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Keywords:

  • analytical process-based model;
  • bed morphology;
  • flow regime;
  • hyporheic flow;
  • nitrogen cycle;
  • pool-riffle bed form

Abstract

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

[1] Hyporheic flows, which stem from the interaction between stream flow and bedform, transport solute-laden surface waters into the streambed sediments, where reactive solutes undergo biogeochemical transformations. Despite the importance of hyporheic exchange on riverine ecosystem and biogeochemical cycles, research is limited on the effects of hyporheic fluxes on the fate of reactive solutes within the hyporheic zone. Consequently, we investigate the controls of hyporheic flowpaths, which we link to stream morphology and streamflow, on prevailing hyporheic redox conditions and on biogeochemical transformations occurring within streambeds. We focus on the dissolved inorganic reactive forms of nitrogen, ammonium and nitrate, because nitrogen is one of the most common reactive solutes and an essential nutrient found in stream waters. Our objectives are to explore the influence of stream morphology, hyporheic water temperature and relative abundance of ammonium and nitrate, on transformation of ammonium, removal of nitrates and production of nitrous oxide, a potent greenhouse gas. We address our objectives with analytical solutions of the Multispecies Reactive Advection-Dispersion Equation coupled with linearized Monod's kinetics and analytical solutions of the hyporheic flow for alternate-bar morphology. We introduce a new Damköhler number,Da, defined as the ratio between the median hyporheic residence time and the time scale of oxygen consumption, which we prove to be a good indicator of where aerobic or anaerobic conditions prevail. In addition, Dais a key index to quantify hyporheic nitrification and denitrification efficiencies and defines a new theoretical framework for scaling results at both the morphological-unit and stream-reach scales.

1. Introduction

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

[2] Dissolved inorganic reactive nitrogen (Nr) is a common solute found in stream waters. It affects water quality, plant growth, aquatic and terrestrial ecosystems, but is also one of the main cause of eutrophication of water bodies [Spalding and Exner, 1993; Galloway et al., 2003]. Nr is present at low concentrations in natural stream waters, but many streams flowing in agricultural and urban areas suffer from an excess of Nr, typically in the form of ammonium (NH4+) and nitrate (NO3) [Alexander et al., 2000; Peterson et al., 2001]. Microbial processes are the primary mechanisms reducing nitrogen loads by removing Nr species from rivers [Master et al., 2005]. Under oxidizing conditions, aerobic bacteria use dissolved oxygen (DO) as a terminal acceptor to transform ammonium into nitrate (nitrification), whereas under reducing conditions, in the presence of electron donor compounds such as organic carbon, anaerobic bacteria reduce nitrate to nitrous oxide (N2O) and/or molecular nitrogen (N2) through denitrification [e.g., Naiman and Bilby, 1998]. These transformations occur primarily in the streambed sediment, where the rich microbial community colonizing the streambed particle surfaces are in contact with solutes dissolved in the stream water [Master et al., 2005]. In fact, hyporheic exchange is the primary mechanism that delivers stream solutes within the streambed sediment and mixes solute-laden waters between stream and pore waters [e.g.,Tonina and Buffington, 2009a, and citations therein].

[3] Field investigations of nitrogen cycle support the importance of hyporheic exchange in nutrient cycling in rivers [Alexander et al., 2000; Binley, 2005] and of the hyporheic zone (HZ) as a transformation hot spot, zone with high biogeochemical transformation, for nitrogen compounds [Triska et al., 1993; Mulholland et al., 2004; Zarnetske et al., 2011]. Additionally, numerical simulations of hyporheic chemistry within dunes at the sea floor [Cardenas et al., 2008] and within stream meanders [Boano et al., 2010] show the importance of hyporheic flow structure in biogeochemical zonation of the hyporheic zone.

[4] Despite these evidences, there is a lack of knowledge on the controls of streambed morphology, which is a primary driver of hyporheic flows [e.g., Tonina and Buffington, 2009a], on hyporheic biogeochemical processes. In the present work, we investigate the control of stream morphology and flow on prevailing aerobic and anaerobic conditions within the streambed hyporheic zone. In addition, we quantify the efficiency of the hyporheic zone in transforming ammonium, removing nitrates and in producing nitrous oxide as a function of stream morphology and ambient conditions, such as hyporheic water temperature and relative abundance of ammonium and nitrate. We show that prevailing redox conditions within the hyporheic zone can be predicted according to the value assumed by a new dimensionless number, Da, defined as the ratio between the hyporheic median residence time and the time of consuming dissolved oxygen to a prescribed threshold concentration below which reducing reactions are activated.

[5] To address our objectives, we use a Lagrangian model based on analytical solutions of the Multi Species Reactive Advection-Dispersion Equation (RADE) with advection obtained by solving the flow equation within the hyporheic zone, and expressing Nr transformations as a function of the travel time distribution of a passive solute. This model is a generalization of the semi-analytical model proposed byMarzadri et al. [2011]in the absence of dispersion. Here, we focus on alternate-bar morphology because of its ecological importance and ubiquity in gravel bed rivers [Tonina and Buffington, 2007; Buffington and Tonina, 2009]. This bed form is composed of an alternate sequence of pools, where water is deep and slow, and riffles, where flow is shallow and fast, with two successive diagonal fronts delimiting the bar unit with a pool at the downstream end of each front in proximity of the channel banks (Figure 1) [e.g., Tonina and Buffington, 2009b].

image

Figure 1. Reach with alternate-bar topography (z). The coordinates x, y, and z are positive downstream, leftward, and upward.

