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Quantifying the Spatial Variations of Hyporheic Water Exchange at Catchment Scale Using the Thermal Method: A Case Study in the Weihe River, China.

1. Introduction

A hyporheic zone is an active ecotone which connects the surface water and groundwater [1]. It is characterized by the hydrological, chemical, biological [2], hydrogeological [3], and biogeochemical features [4]. Studies of hyporheic zones have been significantly increased in recent years (Figure 1).

Water exchange is a fundamental interest in the energy transport of a hyporheic zone [5]. That is associated with the substantial transient including heat and dissolved and suspended substances, as well as physicochemical processes [1,6,7]. The spatiality of water exchange at the stream-aquifer interface has important implications for the fate and transport of contaminants in river basins [8]. Therefore, hyporheic water exchange (HWE) provides hydrogeological information about the interactions between groundwater and surface groundwater, whose function is crucial to the overall riverine ecosystem.

However, the interaction between groundwater and surface water has been regarded as two distinct entities and focused on the distinction of within system and inner single objects for a long period [9]. In reality, interactions in this zone are more complex and have the importance of the water quality [10,11]. This process is influenced by the spatial variation of hydrologic conditions such as topographic relief and regional scale [12]. An accurate estimate of HWE at catchment scale is challenging, in terms of hydrological heterogeneity [1, 13-15]. Therefore, the new sight to couple groundwater and surface water as an integrated system to estimate the water exchange is essential for the management of fluvial and lotic systems.

Numerous methods have been used to assess stream and groundwater interaction [16]. They can be classified into seepage meters, hydrological elements, numerical model, remote sensing, and tracer method. The bag-type seepage meter has been widely used to estimate water exchange in lakes, estuaries, reservoirs, and streams [17]. But the seepage meter's success has been limited by operational problems during field work [18]. Water velocity can be deducted using solute travel time and distance data. The relationship between water temperature and the water velocity has been used to calculate the water exchange from the groundwater into streams [13]. The application of contaminants modeling has developed the theory and simulation technique [19, 20]. Remote sensing provides the new approach to investigate the water exchange [21]. New technologies are increasingly used to measure HWE such as distributed temperature sensing [22, 23]. The tracer method, such as calcium chloride, salt, and dye, has frequently been used to estimate the water exchange in hyporheic zone [16]. Heat, as a natural tracer, has been used to simulate HWE owing to temperature distribution; on the one hand, it is the result of heat conduction in the subsurface, but also it is the consequence of the advection movement of water through the porous medium [24]. Hence water fluxes between groundwater and surface water can be estimated by measuring temperature distributions within the coupled systems [25,26]. However, studies using heat as a water exchange estimator have mainly measured temperature within a single stream or in one segment of a river. The water exchange in a hyporheic zone at catchment scale is poorly understood and needs further investigation. Moreover, for the Weihe River, which is long and crosses different topographic classes, interactions between the surface water and groundwater in the mainstream channel and its tributaries have been relatively unknown.

Using heat as a tracer to investigate HWE in the Weihe River extends the application of the thermal method to the catchment scale. The principal foci of this study are to investigate the water exchange across the large basin scale and find the relationship between the exchange and the spatial distribution of rivers. The objectives of the paper are (1) to detect patterns of water exchange in the hyporheic zone, (2) to quantify the rate of hyporheic water exchange, and (3) to describe the spatial variability of HWE at catchment scale.

2. Study Area Description

As the largest tributary of the Yellow River, the Weihe River plays a vital role in water supply and agricultural development in Guanzhong Basin. The Weihe River originates from Gansu Province, China, from where it flows eastward through Shaanxi Province, and, at Tongguanxian in the east of Shaanxi Province, it merges into the Yellow River. The river has a total length of 818 km and a drainage area of 13.4 x [10.sup.4] [km.sup.2]. The whole river has a longitudinal inclination of about 1.7 [per thousand]. The drainage area and transportation of the sediments of this river account for 17.9% and 2.5% for the Yellow River [27], respectively. The Weihe River flows along the northern Qinling Mountains in Shaanxi Province, which have an altitude of 1500-3000 m.

