The use of temperature and the isotopes of O, H, C, and noble gases to determine the pattern and spatial extent of groundwater flow

James, Elizabeth R.; Manga, Michael; Rose, Timothy P.; Hudson, G. B.

doi:10.1016/s0022-1694(00)00303-6

Cited by 81 publications

(80 citation statements)

References 43 publications

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“…Their intercept of À10.57% was also lower than ours (À8.1%) and from Corvallis precipitation (À9.1%), while the isotope values at 1800 m elevation overlapped those we found. James et al (2000) constructed an elevation isotope relationship for snow collected in the High Cascade Mountains (both east and west side). Similar to Jefferson et al, their intercept and slope (À10.9% km À1 and À1.8% km À1 , respectively) were less than ours but values predicted at high elevation (2000 m) were similar between our regression and theirs.…”

Section: Seasonal Variation In (A) Dmentioning

confidence: 99%

“…Because James et al (2000) only measured snow, their lowest elevation was 1200 m, and they included samples from the east side of the Cascades which would be expected to have a different rainout affect than the west side used in our study. The Jefferson et al (2006) lapse rate was also determined with data mainly from higher elevation sites using only a few groundwater wells below 500 m. Because the isotopic values of water from these low elevation wells were more depleted in the heavy isotopes than that of Corvallis precipitation and low elevation surface water, the sources of their low elevation well water likely included water from higher elevations than the elevation of the well (James et al 2000). Based on our elevation regression model, we estimate that water in those wells below 500 m that Jefferson et al used likely had a water-source elevation between 750 and 1000 m.…”

Section: Seasonal Variation In (A) Dmentioning

confidence: 99%

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Willamette River Basin surface water isoscape (δ¹⁸O and δ²H): temporal changes of source water within the river

et al. 2012

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Citation: Brooks, J. R., P. J. Wigington, Jr., D. L. Phillips, R. Comeleo, and R. Coulombe. 2012 H) of river and stream water within the southern Willamette River Basin in western Oregon over two years. Within this basin, eighty-four percent of the isotopic variation in small tributary streams was explained by the mean elevation of the catchments, whereas seasonal variation was minimal. However, water within the Willamette River had distinct isotopic seasonal patterns that likely occurred because of changes in the mean elevation of source water for the river. River isotopic values were lowest during summer low flow and highest during February/March when snow accumulated in the mountains. We estimated that the mean elevation of the source water for the Willamette River shifted over 700 m, seasonally. During winter when rain occurred in the valley and snow accumulated in the mountains, the river reflected a mixture of low mountains and valley bottom precipitation. During the dry Mediterranean summer, 60-80% of the river water came from the snow zone above 1200 m, which is only 12% of the land area and accounts for 15.6% of the annual precipitation within the Willamette Basin. This high elevation area contains the High Cascades geological region with highly permeable bedrock that sustains latesummer baseflow compared to the Western Cascades with low permeable bedrock. Reliance on highelevation water during summer low flow highlights the vulnerability of this system to influences of a warming climate, where snowpacks in the Cascade Mountains are predicted to decrease in the future.

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Section: Seasonal Variation In (A) Dmentioning

confidence: 99%

Section: Seasonal Variation In (A) Dmentioning

confidence: 99%

Willamette River Basin surface water isoscape (δ¹⁸O and δ²H): temporal changes of source water within the river

et al. 2012

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“…Manga (1998) and James et al (2000) propose calculating the thermal energy from the di¡erence in discharge and recharge temperatures (using isotopes to determine recharge elevation) and then go on to assign the source of the thermal energy to geothermal heating. However, the temperature of the ground surface is determined by a balance between incoming solar energy and the outgoing ground radiation (Watson, 1975).…”

Section: Temperature Chemistry and Isotopes Of Springsmentioning

confidence: 99%

“…For example, for a heat £ux into the ground of 30 mW/m 2 and a thermal conductivity for andesite of 3 W/(m K), the temperature di¡er-ences between the surface and water £owing in the ground need only be 0.2, 1, 2, and 3 ‡C at depths of 20, 100, 200, and 300 m. McCloud River Spring is cooler than air temperature at its discharge elevation by about 3 ‡C, and it could be receiving signi¢cant thermal energy during its £ow from high to low elevation. The addition of thermal energy to the ground surface from solar energy may explain the calculations of James et al (2000) requiring the capture of all conductive heat £ow in the recharge area to add the thermal energy necessary to obtain the measured temperature of the Metolius River. For most purposes, the calculation of thermal energy is more appropriately done using the temperature of the spring di¡erenced from a reference temperature for springs at the same elevation that do not appear to be anomalous.…”

Section: Temperature Chemistry and Isotopes Of Springsmentioning

confidence: 99%

Slightly thermal springs and non-thermal springs at Mount Shasta, California: Chemistry and recharge elevations

