
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Snow Remote Sensing Posters 135
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ABSTRACT 63 rd EASTERN SNOW CONFERE
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day and has a mean pixel resolution
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Table 1. Wheaton River basin EASE-G
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The SSM/I snowmelt onset algorithm
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coarse-resolution pixel with the hi
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Figure 5. (a) Scatterplot of snowpa
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For both 2004 and 2005, the AMSR-E
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threshold of ±18 K that reflects t
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ABSTRACT 153 63 rd EASTERN SNOW CON
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DATA USED SSM/I & QuikSCAT Coverage
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180 160 140 120 100 80 60 40 20 0 1
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independent of regions. This greatl
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slightly vary the IMS with this pro
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imagery, the higher latitudes rely
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MODIS Land Science Team, NASA Godda
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FUTURE OF IMS Enhancements to the I
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information never present before on
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Brubaker, K.L., R. Pinker and E. De
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The Sierra Nevada del Cocuy region
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Colombia Venezuela Glacier Series R
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Table 4. Glacier Areas of the Ruiz-
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Pico Bonpland Massif-Sinigüis Glac
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Linder W, Jordan E, 1991. Ice-mass
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Snowpack Processes 193
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63 rd EASTERN SNOW CONFERENCE Newar
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In the following paragraph the main
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Figure 1: Variation of the season a
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Figure 3: 8-day composite maps (24
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The third pair (Figure 5) represent
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Figure 9: Time evolution of SWE ave
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melting occurs, whereas at the high
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Colbeck SC, Anderson EA. 1982. The
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ABSTRACT 211 63 rd EASTERN SNOW CON
Page 225 and 226: A B Figure 1. Low-magnification sec
Page 227 and 228: GB ridge GB groove Figure 3. Higher
Page 229 and 230: CONCLUSION Figure 5. Indexed electr
Page 231 and 232: 219 63rd EASTERN SNOW CONFERENCE De
Page 233 and 234: Meteorological data for the winter
Page 235 and 236: monthly probability adjusted data 4
Page 237 and 238: 225 Pullman WA Rawlins WY Leadville
Page 239 and 240: The daily wind speed can exceed 6.5
Page 241 and 242: NCDC. 2006. National Climate Data C
Page 243 and 244: ABSTRACT 231 63 rd EASTERN SNOW CON
Page 245 and 246: and mass balances for 540 environme
Page 247 and 248: Temperature, precipitation, windspe
Page 249 and 250: the left in response to snow compac
Page 251 and 252: Pinched-cone dimensions for each sl
Page 253 and 254: Terrain slope (degrees) Terrain slo
Page 255 and 256: ACKNOWLEDGEMENTS This work was fund
Page 257 and 258: Glacial and Periglacial Processes 2
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Page 261 and 262: From linear regression the constant
Page 265 and 266: DATA COLLECTION Figure 1. Location
Page 267 and 268: Table 1. Comparison of GPS measured
Page 269 and 270: Transverse Velocity Profiles Surfac
Page 271 and 272: is shown in Figure 4. This variatio
Page 273 and 274: Table 4. The calculated volume flux
Page 275: 263 63 rd EASTERN SNOW CONFERENCE N
Page 279 and 280: MATERIALS AND METHODS Field Measure
Page 281 and 282: Data analysis techniques We synthes
Page 283 and 284: season, but unacceptable for the dr
Page 285 and 286: significant, although more informat
Page 287 and 288: (a) Liquid Water (mm) Dry Period: M
Page 289 and 290: Future Work We are installing addit
Page 291 and 292: Shuttleworth, W.J., and J.S. Wallac
Page 293 and 294: Snow and Periglacial Processes Post
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Page 299 and 300: No one to date has shown why snowfl
Page 301 and 302: APPENDIX A Northern Hemisphere Year
Page 303 and 304: 62nd ESC Papers 291
Page 305 and 306: 62 nd EASTERN SNOW CONFERENCE Water
Page 307 and 308: each other; and, they both decrease
Page 309 and 310: 297 62 nd EASTERN SNOW CONFERENCE W
Page 311 and 312: comes in the form of precipitation.
Page 313 and 314: averaged to reduce bias in this var
Page 315 and 316: RESULTS Figure 2. Flow chart of reg
Page 317 and 318: Table 6: Actual-Conditions SWE, dep
Page 319 and 320: 307 Table 9: Regression results bet
Page 321 and 322: Goita, K., A. Walker, B. Goodison,
Page 323: TO ERR IS HUMAN, TO FORGET IT WOULD
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