Ten study sites across catchment were chosen for this study (Figure 2). Four sites are located along the main channel, while the rest of the tributaries are secondary and tertiary rivers. The Beiluo River is the largest tributary of the Weihe River. Some sites allocated in the southern tributaries are stemmed from Qinling Mountains. The climate and vegetation are distinctive on north and south sides; loess has preserved well on the eastern side [28]. Table 1 lists the testing sites and abbreviations in this study. At those sites, the components of the deposits along the study bank differ from fluvial sand, silt, clay, coarse-grained sediments, and gravels. During annual flood periods, which occur in late autumn, the river carries about two to three times more water than the average mean recharge.

3. Methods

3.1. Sediment Temperatures Collection. The measurements were taken during the summer of 2013. A two-meter thermal bar with a small flat plate at the upper end and a pointed tip at the bottom end (Figure 3) was utilized to measure sediments temperature. This design allows the thermistor to be inserted into the sediment easily. Measurements of streambed temperature were collected at multiple depths at each location (various depths: 0,0.1, 0.2, 0.35,0.5, and 0.7 m), the data were collected 15 minutes after the temperature kept stable, and then temperature profiles in the hyporheic zone were plotted.

Measurement of the sediment temperature was carried out along one side of the riverbank. Thus the field points were allocated to a relatively shallow area of the river. The distance interval between each point was about 10 meters. There was a range of around 1.5-meter distance away from the bank side of the river (Figure 3).

3.2. Water Exchange Modeling. The transportation of energy in the hyporheic zone involves sediment conductivities and water percolation [24]. Assuming the sediment has uniform distribution, and the water exchanges only occur in a vertical direction (upward or downward), the one-dimensional thermal equation can be used to calculate the water transfer as follows [29]:

K/[rho]c [[partial derivative].sup.2]T(z)/[partial derivative][z.sup.2] - v[[rho].sub.0][c.sub.0]/[rho]c dT(z)/dz = [partial derivative]T(z)/[partial derivative]t, (1)

where v is vertical water exchange in the sediments at depth z (mm/d), T(z) is the temperature ([degrees]C) of the streambed sediments at z-depth, and [rho]c and [[rho].sub.0][c.sub.0] are the volumetric heat capacity of saturated streambed system (J [m.sup.-3] [K.sup.-1]) and the volumetric heat capacity of the fluid (J [m.sup.-3] [K.sup.-1), respectively. Moreover, K is the thermal conductivity of the solid-fluid system (J [s.sup.-1] [m.sup.-1] [K.sup.-1]).

In thermal steady-state conditions, the right-hand of (1) tends to 0 and can be written as follows [18]:

[[partial derivative].sup.2]T(z)/[partial derivative][z.sup.2] - v[[rho].sub.0][c.sub.0]/K dT(z)/dz = 0. (2)

With the assumption that there is a quasi-constant groundwater temperature at depth and assuming the boundary conditions T = [T.sub.0] for z = 0, and a fixed temperature [T.sub.L] for z = L, the temperature profile can be fitted by the analytical steady-state solution of one-dimensional heat transport equation [24], then the solution of Eq. (2) can be written as:

v = [absolute value of K/[[rho].sub.0][c.sub.0]z ln T(z) - [T.sub.L]/[T.sub.0] - [T.sub.L]] (3)

Using this equation to quantify the vertical water exchange V (mm/d), the performance of this method has the following advantages: (1) it can be used with relatively small data; (2) it has high measurement efficiency in the field work [14]; (3) it was a steady-state thermal-flux model [18]. Considering the cost of data measurements in many locations, the ten sites across the large basin can provide catchment scale benefits.

3.3. Determination of Hyporheic Water Exchange Patterns. HWE patterns can be illustrated using a conceptually simplified diagram (Figure 4). The line "(a)" indicates the upward flux into the surface water; the line "(b)" shows the downward flux into the groundwater. The details of the conceptual diagram were described in some previous studies [18,26].