Nathenson

Thompson

White

2003

Journal of Volcanology and Geothermal Research

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Temperature measurements, isotopic contents, and dissolved constituents are presented for springs at Mount Shasta to understand slightly thermal springs in the Shasta Valley based on the characteristics of non-thermal springs. Non-thermal springs on Mount Shasta are generally cooler than mean annual air temperatures for their elevation. The specific conductance of non-thermal springs increases linearly with discharge temperature. Springs at higher and intermediate elevations on Mount Shasta have fairly limited circulation paths, whereas low-elevation springs have longer paths because of their higher-elevation recharge. Springs in the Shasta Valley are warmer than air temperatures for their elevation and contain significant amounts of chloride and sulfate, constituents often associated with volcanic hydrothermal systems. Data for the Shasta Valley springs generally define mixing trends for dissolved constituents and temperature. The isotopic composition of the Shasta Valley springs indicates that water fell as precipitation at a higher elevation than any of the non-thermal springs. It is possible that the Shasta Valley springs include a component of the outflow from a proposed 210 ‡C hydrothermal system that boils to supply steam for the summit acid-sulfate spring. In order to categorize springs such as those in the Shasta Valley, we introduce the term slightly thermal springs for springs that do not meet the numerical criterion of 10 ‡C above air temperature for thermal springs but have temperatures greater than non-thermal springs in the area and usually also have dissolved constituents normally found in thermal waters. ß

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“…Bounded by Taihang Mountain to the west, Yanshan Mountain to the north, the Bohai Sea to the east, and the Yellow River to the south, the plain is a faultsubsidence basin with Quaternary sediment about 400-600 m thick. Rivers include the Yellow River and the GROUNDWATER FLOW IN THE NORTH CHINA PLAIN 3135 Katz et al, 1997;James et al, 2000). Surface water usually has an isotopic signature resulting from evaporation.…”

Section: Introductionmentioning

confidence: 99%

Spatial geochemical and isotopic characteristics associated with groundwater flow in the North China Plain

Chen

Tang

Sakura

et al. 2004

Hydrological Processes

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Abstract:The North China Plain (NCP) is an important agricultural area in China and has a high population density. Serious water shortages have occurred in this region over the last 20 years. Water transfer from the Yangtze River (the east route) was initiated in the year 2002 to provide water for the major cities of the NCP. This study was carried out before the implementation of the water transfer project, focusing on the spatial integration of the groundwater flow system and geochemical characteristics, which are mainly controlled by tectonics, geomorphology, and lithology. The field survey and the geochemical analyses of the groundwater samples indicated that the groundwater in the NCP has a two-layer structure, with a boundary at a depth of about 100-150 m. The two layers differ in pH, concentrations of SiO 2 and major ions, and isotopes ( 18 O, deuterium and tritium (T)). Chemical components in the upper layer showed a wider range and higher variability than those in the lower layer, indicating the impact of human activity. The flow direction of the groundwater in the upper layer was examined in detail in two profiles, showing that the upper layer flows east towards the Cangzhou-Daming fault, while the groundwater in the lower layer flows northeast towards Tianjin. Three hydrogeological zones are identified: recharge (Zone I), intermediate (Zone II), and discharge (Zone III). The recharge zone was found to be low in chloride (Cl ) but high in T. The discharge zone was found to be high in Cl and low in T. This may be due to the difference in groundwater age. The discharge zone was subdivided into two sub-zones, Zone III 1 and Zone III 2 , by considering the effects of human activities. Zone III 2 was strongly affected by water diversions from the Yellow River. As groundwater flows from the recharge zone to the intermediate and discharge zones, chemical patterns evolve in the order: Ca-HCO 3 > Mg-HCO 3 > Na-Cl C SO 4 .

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The use of temperature and the isotopes of O, H, C, and noble gases to determine the pattern and spatial extent of groundwater flow

Cited by 81 publications

References 43 publications

Willamette River Basin surface water isoscape (δ¹⁸O and δ²H): temporal changes of source water within the river

Willamette River Basin surface water isoscape (δ¹⁸O and δ²H): temporal changes of source water within the river

Slightly thermal springs and non-thermal springs at Mount Shasta, California: Chemistry and recharge elevations

Spatial geochemical and isotopic characteristics associated with groundwater flow in the North China Plain

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The use of temperature and the isotopes of O, H, C, and noble gases to determine the pattern and spatial extent of groundwater flow

Cited by 81 publications

References 43 publications

Willamette River Basin surface water isoscape (δ18O and δ2H): temporal changes of source water within the river

Willamette River Basin surface water isoscape (δ18O and δ2H): temporal changes of source water within the river

Slightly thermal springs and non-thermal springs at Mount Shasta, California: Chemistry and recharge elevations

Spatial geochemical and isotopic characteristics associated with groundwater flow in the North China Plain

Contact Info

Product

Resources

About

Willamette River Basin surface water isoscape (δ¹⁸O and δ²H): temporal changes of source water within the river

Willamette River Basin surface water isoscape (δ¹⁸O and δ²H): temporal changes of source water within the river