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2. Method

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

2.1. Hyporheic Flow

[6] We consider a straight gravel bed river of constant width and discharge with alternate-bar morphology and a homogeneous and isotropic hydraulic conductivity (K) of the streambed sediment. Under these hypotheses, the governing equation of the hydraulic head h assumes the following form [Marzadri et al., 2010]:

  • equation image

which can be solved analytically with the following boundary conditions (see Figure 1):

  • equation image

where x, y and z are the spatial coordinates, 2B is the channel width, Y0 is the mean flow depth above the mean streambed elevation, which is fixed at z = 0, zd is the alluvium depth, L is bar wavelength and hb is the head at the stream bed. In the present work, we approximate hb with the theoretical expression provided by Colombini et al. [1987], but other approximations, analytical, numerical or empirical, may be used when needed [e.g., Elliott and Brooks, 1997; Marion et al., 2002; Tonina and Buffington, 2009b, 2011]. Strictly speaking, this condition should be applied to the surface z = η(x, y), representing the elevation of the streambed above its mean (Figure 1). However, in a previous paper [Marzadri et al., 2010] we showed that applying it to the plane z = 0 modifies only slightly the distribution of h with negligible effects on the travel time distribution within the hyporheic zone. This assumption dramatically simplifies the differential equation and allows deriving an analytical solution for the head.

[7] Once h is known from the solution of equation (1) with the boundary conditions (2), it can be substituted into the Darcy equation:

  • equation image

to obtain the velocity field u[u, v, w]. In equation (3) ϑ is the alluvium porosity, such that the hyporheic flux is q = ϑ u.

[8] In the present work, we employ the analytical solutions of the equations (1) and (3) with the boundary conditions (2) obtained by [Marzadri et al., 2010].

2.2. Biogeochemical Model

[9] We model the nitrogen cycle within the hyporheic zone by using the simplified conceptual model depicted in Figure 2, which accounts for nitrification, denitrification, and biomass uptake [Valett et al., 1996; Pinay et al., 2009; Zarnetske et al., 2011]. Nitrogen transformations are controlled by the reaction rates fi of dissolved oxygen (i = 0), and the four nitrogen species (i = 1,2,3 and 4 for ammonium, nitrate, dinitrogen and nitrous oxide, respectively) reported in the Appendix A (equations (A5)(A7)). As discussed by Marzadri et al. [2011], these linear reaction rates are obtained from linearization of the Monod's kinetics and are shown to provide a very good approximation of nitrogen transformations in both natural and biogeochemically altered rivers, where the concentrations of Nr species are typically much smaller than the corresponding equilibrium concentrations in the Monod's equations [Buss et al., 2006; Kjellin et al., 2007].

image

Figure 2. Proposed nitrogen cycle within the hyporheic zone.

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[10] Besides the concentration of the nitrogen species, other important factors control biological activity, such as dissolved oxygen (C0), organic carbon, pH and water temperature. Dissolved oxygen concentrations are about 9–10 mg/l (at the water temperature of 15°C) in well aerated streams, but conditions shift from aerobic to anaerobic when C0 falls below a given threshold C0,lim. In line with our simplified geochemical model, we assume that aerobic reactions (nitrification and biomass respiration), which consume oxygen, are active along the flow paths where C0 > C0,lim. However, from where this limit is reached inward, redox conditions are not longer favorable to nitrification, which ceases, while denitrification is triggered [Böhlke and Denver, 1995].

[11] Nutrient cycling is also influenced by the ratio between ammonium and nitrate concentrations in streams [Sjodin et al., 1997], because ammonium is a source of nitrate through nitrification. We identify the relative abundance of one with respect to the other Nr species through the following coefficient:

  • equation image

where the subscript 0 indicates the concentrations at the entry downwelling surface. Therefore RC < 1 identifies stream with relative abundance of nitrate with respect to ammonium. As in the work of [Marzadri et al., 2011], we neglect the Dissimilatory Nitrate Reduction to Ammonium (DNRA), which has been recently observed in soils [Sylvia et al., 2005], but it is considered a minor factor in streambed [Kelso et al., 1999; Puckett et al., 2008; Duff and Triska, 2000]. Furthermore, we neglect the ANAMMOX reaction occurring during the anaerobic oxidation of NH4+ to N2O because very little is known regarding its relevance with respect to aerobic nitrification in surface and subsurface water bodies [Kendall et al., 2007].

[12] Finally, we assume that organic carbon (C) is not a limiting factor and that pH is constant. With the former assumption, we implicitly consider that the molar ratio between C:N is within the range from 30 to 40, for which mineralization and immobilization reactions are balanced [Maier et al., 2009], a common condition in most real streams [Arango and Tank, 2008]. With the latter assumption, we neglect the effect of pH variations on redox conditions. Finally, we account for the temperature effects on the reaction rates through the Arrhenius equation [Fogler, 1999]:

  • equation image

where Ki are the rate coefficients at the hyporheic temperature T, which for simplicity is assumed constant within the hyporheic zone, Ki(20°C) are the rate coefficients at 20°C and φi are the temperature coefficients (dimensionless).

2.3. Solute Transport Model

[13] The total mass flux QMi of the i-th species across the upwelling surface can be written as the summation of the contributions from the streamlines crossing the surface, as follows [Marzadri et al., 2011]:

  • equation image

where q(a) is the component of the downwelling flux normal to the infinitesimal cross section area dA(a) of the streamline originating from x = a within the downwelling surface Adw. The corresponding quantities at the upwelling surface are q(ξ) and dA(ξ), respectively, with ξindicating the position where the same streamline crosses the upwelling surface. The second right-hand expression inequation (6) is obtained by imposing the continuity equation along the streamline: q(a)dA(a) = q(ξ) dA(ξ). The travel time τ assumes the following expression [Shapiro and Cvetkovic, 1988; Dagan et al., 1992; Cvetkovic and Dagan, 1994]:

  • equation image

where s′ is the distance from a measured along the streamline, u(s′) is the velocity at the same position and s(a) is the distance from the origin of the point where the travel time is evaluated. Notice that at each travel time τ(a) is associated a position s(a) along the streamline. The dependence from a is introduced to identify the streamline. Hereafter, we indicate with τup(a) the time needed by the particle entering the hyporheic zone at x = a to reach the upwelling surface at the position x = ξ. Notice that at each position ξ within the upwelling area corresponds a single value of τup. Consequently, the probability distribution of τup(a) describes the hyporheic residence time distribution of stream waters within the alluvial sediments. In the following, for simplicity of notation, we omit the dependance of τ from a.