4. Results

4.1. Sediment Temperatures. The statistical analyses of the temperatures at different testing sites are shown in Figure 5. For the ten investigated sites, the maximum and the minimum temperatures of the sediment are 33[degrees]C and 18.2, respectively. The difference between the highest and lowest is 14.8[degrees]C. The average temperature difference between the upper layer and the deepest layer is 4[degrees]C. The maximum residual of the stratification sediment is 2.5[degrees]C, and the minimum of the residual is 0.07[degrees]C.

The average temperature of the deposits in the upper boundary is 28.1[degrees] C, while the temperature at the deepest depth is 24.1[degrees]C. The difference of temperature ranges from 8.9[degrees]C in MX to 2.5[degrees]C in LH.

4.2. Distribution of Temperatures. Figure 6 shows the variation of the temperature-depth profiles for the sediments in the different segments of the river. For the temperature-depth profiles at each testing site, the whole trend of changes is similar. However, the shape of the profiles displays a dissimilar tendency at certain depths. For instance, the profiles have relative tremendous changes in JH, HX, and TYH.

The results show a distinct gradient of temperature profiles among the testing sites. In the summer season, the diffusion of the temperature variations differs in the segments of the river; the sediment temperatures decreased as the water became deeper. Sediment temperature can be categorized into five classifications using the change of temperature gradient: (1) rivers that had an extreme change of the temperature including the HX and TYH; (2) rivers that had a moderate degree of the temperature changes including JH and BLH; (3) rivers that had good temperature profiles including HH and HSH; (4) rivers that had a weak changed profile including MX and LH; and (5) rivers that had a stable change profile, XA, and LT.

4.3. Hyporheic Water Exchange. The maximum rate of water exchange is 78.7 mm/d, which occurred in the HH, and the minimum of the median is 27.56 mm/d which occurs in JH, which is one of the second-order tributaries and is in the southern part of the Weihe River.

The water exchange along the Weihe River has apparent spatial variability from the upstream to downstream; the water exchange at MX in upstream location is close to two times greater than tributaries in middle reaches of the river such as the JH and TYH (Figure 7(a)).

Figure 7 shows the relationship between the HWE and the average temperature from the upstream to downstream. For the average temperature, the sediment temperature increased with the distance away from the upstream; however, the median of the water exchange was greater downstream. The spatial correlation coefficient R2 of the water exchange and average temperature is 0.62 and 0.84, respectively. We can find that the water exchange has a close correlation with the distance from the upstream. Secondly, the tributaries also had the same pattern on the southern river. Furthermore, all the testing sites were compared, and there is good agreement overall (Figure 7). The trend demonstrates the general distribution of water exchange in variations across the catchment.

5. Discussion

5.1. Temperature Spatiality. Temperature has increasing tendency from the upstream to downstream (Figure 7(b)). The hydrological heterogeneity leads to the spatial characteristics of different segments of the river. Spatial variations of the sediment could result in the spatial changes of the streambed temperature. Previous studies found that sediments structure has an impact on thermal transportation [30]. The sediment temperature is influenced by hydraulic conditions, sediments temperature with relevance to the conductivity of the heat transport of the fluid, and solid mixing textures. Additionally, the temperature of streambed sediments was affected by the changes in atmospheric temperature and radiation from the center of the earth and has the diurnal and seasonal variations [26]. For instance, the spatial structure of the microtopography from some transects in the catchment influenced the distributions of the elevation classes and affected the allocation of the temperature in the sediments [31]. Fluxes and residence times varied in different geomorphic features such as streams in mountain regions [20]. Moreover, some studies have investigated flow path status in the hyporheic zone; the exit and reenter phenomenon would take place within ten meters [32,33] and displayed that the variations of upward flux would influence the streambed temperatures measured over a short period at many locations [34].

