Delineation of Recharge Areas for Karst Springs in Logan Canyon, Bear River Range, Northern Utah
Delineation of Recharge Areas for Karst Springs in Logan Canyon, Bear River Range, Northern Utah
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犹他州北部熊河山脉洛根峡谷喀斯特泉补给区划定
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发表时间：
2001
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影响因子：
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通讯作者：
L. Spangler
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作者：
L. Spangler
使用荧光染料示踪技术确定了犹他州北部熊河山脉洛根峡谷地区四个岩溶泉水的补给区域、地下水的大致流向和停留时间。DeWitt、Wood Camp Hollow、Logan Cave和Ricks Springs从古生代碳酸盐岩排放到洛根河，这是从这个高山地区排放地下水的基准面。碳酸盐含水层的补给通过点源、通过河流冰川沉积的渗漏损失和扩散渗透发生。根据到目前为止(1999年)的染料追踪，杜威特、伍德坎普山谷和瑞克斯泉的补给区域估计在7.5至15平方英里之间，比泉水的海拔高出3200英尺。染料追踪的结果表明，从失去的溪流到7.2英里远的地方，地下水的最长旅行时间为8到31天。染料追踪还表明，地表水排水盆地通常与地下水盆地不重合。该地区大部分地区的地下水运动受洛根峰向斜的影响。弹簧的流量从小于1立方英尺每秒到约75立方英尺每秒。春季径流主要对融雪径流作出响应，高峰流量出现在春末夏初，基流量出现在冬季。在25摄氏度下，1994年5月至1997年7月泉水的比导为每厘米250至420微西姆，水温为5.5至8.0摄氏度。对于所有的弹簧，比电导和温度与流量呈负相关。观测到的测量值之间的差异主要是由于融雪产生的补给与地下水的混合造成的。
Fluorescent-dye tracing was used to determine recharge areas, general directions of ground-water flow, and residence times for water from four karst springs in the Logan Canyon area of the Bear River Range in northern Utah. Dewitt, Wood Camp Hollow, Logan Cave, and Ricks Springs discharge from Paleozoic-age carbonate rocks into the Logan River, which is base level for ground water that discharges from this alpine region. Recharge to the carbonate aquifer occurs through point sources, as seepage losses through fluvioglacial deposits, and as diffuse infiltration. On the basis of dye tracing to date (1999), recharge areas for Dewitt, Wood Camp Hollow, and Ricks Springs are estimated to be between 7.5 and 15 square miles and as much as 3,200 feet higher than the altitude of the springs. Results of dye tracing indicate maximum ground-water travel times of 8 to 31 days from losing streams as far as 7.2 miles. Dye tracing also indicates that surface-water drainage basins generally do not coincide with ground-water basins. Ground-water movement in a large part of the area is influenced by the Logan Peak syncline. Discharge of springs ranges from less than 1 to about 75 cubic feet per second. Spring discharge responds primarily to snowmelt runoff, with peak flow from late spring to early summer and base flow during the winter months. Specific conductance of spring water from May 1994 to July 1997 ranged from 250 to 420 microsiemens per centimeter at 25 degrees Celsius and water temperature ranged from 5.5 to 8.0 degrees Celsius. For all springs, specific conductance and temperature were inversely related to discharge. Observed differences between measured values result primarily from mixing of recharge derived from snowmelt with ground water.