[14] The concentration flux of the i-th species at the position where the streamline crosses the upwelling surface is defined as follows:

  • equation image

where DL = DL + αLq(ξ)/ϑ is the effective longitudinal dispersion coefficient. In equation (8) DM is the molecular diffusion and αL is the longitudinal local dispersivity, which is assumed constant through the domain, such that the longitudinal component of the mechanical dispersion tensor depends linearly from the local velocity. Classical experimental results summarized by Saffman [1960] and Pfankuch [1963] and later reinterpreted by Bear [1972] suggest that for grain Peclet numbers, Pe = q d50/(ϑ DM), larger than 100, the experimental longitudinal dispersivity is well approximated by the following expression: αL = βB d50, where d50 is the median grain size of the sediment and βB ≃ 1.8. In the present work, we assumed d50 = 0.01 m, which leads to αL = 0.018 m.

[15] An expression similar to equation (6) can be written for any other surface crossed by the streamlines including the downwelling area:

  • equation image

where Cf,i(0, t) is the concentration of the species i in the stream water. The concentration flux Cf,i, i = 0, 1, 2, 3, 4 of dissolved oxygen and the four Nr species is obtained by substituting into equation (8) the expressions of the resident concentrations obtained by solving the RADE along the streamlines with reaction rates provided in the Appendix A and neglecting lateral local dispersion:

  • equation image

[16] Solutions of the equation (10), with the biogeochemical model reported in Appendix A, are provided in Appendix B, which for completeness also reports the solution developed by Marzadri et al. [2011] for purely advective transport, i.e., by assuming DL = 0 in equation (10). Similar solutions, but for a different biogeochemical model, have been obtained by van Genuchten and Alves [1982] and Gelhar and Collins [1971], while Bellin and Rubin [2004]adopted a similar approach to solve the ADE for a non-reactive tracer. Solutions provided inAppendix B are with the concentration of the Nr species normalized with respect to the total downwelling dissolved inorganic reactive nitrogen concentration: Nr0 = C1,0 + C2,0.

[17] Nitrification processes and respiration of the biomass consume oxygen within the hyporheic zone, such that aerobic processes are active from the downwelling area (which is identified by τ = 0 in our Lagrangian reference system), where C0 = C0,0, to the position along the streamline where C0 = C0,lim. This specific position is identified by the travel time τ = τlim. In the remaining part of the streamline, aerobic processes are assumed to switch off because the environment becomes anaerobic. Consequently, τlim uniquely identifies the position along the streamline where the processes switch from aerobic to anaerobic. The evolution of C0 along the streamline is provided by equation (B1), which solved with respect to τlim after imposing C0(τlim, t) = C0,lim leads to the following expression for τlim:

  • equation image

This solution coincides with that obtained by Marzadri et al. [2011] under the hypothesis of negligible longitudinal dispersion.

[18] The prevailing aerobic or anaerobic conditions within the hyporheic zone influence the biogeochemical processes occurring along the streamlines and in turn the nitrogen removal efficiency of the streambed sediments. There are several ways to define the efficiency of the hyporheic zone in removing ammonium and/or nitrate. Here, we adopt the following two definitions:

  • equation image

and

  • equation image

where QS is the stream discharge. Equation (12) represents the efficiency of the hyporheic zone in removing the Nr species, evaluated with respect to the mass flux of the same species entering through the downwelling surface, while equation (13) represents the efficiency with respect to the mass flux in the stream.

[19] Furthermore, we define the normalized production of nitrogen gases as follows:

  • equation image

which is normalized by the total downwelling Nr mass flux (C1,0 + C2,0)Qdw(t) = Nr0 imageq(0) dA.

2.4. Comparison With Field Measurements

[20] Before analyzing the impact of river morphology on the nitrogen cycle we verify our model against the experimental data published by Beaulieu et al. [2008, 2009]. To our best knowledge, these are the only works reporting both morphodynamic and nutrient concentration data needed for the application of our models without resorting to some type of fitting of the model on measured output data. This analysis complements the comparison performed by Marzadri et al. [2011] with the same data set but neglecting local dispersion and allows detecting the effect of local dispersion on Nr transformation within the hyporheic zone.

[21] Morpho-hydrodynamic (water dischargeQ, stream velocity v and water depth Y0) and biogeochemical parameters used in modeling the field measurements are published in the work of Marzadri et al. [2011].

[22] Figure 3 shows the comparison of nitrous oxide (N2O) production computed with our models with measurements in 7 streams, whose characteristics are reported in the papers by Beaulieu et al. [2008, 2009] and Marzadri et al. [2011]. Both purely advective (AR) model developed by Marzadri et al. [2011], and advective-diffusive (ADR) model, developed here, well match the observed values with some large differences in streams 3 and 6 as previously observed byMarzadri et al. [2011]. Differences between the AR and ADR are small, thereby supporting the hypothesis that advection dominates solute transport within the hyporheic zone and local dispersion is of secondary importance, with respect to the impact of uncertainty of the measurements as reported by Beaulieu et al. [2008, 2009] and shown by the 95% error bars in Figure 3. However, local dispersion may be important under non-steady-state conditions, such as with varying solute loads and discharges of the stream flow. Whereas, the neglected transverse component of the local dispersion may be important in mixing hyporheic with groundwaters along the fringe between hyporheic zone and the underlying aquifer. Evaluating these effects is beyond the scope of this work.

image

Figure 3. Comparison of the areal production of nitrous oxide obtained using the ADR model developed in this study with the AR model proposed by Marzadri et al. [2011] and field data published in studies by Beaulieu et al. [2008, 2009].

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3. Results

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

3.1. Simulation Setup

[23] Alternate-bar morphology can be described synthetically through three dimensionless parameters: the relative submergenceds = d50/Y0, the Shields number θ (an index of sediment mobility), and the aspect ratio β = B/Y0 [Colombini et al., 1987]. In the present work, in order to analyze how different hydraulic and morphodynamic characteristics control the hyporheic inorganic nitrogen cycle, we explore a wide range of bedform topographies by letting ds to vary between 0.01 and 0.03, while keeping the other two parameters constant and equal to β = 15 and θ = 0.08. All the computations are performed with d50 = 0.01 m, such that variations of ds are obtained by varying the flow depth Y0. Table 1, shows the depths Y0 used in the simulations and the corresponding stream's characteristics computed by using classic morphological expressions [e.g., Colombini et al., 1987]. Our analysis spans a wide range of channel's width (2B = 1.5–30 m), slopes (s0 = 0.13–2.64 %), and discharges (QS = 0.07–51.9 m3/s) (Table 1) and can be considered as representative of a large class of streams. In addition, Table 2 reports the biogeochemical parameters used in the simulations with the reaction rates derived from published field measurements [Rutherford, 1994; Sjodin et al., 1997; Dent and Henry, 1999].