In summary, the temperatures at the testing sites have the negative agreement with the depth. However, the temperatures have the apparent gradient oscillations in certain ranges. This range is mainly concentrated around a depth of 20 cm. In this case, the steady state of the heat transport is disturbed by the sediments properties and hydrologic conditions. The temperature in the sediments was not good satisfying the quasit-steady-state condition in these depth ranges. In those ranges, HWE would be more strongly influenced by water flowing from other directions or the heterogeneity of the sediment. This pattern of temperature distribution reflects the highly variable amplitude ratio values in this content. The complexity of geomorphic features in particular reaches caused a series of related complex flow pathways in the hyporheic zone, which means the water exchange varies in both magnitude and direction [35].

5.2. Hyporheic Water Exchange Patterns. Interactions between surface water and groundwater can be identified using a conceptual model (Figure 4). Generally, water interaction is mainly from groundwater to surface water.

HWE has the distributional patterns in space, the variables of the water exchange influence the inflows and outflows processes [36], and, to a great catchment scale, those hugely amplified the water exchange magnitude by even some orders. However, in this study, for the median of water exchange, the difference for the water exchange magnitude does not reach several orders. The maximum is about three times the minimum. The extreme values all exist in secondary tributaries of the river flowing in the mountains. This may be related to more complex morphologic attributes underlying the surface water.

5.3. Controlling Drivers of Hyporheic Water Exchange. The medians of HWE compared to the distance away from the upstream in space (Figure 7(a)). The water exchange in different stream reaches of the stream corresponds to the creek features from upstream to downstream.

Many factors are influencing the water exchange in the hyporheic zone, such as the hydraulic conductivity, sediment component, sediment grain size, and the discharge from the groundwater [37]. The spatial distribution of water exchange has a high correlation to the topographic patterns and the local space [38]. In the downstream reaches, other factors are controlling the HWE; for example, in meandering river channels, the horizontal flow through the streambed may be contributing to complex flow [35].

The hyporheic water exchange is associated with the local streambed attributes (i.e., sediment structure and topography) [6]. In hydrological processes, the heterogeneities of the sediments influence water exchange, and both the water exchange and other transient processes have a heterogeneous spatial distribution [39]. The deposit structure with the wood or other materials could create a heterogeneous streambed, the fine sediments of the streambed. Generally, the water exchange is relatively smaller than the heterogeneities of the streambed [40].

Vegetation is another driver influencing the water exchange in the hyporheic zone. There are relatively good vegetated plants around the Heihe environment; the plants are, especially, central great high trees. In summer, water head change is due to pumping function from vegetation [41].

It should be noted that the human constructions also influence the HWE processes. In TYH, the measurements of the location are about 50 meters from the dam, which has been blocked by fine silt and gravel. Therefore, in this environment, the hydraulic conductivity tends to be small, and the sediment has the uniform texture with little heterogeneity. As a result, HWE tends to be low. For some deposits with a particular volume close to surface water, there was no good steady state due to the sediments influenced by fluctuations from surface water flow. The exchange energy of HWE will control the water transfer pattern in the individual range [42]. Where there are variations at sites only in some meters apart, this probably represents outflow within the hyporheic zone [36]. If the water transfer occurs in fine-grained upper sediments, a shallow impermeable layer can be created and thus leads to the changes in water exchange patterns.

5.4. Hyporheic Water Exchange Scales. The HWE dimensional scales influence the spatial patterns of the river to some degree. The HWE can be categorized into two scales based on its driving processes, which are large-scale and small-scale [6]. Large-scale hydrological exchange results from the spatial and temporal differences between the stream and the surrounding groundwater levels. The small-scale exchange is mainly driven by the hydrologic flow conditions and the morphological features of the streambed [7]. For instance, the small slope and the irregular streambed of a riffle-pool sequence beneath the stream are not perceptible [20, 25], meaning the topographic changes in the streambed and the elevation of the surface water would lead to the surface water discharge and connect with groundwater [34]; these structures enhanced the complex dynamics between groundwater and surface water. Streambeds with highly permeable bed sediments have apparent vertical water exchange [36, 43]. In this study, the HWE has the same trend with the hydraulic conductivity in the main channel of the river.