Table 1. Morphological and Hydrodynamic Parameters Considered in the Simulationsa
Test12345678910
  • a

    Relationships with reference parameters are also indicated: mean flow depth Y0(= d50/ds); channel width 2B(= 2Y0 β); alluvium depth zd; streambed slope s0(= θ Δ ds), where Δ = 1.65 is the submerged specific gravity of the sediment; stream water discharge QS = CC β s0(1/2) Y0(5/2), where CC = Czg1/2 is the roughness coefficient, with Cz indicating the dimensionless Chezy coefficient Cz = 6 + 2.5 ln image and g the gravitational acceleration; bed form length L; and bar amplitude HBM. Note that in all cases we fixed zd = 2B, d50 = 0.01 m and β = 15.

HBM (m)0.260.310.320.340.350.390.410.440.460.49
2B = zd (m)1.522.142.312.533.333.754.295
Y0 (m)0.050.070.070.080.080.10.110.130.140.17
L (m)10.1113.2914.1915.2216.4219.5321.5824.1527.4331.81
s0 (%)2.641.981.851.721.581.321.191.060.920.79
QS (m3 s−1)0.070.130.150.180.210.320.410.530.721.02
Test11121314151617181920
HBM (m)0.530.580.650.770.870.90.930.9611.05
2B = zd (m)67.510152021.4323.082527.2730
Y0 (m)0.20.250.330.50.670.710.770.830.911
L (m)37.9247.162.4693.42124.74133.74144.17156.36170.82188.24
s0 (%)0.660.530.40.260.20.190.170.160.150.13
QS (m3 s−1)1.532.514.7311.5121.5625.0629.4639.9642.2451.97
Table 2. Physical and Biogeochemical Parameters Used in the Simulations
ParameterUnitTest ATest BTest C
Relative Concentration[−]0.31.104.1
DL(m2/s)10−610−610−6
C0,0a(mg/l)101010
C0,lima(mg/l)444
C1,0(mg/l)0.374b1.4585.460
C2,0(mg/l)1.325b1.3251.325
Nr0(mg/l)1.6992.7836.785
C3,0(mg/l)0.00.00.0
C4,0(mg/l)0.00.00.0
KR(20)a(d−1)0.100.100.10
KN(20)b(d−1)3.463.463.46
KC(20)c(d−1)1.01.01.0
KD(20)b(d−1)1.651.651.65
φR(20)a(−)1.0471.0471.047
φN(20)b(−)1.0401.0401.040
φC(20)c(−)1.0471.0471.047
φD(20)b(−)1.0451.0451.045

3.2. Morphodymanic Control on Hyporheic Residence Time

[24] The median hyporheic residence time τup,50, for which 50% of the streamlines have a residence time shorter than its value, is a good index of the time available for biochemical reactions to occur within the hyporheic zone [Tonina and Buffington, 2011]. Figure 4 shows the dimensionless median residence time τup,50* = τup,50/tf, where tf is a suitable advective characteristics time scale, versus the dimensionless depth YBM* = Y0/HBM for different values of hydraulic conductivity, K. We use here the expression of YBM* derived from Colombini et al. [1987] for alternate bar morphology

  • equation image

where βc is the threshold value of the aspect ratio βfor alternate-bar formation andb1 and b2 are functions of the flow field and sediment characteristics [see Colombini et al., 1987, Figures 5–6]. Furthermore, the time scale is tf = L/(K s0Cz), where s0 is the bed slope, Cz is the dimensionless Chezy coefficient and L is the bed form wavelength [Marzadri et al., 2010]. Notice that we assumed L and K s0as length and velocity scales of the hyporheic exchange, respectively. The Chezy coefficient accounts for streambed roughness, which affects surface water elevation and consequently near-bed pressure distribution. The later is the primary driver of the hyporheic flow for this type of bed form [Tonina and Buffington, 2007, 2009a; Marzadri et al., 2010].

image

Figure 4. Dimensionless median residence time τup,50* = τup,50Ks0Cz/L (open symbols) and coefficient of variation CV = image (solid symbols) as a function of the dimensionless depth YBM* for different values of hydraulic conductivity K. Simulations have been conduced with the following values of hydraulic conductivity: K = 0.01 m/s (diamonds), K = 0.005 m/s (triangles), K = 0.001 m/s (circles) and K = 0.0001 m/s (squares). Because of the normalization, results for τup,50* and CV with different K collapse along a single line; thus all the symbols overlap and only the squares are visible.

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[25] As expected, τup,50* is insensitive to K as a consequence of the linearity of Darcy's equation, such that a variation of K causes a proportional variation of the travel times, and of tf as well (Figure 4). However, nonlinear effects are expected in case K is spatially variable (heterogeneous). Whereas τup,50* increases with YBM*, the coefficient of variation CV = image where image is mean and image the standard deviation of the travel time, remains approximately constant around a value of 1.3. A similar value (i.e., CV = 1.4) was observed by Tonina and Buffington [2011] in flume experiments with fully submerged bars of small amplitude. This rather high CVindicates a wide distribution of residence times experienced by the solutes emerging from the upwelling area, which is therefore expected to exert a strong influence on biogeochemical transformations. In addition, the strong relationship we found here between the residence time distribution and the morphological characteristics of streambed have been also observed experimentally in branches of the Mississippi-Missouri river network [Mulholland et al., 2008]. This connection cannot be established with a purely diffusional zero-dimensional exchange model, often used in modeling the hyporheic exchange.

[26] The dimensionless median residence time, τup,50*, can be used to identify streams, whose morphodynamic characteristics result in comparable residence time distributions and therefore showing comparable effects on Nr species. We observe that τup,50* is proportional to YBM*such that it increases from small and steep to large low-gradient streams. Therefore, our model captures what already observed in river systems, i.e., that Nr cycling changes from low to high order streams along river networks [Alexander et al., 2000; Peterson et al., 2001].

[27] The following exponential function well approximates τup,50* obtained with our model for fully submerged alternate bar topography (Figure 4):

  • equation image

with R2 = 0.99, which quantifies the effect of streambed morphology, epitomized by the dimensionless depth (YBM*), on the residence time within the alluvial sediments.

[28] Equation (16) expresses τup,50* as a function of physical quantities (e.g., mean water depth, streambed slope, stream width, bed form amplitude and wavelength, sediment hydraulic conductivity and median sediment grain size) which are available, or can be obtained with a limited effort, and allows correlating hyporheic travel time characteristics to river and sediment hydraulic properties. Although, we derive this relationship under the hypothesis of equilibrium conditions between flow regime and streambed morphology, the work of Marzadri et al. [2010] shows that it is applicable for any discharge that entirely submerges the gravel bars.

3.3. Hyporheic Aerobic-Anaerobic Zones

[29] Geochemical transformations occurring in the hyporheic zone depend on the reciprocal values assumed by the residence time of solutes and the time needed to reach the anoxic conditions as expressed by the ratio image = τ/τlim, between the residence time, which in stationary conditions coincides with the travel time of the particle traveling along the streamline, and the time needed to deplete oxygen concentration C0,lim. image indicates whether at a given position along the streamline redox conditions are aerobic ( image < 1) or anaerobic ( image > 1).

[30] With these considerations in mind, we introduce a dimensionless number defined as the ratio between the median residence time (τ50) evaluated at a control surface within the hyporheic zone and the residence time limit (τlim) at which oxygen concentration is depleted to C0,lim: imageHZ = τ50/τlim. This new metric provides an immediate indication of the prevailing conditions within the hyporheic zone from the downwelling area to the compliance surface, which can be the upwelling area, or any other control surface internal to the hyporheic zone. Values of imageHZ < 1 are indicative of prevailing aerobic conditions upstream, while imageHZ > 1 indicates that more than 50% of the streamlines are already in anaerobic conditions at the point where they cross the compliance surface. An indication of the global geochemical status of the hyporheic zone is therefore provided by the following dimensionless Damköhler number: Da = τup,50/τlim. Consequently, values of Dalarger than 1 indicate prevailing anaerobic conditions, whereas values smaller than 1 prevailing aerobic conditions, within the hyporheic sediment between the downwelling and upwelling surfaces. This allows analyzing the prevailing redox conditions within the hyporheic zone induced by alternate-bar morphology as a function of stream size as shown inFigure 5, which depicts Da as a function of YBM*. In our simulations, transition between prevailing aerobic and prevailing anaerobic conditions occurs for YBM* between 0.3 and 0.6 depending on hydraulic conductivity of the streambed material. For given hydraulic and biogeochemical characteristics of the sediment (i. e. for a given curve in Figure 5), Da increases passing from small to large streams implying that the fraction of the hyporheic zone in anaerobic conditions increases with stream size. Notice that the surface separating aerobic from anaerobic portions of the hyporheic zone can be identified by detecting the points along the streamlines where image = 1; the volume upstream of this surface is in aerobic condition, while that downstream is in anaerobic condition.

image

Figure 5. Damköhler number Da = τup,50/τlim as a function of the dimensionless depth YBM* = Y0/HBM for different values of hydraulic conductivity K.

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[31] The above results are in line with the experimental findings of Triska et al. [1993] along a reach of the Little Lost Man Creek, California, where they observed low concentrations of dissolved oxygen and nitrate in zones with long travel times, where likely image > 1, while both species were present at higher concentrations in zones with short travel times ( image < 1) i.e., close to the downwelling area. Furthermore, the study of Krause et al. [2009] highlights the importance of the residence time on denitrification efficiency, which increases with long residence times within the hyporheic zone as the anaerobic portion of the hyporheic zone becomes dominant with respect to the aerobic portion. Most recently, Zarnetske et al. [2011] measured that dissolved oxygen below one parafluvial gravel bar decreases almost exponentially with hyporheic residence time. Our results are in qualitative agreement with this experimental findings because the length of the streamlines crossing the points along a vertical section increases with depth.

[32] Because Da includes the effects of streambed morphology via τup,50 and hyporheic biogeochemical properties via τlim, we use this index to study the effects of alternate-bar morphology in our analysis.

3.4. Ammonium and Nitrate Removal

[33] Figure 6a shows the efficiency, R1S, in transforming NH4+ to NO3, evaluated with respect to the stream mass flux, as a function of Da for both the ADR, (see equation (A3) in Appendix A), and the simplified AR models. Figure 6b repeats Figure 6a for the efficiency R1HZ, evaluated with respect to the downwelling mass flux. The physical, chemical, and geomorphological parameters used in the simulations are reported in Table 2. Differences between the two models are small regardless of residence time. This shows that mixing due to local dispersivity influences only marginally the global transformation of NH4+ to NO3 occurring within the hyporheic zone, although locally larger differences may be observed. The hyporheic zone is always a sink of ammonium irrespective to RC (RC < 1 for streams richer in nitrate than ammonium). This is in line with field measurements conducted by Fernald et al. [2006] in a gravel bed river. Both models show R1S decreasing with Da, thus with stream dimension and inversely with bacterial activities (represented by τlim), again irrespective to RC. Efficiency is greater for RC > 1 because of the predominance of ammonium with respect to nitrate in the stream water. For a fixed value of τlim and K, Da increase with the stream dimension and consequently with the stream water discharge. Therefore, the reduction of R1S with Da is mainly due to the increase of stream discharge, which we use to normalize ammonium transformation in the definition of R1S.

image

Figure 6. Transformation of ammonium within the hyporheic zone relative to (a) stream ammonium mass flux, R1S, and (b) downwelling ammonium mass flux, R1HZ, versus the Damköhler Da = τup,50/τlim for streams initially richer with nitrate RC < 1 and ammonium RC > 1. Both ADR and AR solutions are shown.