Furthermore, the no-parameter test of Kruskal-Wallis was used to evaluate the difference between the HWE amount in the main channel and its tributaries. The P value of the water exchange magnitude was close to 0.4, and this highlights the spatial difference in the catchment.

6. Conclusions

The one-dimensional equation was used to estimate hyporheic water exchange and evaluate its spatial distribution in the Weihe River catchment. The thermal method is an easy, cheap, and robust way to obtain temperature variations. This approach provides spatial information that could be substantial when estimating the interaction between groundwater and surface water.

Our findings show that the hyporheic water exchange has spatial variations across the catchment. The exchange magnitude has a decreasing tendency from the upstream to downstream, which is controlled by the distance away from the downstream. The hyporheic water exchange trend has a consistency with the main river channel. The complexity of water exchange takes place in the southern tributaries in mountainous regions. The rate of the water exchange tends to be the underestimate because of only consideration in vertical fluxes. In the future investigation, some new parameters will be encouraged to improve the accuracy of the estimation on hyporheic water exchange.

https://doi.org/10.1155/2017/6159325

Conflicts of Interest

The authors declare that there are no conflicts of interest and funding regarding the publication of this paper.

Acknowledgments

This work was support by National Natural Science Foundation of China (Grant nos. 51379175 and 51679200), Specialized Research Fund for the Doctoral Program of Higher Education (Grant no. 20136101110001), Program for Key Science and Technology Innovation Team in Shaanxi Province (Grant no. 2014KCT-27), and The Hundred Talents Project of the Chinese Academy of Sciences (Grant no. A315021406). The authors thank Jiaxuan Li, Xiaojuan Li, Xiaogang Yang, and other members for assistance in field sampling and laboratory experiments.

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Junlong Zhang, (1) Jinxi Song, (1,2) Yongqing Long, (1) Yan Zhang, (1) Bo Zhang, (1) Yuqi Wang, (3) and Yuanyuan Wang (1)

(1) College of Urban and Environmental Sciences, Northwest University, Xi'an 710127, China

(2) State Key Laboratory of Soil Erosion and Dryland Farming on the Loess Plateau, Institute of Soil and Water Conservation, Chinese Academy of Sciences, Yangling 712100, China

(3) Fenner School of Environmental and Society, Australian National University, Canberra, ACT 2601, Australia

Correspondence should be addressed to Jinxi Song; jinxisong@nwu.edu.cn

Received 8 January 2017; Accepted 2 March 2017; Published 21 March 2017

Academic Editor: Xiaofeng Li

Caption: Figure 1: Number of citations of papers on hyporheic zone since 1997, based on a search in the ISI Web of Science (http://apps.webo&nowledge.com/CitationReport.do?product=UA&searc^mode=CitationR eport&SID=Z2Y7ku9pWciBC3oHJF3&page=1 &cr_p qid=3&viewType=summary).

Caption: Figure 2: Location map of testing sites in this study.

Caption: Figure 3: Collection of the temperature data along one side of the river.

Caption: Figure 4: The simplified schematic diagram to determine the water exchange patterns.

Caption: Figure 5: Box plot of sediment temperatures in testing sites.

Caption: Figure 6: Temperature profiles of streambed sediment in testing sites.

Caption: Figure 7: The treads of hyporheic water exchange and temperature with the upstream of the Weihe River.
Table 1: Testing sites and the abbreviations in this study.

Testing site   Meixian   Xi'an   Lintong   Huaxian    Hengshuihe
Abbreviation     MX       XA       LT         HX         HSH

Testing site    Heihe    Laohe    Juehe    Tangyuhe    Beiluohe
Abbreviation     HH       LH       JH        TYH         BLH
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Title Annotation:Research Article
Author:Zhang, Junlong; Song, Jinxi; Long, Yongqing; Zhang, Yan; Zhang, Bo; Wang, Yuqi; Wang, Yuanyuan
Publication:Advances in Meteorology
Article Type:Case study
Geographic Code:9CHIN
Date:Jan 1, 2017
Words:5057
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