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[34] Conversely, R1HZ increases with Da because of the longer time available for nitrification and reaches a constant value for Da ≈ 10. The transport model has a marginal effect on transformation of ammonium, with ADR predicting a slightly smaller value of R1S than AR, because diffusion lowers local solute concentrations, thereby reducing the overall reaction rates. Lower concentrations result in lower transformations and therefore a higher export of solute from the hyporheic zone through the upwelling surface. The difference between R1S obtained with ADR and AR models decreases with RC due to lower initial ammonium concentrations in the stream.

[35] Figures 7a and 7b show the two efficiency indexes R2S and R2HZ for nitrate removal predicted with the ADR (A4) model as a function of Da. AR produces similar results, which are not reported here. Figure 7a shows R2S for three different streambed hydraulic conductivity values and for RC = 0.3 and RC = 3. Large hydraulic conductivities increase downwelling mass fluxes and thus the amount of nitrate subject to denitrification. The efficiency R2S, evaluated with respect to the stream mass flux, increases with K, which has a double effect because it acts also on the mean dimensionless time and consequently on Da distribution (as previously commented in Figure 5). We observe that R2S increases reaches a maximum and then decreases with Da, suggesting that there is a particular streambed geometry, which maximizes nitrate removal. The reduction of R2S at large Da after the peak is due to the combined effect of the upper limit of the removal evidenced in Figure 7b and the increase of mass flux in the stream associated to the increase of water discharge. In fact, in our simulations Da increases with the water discharge when τlim and K are kept constant.

image

Figure 7. Removal of nitrate within the hyporheic zone relative to (a) stream nitrate mass flux, R2S, and (b) downwelling nitrate mass flux, R2HZ, computed with the ADR model versus the Damköhler Da = τup,50/τlim in stream initially rich with nitrate RC < 1 (open symbols) and ammonium RC > 1 (solids symbols), for different values of hydraulic conductivity (top) and for a constant value of hydraulic conductivity K = 0.001 m/s (bottom).

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[36] When the stream water is richer in NO3 than in NH4+ (i.e., RC = 0.3), R2S is always positive and thus the hyporheic zone is a sink of nitrate. On the other hand, when the stream water is richer in NH4+ than NO3 (i.e., for RC = 3) and for relatively small Da values, nitrate produced by nitrification of ammonium is larger than that removed in the anaerobic portion of the hyporheic zone. This causes R2S to assume negative values, which indicates production of nitrate. However, as Da increases, denitrification removes more and more nitrate and R2S increases, reaches a maximum and then decreases due to the parallel increase of water discharge. Similarly, R2HZ shows that hyporheic zone is always a sink of nitrate for small values of relative concentration (RC = 0.3). Because of this behavior we can identify a particular value of Da, which we call Das, above which the hyporheic zone acts as a sink of NO3. Das is only a function of RC and not of streambed hydraulic conductivity (at least for a spatially uniform hydraulic conductivity) and temperature (Figure 8). Therefore, all reaches of streams with Da > Das are sinks of NO3.

image

Figure 8. Das as a function of the stream relative concentration (RC) for several values of the hydraulic conductivity K and two temperatures (T = 6°C and T = 13°C). The linear regression equation is valid for RC > 0.48 and for the reaction rate of biomass uptake and denitrification reported in Table 2.

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[37] Experimental studies conducted in a gravel bed river by Fernald et al. [2006] also confirm that the hyporheic zone may act as a source or a sink for NO3 depending on the hyporheic flow rate qH, which is an index of hyporheic residence time, such that streams with low qH are in prevailing anaerobic conditions and consequently the hyporheic zone acts as sink for nitrate. Field measurements conducted by Zarnetske et al. [2011] show similar results with nitrification producing NO3 at short residence times and denitrification removing NO3 at long residence time. As in our model the transition occurs when dissolved oxygen reaches a threshold value, which is assumed 0.2 mg/l in their field observations.

[38] Similarly to R1HZ, the efficiency, R2HZ evaluated with respect to the downwelling mass flux of nitrate, reaches a maximum value smaller than 100%. This maximum value depends on the residence time distribution; the relatively high values of CV suggests that there will be always streamlines in aerobic conditions such that not all the mass flux of nitrate entering the hyporheic zone can be removed and the efficiency should be smaller than 100%.

3.5. Temperature Effects

[39] Water temperature plays an important role in biogeochemical processes because reaction kinetics are temperature dependent. The effect of temperature on the dimensionless production of nitrous oxide, P4S, in the stream water, is shown in Figure 9 as a function of Da for both AR and ADR models and with T = 6°C and T = 13°C. The flux concentration of nitrous oxide C4 is evaluated with equations (B6), (6) and (9). In all cases RC = 0.3, such that the initial pulse is richer in NO3 than NH4+.

image

Figure 9. Effects of hyporheic water temperature on the dimensionless production of nitrous oxide, P4S, within the stream versus the Damköhler Da = τup,50/τlim. In all cases RC = 0.3 and K = 0.001 m/s.

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[40] High temperatures increase the reaction rate coefficient according to Arrhenius law (equation (5)) and consequently the production of molecular nitrogen. However, the figure shows that P4HZ is less sensitive to the water temperature when Da is large, i.e., for large residence times or fast reaction rate (small τlim). For given stream Nr concentrations and constant τlim, large streams (large Da) produce larger quantities of nitrogen gases than small streams, irrespective of water temperature, because of the prevailing anaerobic conditions along the streamlines. However, the emission relative to the nutrients load in the stream, P4S, reduces as an effect of the increase of stream discharge. Conversely, because of the shorter residence times temperature variations have a stronger impact in small steep than in large low-gradient streams as shown inFigure 9 for intermediate Da results.

[41] This implies that small steep and large low-gradient streams respond differently to seasonal temperature changes in temperate regions. Small steep streams produce more Ngasduring the warm season, while smaller differences with respect to the cold season are expected for large low-gradient streams. This may suggest that field measurements and monitoring procedure of nutrients should account for seasonal variations but also for the daily cycle as temperatures may vary remarkably between day and night in small streams where typically these measurements are taken. Additionally, biomass nitrate uptake could potentially increase with temperature much faster than denitrification rates in some systems. Consequently, biomass uptake could lower the available nitrate for denitrification and hence it could offset the observed increase inP4S with temperature.

4. Conclusions

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

[42] Our analysis based on analytical solutions of a multispecies reactive solute transport within the hyporheic zone presents several results:

[43] 1. The ratio between a representative hyporheic residence time, whose value depends on the scale of the analysis, and the characteristic time of oxygen consumption, τlim, can be used to identify the aerobic and anaerobic zonation of the hyporheic zone.

[44] 2. A new Damköhler number, Da, defined as the ratio between the median hyporheic residence time, τup,50 and τlim can be used to identify the prevailing aerobic (Da < 1) or anaerobic (Da > 1) conditions at the scale of a single bedform.

[45] 3. Streambed morphology and flow by influencing Da have a strong control on redox conditions within the hyporheic zone.

[46] 4. Hyporheic efficiency in removing ammonium and nitrate increases with Da such as nitrous oxide production.

[47] 5. A particular value of Da, Das, which does not depend on streambed hydraulic conductivity, for homogenous hydraulic properties of the sediment, and on hyporheic temperature but only on the relative abundance of ammonium and nitrate, defines when the hyporheic zone is a source or a sink of nitrate.

[48] 6. Hyporheic efficiency in removing ammonium and nitrate is lower than 100% in streams with alternate-bar morphology due to the large distribution of residence time induced by this topography.

[49] 7. Diffusion is of secondary importance compared to advection in the transformation and removal of reactive nitrogen within the hyporheic zone.

[50] 8. Hyporheic water temperature affects nitrogen transformation in systems with small but not for those with large Da values.

[51] Our proposed Lagrangian approach applied at the single streamline suggests that the dimensionless number image = τ/τlim, where τ is the residence time of the flow path, can be used to determine whether the flow path has prevailing aerobic ( image < 1) or anaerobic ( image > 1) conditions. If the analysis is restricted over a portion of the hyporheic zone, a dimensionless travel time could be defined as imageHZ = τ50/τlim, where τ50 is the median residence time evaluated at a control surface within the hyporheic zone. For instance, the analysis could be applied to a portion of the hyporheic zone as defined in the work of Gooseff [2010].

[52] At the bedform scale, our results show a strong dependance between nitrification-denitrification processes and alternate-bar morphology. Throughequations (16) and (11) we define a new Damkhöler number Da = τup,50/τlim able to represent this interaction between biogeochemical and morphological processes.

[53] Consequently, this Lagrangian approach can be extended to any other bed forms provided that τup,50can be obtained. For instance, this analysis could be readily applied to dune-like bedform for which solutions of the residence time distribution are available [e.g.,Elliott and Brooks, 1997; Bottacin-Busolin and Marion, 2010] or for studying localized hyporheic flow such as that induced by logs [Sawyer et al., 2011].

[54] Da values lower than 1 results in prevailing aerobic conditions with low reactive nitrogen removal at the unit scale. Values of Da larger than 1 indicate prevailing anaerobic condition with large opportunity of Nr removal and production of nitrogen gases. As a result, the hyporheic zone may be an important source of N2O to stream waters and may play a significant role regulating greenhouse gas emissions and consequently the greenhouse effect.

[55] Application of Dafor increasing stream size with alternate-bar morphology, shows different roles between hyporheic zones of mountain headwaters, which are typically small and steep streams, and those of large low-gradient streams, typical of valley bottoms. Nitrification processes dominate in the former streams because of short residence times whereas denitrification plays a major role in the latter streams. Emissions of nitrogen gases increase with temperature in small steep streams such that they are more efficient in removing nitrate during the warm than cold season. Conversely, streams at the valley bottom can act as sinks of nitrate and source of nitrogen gases with similar efficiency regardless of seasonal or daily temperature variations.

Appendix A:: Biogeochemical Model

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

A1. Dissolved Oxygen

[56] Dissolved oxygen transport and transformation within the hyporheic zone is modeled by specializing equation (10) for i = 0:

  • equation image

with

  • equation image

where KRN(T) is the oxygen rate coefficient that accounts for respiration and nitrification. For simplicity and without loosing generality, we assume that C0 is at saturation in the stream waters at all time such that C0,0 = 10 mg/l in all simulations. Furthermore, C0 = C0,lim at t = 0 within the hyporheic zone, and image = 0 for long residence times (i.e., for τ [RIGHTWARDS ARROW] ∞).

A2. Nr Species

[57] The streamline is divided into two parts: in the first part, which is identified with ττlim, a solution is obtained by assuming KD = 0 (denitrification is switched off) and imposing only the boundary condition at the downwelling surface. In the second part (i.e., for τ > τlim), the solution is obtained by assuming KN = KC = 0 and imposing the boundary condition at the upwelling surface. The two remaining constants are obtained by simply imposing that the two expressions of the concentration assume the same values at the interface between these two zones (i.e., for τ = τlim). Comparisons between accurate numerical simulations based on conservation of concentration fluxes, obtained by imposing image = image, where Ci,ox and Ci,aox are the two solutions obtained for τ < τlim and τ > τlim, respectively, and our simplified analytical solution, obtained by imposing image = 0, show negligible differences. The error increases slowly with τlim and we observe less than a 3% difference for τlim = 8 days.

[58] The dynamics of ammonium species can be obtained by solving the differential equation that results from specializing the governing equation (10) for i = 1 as follows:

  • equation image

[59] Similar to the previous case, the evolution of C2 can be obtained by solving the differential equation obtained by specializing the equation (10) for i = 2:

  • equation image

In equations (A3) and (A4) the reaction terms f1 and f2 represent the interplay between oxygen, ammonium and nitrate and are modeled with the following Monod kinetics [Bailey and Ollis, 1977]:

  • equation image

where μN(T), μC(T) and μD(T) are the nitrification, biomass assimilation, and denitrification potential (maximum) rate, respectively and K1N(T), K1C(T), and K1D(T)their associated half-saturation (Monod) constants. Considering streams with low pollution [Buss et al., 2006; Kjellin et al., 2007] and consequently with low concentrations (K1i ≫ [Ci]) [McLaren, 1976; Sheibley et al., 2003], equations (A5)simplify to the following first-order (linear) kinetics [Marzadri et al., 2011]:

  • equation image

with

  • equation image

where KN(T), KC(T), and KD(T) are the nitrification, biomass assimilation and denitrification rate coefficients, respectively.

[60] Finally, nitrogen gases are the products of denitrification processes and their concentration can be computed by solving the following equation:

  • equation image

Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

B1. Dissolved Oxygen

[61] The solution of model (A1) assumes the following form:

  • equation image

B2. Nr Species

[62] Along the aerobic part of the streamlines the solutions of the models (A3), (A4) and (A8) assume the following expressions:

  • equation image

where

  • equation image

[63] In the particular case in which the flow along the streamlines is purely advective (i.e., for DL = 0), the solutions (B2) simplify as follows:

  • equation image

which coincide with the solution obtained by Marzadri et al. [2011] in the absence of local dispersion. On the other hand, along the anaerobic part of the streamlines, the concentration of the four Nr species assume the following expressions (obtained by solving the equations (A3), (A4) and (A8) with the respective boundary conditions):

  • equation image

where

  • equation image

[64] Again for a purely advective transport (DL = 0), the solutions (B5) become:

  • equation image

which also coincide with the solutions obtained by Marzadri et al. [2011] in the absence of local dispersion.

Notation
Adw

downwelling area, m2.

Auw

upwelling area, m2.

B

half width of channel, m.

b1

morphological parameter.

b2

morphological parameter.

C0

dissolved oxygen concentration, mg l−1.

C0,lim

dissolved oxygen concentration limit, mg l−1.

C1

ammonium concentration, mg l−1.

C2

nitrate concentration, mg l−1.

C3

dinitrogen concentration, mg l−1.

C4

nitrous oxide concentration, mg l−1.

Cf,i

concentration flux of the ith species, mg l−1.

Ci

resident concentration of the ith species, mg l−1.

CV

coefficient of variation.

Cz

dimensionless Chezy number.

d50

mean grain size, m.

Da

Damkhöler dimensionless number.

dA

infinitesimal cross sectional area, m2.

DL

effective longitudinal dispersion coefficient, m s−2.

DM

molecular diffusion, m2 s−1.

ds

relative submergence.

f0

reaction rate for dissolved oxygen, mg l−1 s−1.

f1

reaction rate for ammonium, mg l−1 s−1.

f2

reaction rate for nitrate, mg l−1 s−1.

f3

reaction rate for dinitrogen, mg l−1 s−1.

f4

reaction rate for nitrous oxide, mg l−1 s−1.

h

hydraulic head, m.

hb

head at the streambed, m.

HBM

amplitude of alternate bars, m.

K

hydraulic conductivity, m s−1.

Ki

rate coefficients at the hyporheic temperature T, s−1.

Ki,(20C)

reaction rate coefficients at 20°C, s−1.

KRN

reaction rate of nitrification and respiration, s−1.

K1C(T)

half saturation (Monod) constant of biomass assimilation, mg l−1.

K1D(T)

half saturation (Monod) constant of denitrification, mg l−1.

K1N(T)

half saturation (Monod) constant of nitrification, mg l−1.

L

bar wavelength, m.

Nr0

total downwelling nitrogen mass flux, mg l−1.

PiHZ

production of nitrogen gases.

q

water flux into the streambed surface, m s−1.

qH

hyporheic flow rate, m s−1.

QM,dw

total mass flux of the ith species across the downwelling surface, mg m3 s−1 l−1.

QM,up

total mass flux of the ith species across the upwelling surface, mg m3 s−1 l−1.

QS

stream discharge, m3 s−1.

RC

relative concentration.

RiHZ

efficiency of hyporheic zone in removing the nitrogen species.

RiS

stream efficiency in removing nitrogen species.

s

distance measured along the streamline, m.

s0

stream slope, m/m.

T

temperature, °C.

tf

advective characteristics time scale, s.

u

longitudinal pore water Darcy velocity, m s−1.

v

transverse pore water Darcy velocity, m s−1.

V

stream velocity, m s−1.

w

vertical pore water Darcy velocity, m s−1.

x

longitudinal coordinate, m.

y

transversal coordinate, m.

Y0

mean flow depth, m.

YBM*

dimensionless depth.

z

vertical coordinate, m.

zd

alluvium depth, m.

αL

longitudinal local dispersivity, m.

β

aspect ratio of alternate bars.

βb

coefficient for experimental longitudinal dispersivity.

βc

threshold value of the aspect ratio b for alternate bar formation.

φi(T)

Arrhenius temperature coefficients for the ith species at temperature T.

η(x, y)

bed surface elevation, m.

μC(T)

biomass assimilation potential maximum rate, s−1.

μD(T)

denitrification potential maximum rate, s−1.

μN(T)

nitrification potential maximum rate, s−1.

μτ,up

mean of the travel time, s.

θ

Shield number.

ϑ

alluvium porosity.

στ,up

standard deviation of the travel time, s.

τ

residence time, s.

τup,50*

dimensionless median hyporheic residence time.

τlim

residence time limit, s.

image

dimensionless parameter for local redox condition at the streamline scale.

τ imageZ

dimensionless parameter for local redox condition at any hyporheic control surface.

τup,50

median hyporheic residence time, s.

Acknowledgments

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

[65] This research has been funded in part by the EU VII framework program through the project CLIMB (244151) and by the national program PRIN through the Analysis of Flow and Transport Processes at the Hillslope Scale project (2008A7EBA3).

References

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information

Supporting Information

  1. Top of page
  2. Abstract
  3. 1. Introduction
  4. 2. Method
  5. 3. Results
  6. 4. Conclusions
  7. Appendix A:: Biogeochemical Model
  8. Appendix B:: Solution of the Advection-Dispersion Transport in the Hyporheic Zone
  9. Acknowledgments
  10. References
  11. Supporting Information
FilenameFormatSizeDescription
jgrg961-sup-0001-t01.txtplain text document1KTab-delimited Table 1.
jgrg961-sup-0002-t02.txtplain text document1KTab-delimited Table 2.

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