1. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 1 CHAPTER 19: EFFECT OF THE HYDROGRAPH ON MORPHOLOGY OF GRAVEL-BED STREAMS Up to this point the effect of a flood hydrograph has been folded into a characteristic flood flow and an intermittency. This, of course, is only intended to be shorthand for a full flood hydrograph. The effect of a full flood hydrograph on the morphology of a gravel-bed river is explored in this chapter. Elbow River, Alberta, Canada at low flow Elbow River, Alberta, Canada during 100-year flood. Images courtesy Alberta Research Council, Canada

2. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 2 NONLINEARITY IN THE SEDIMENT TRANSPORT RELATION The sediment transport rate is in general a nonlinear function of e.g. the Shields number. This means that doubling the Shields number more than doubles the sediment transport rate. To see this, consider a simplified sediment transport relation q* = q*(  *) of the form where q* denotes the Einstein number,  * denotes the Shields number,  t is a constant and n t is equal to an exponent (1.5 for Meyer-Peter and Müller, 2.5 for Engelund-Hansen). It follows that where is any multiplicative factor, In the above simple example, a value of n t of 1.5 means that doubling the Shields number trebles the Einstein sediment transport rate. Because of this nonlinearity, the sediment transport rate averaged over a hydrograph is biased toward the higher flows in the hydrograph, and is thus greater than the sediment transport rate at the average flow of the hydrograph.

3. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 3 SPECIFICATION OF THE HYDROGRAPH In order to perform a numerical calculation with a flow hydrograph, the actual flood hydrograph (black line) must be discretized into a series of constant discharges Q w, each extending for time duration  t w, w = 1..W. The river is assumed to be morphologically inactive when the river is not in flood. Now let  t f denote the (short) flood time step used to to calculate morphodynamic evolution (via the Exner equation of sediment continuity). It is convenient to choose each time duration  t w to be an integral number n step,w of flood time steps  t f, so that

4. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 4 SPECIFICATION OF THE HYDROGRAPH contd. Once  t f is specified along with Q w and n step,w for w = 1..W, it is possible to determine a discharge Q p for every time step p = 1..P in the hydrograph, where An example is given below.

5. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 5 NORMAL FLOW APPROXIMATION In principle it is necessary to model the evolution of a hydrograph in the downstream direction by means of flood routing. In a relatively short reach of a gravel-bed stream without tributaries, however, the hydrograph can be approximated as the same in time at every point in space. Again in a steep mountain stream, the flow can be approximated as satisfying the normal flow approximation. Now let q w,p (= Q p /B p, where B p denotes the channel width at the pth flow) denote the flow discharge per unit width for the pth flow in the hydrograph. Generalizing from Chapter 17, the boundary shear stress of the pth flow in the hydrograph at the kth spatial node  b,p,k is given as where u *,p,k, k s,p,k and S p,k denote the current shear velocity, roughness height and bed slope at the kth node and the pth step in the hydrograph. This boundary shear stress can then be used in a sediment transport formulation of the form of Parker (1991), Powell-Reid-Laronne (2001) or Wilcock-Crowe (2003) to compute the gravel transport rate at any node and at any point in the hydrograph. An implementation of Exner for each time step then allows modeling of the evolution of the bed.

6. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 6 INTRODUCTION TO RTe-bookAgDegNormGravMixHyd.xls The code in the workbook RTe-bookAgDegNormGravMixHyd.xls computes aggradation and degradation in a gravel-bed river subject to a repeating hydrograph. The bedload transport formulation is that of Parker (1990). The input is fairly extensive, and is thus explained in some detail in the next few slides. The user first specifies a flood time step: The user then inputs the number of steps in the flood hydrograph and clicks a button to set up a table for input:

7. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 7 INPUT FOR RTe-bookAgDegNormGravMixHyd.xls Water discharge per unit width q w, sediment feed rate per unit width q bTf and duration of each flow in terms of number of time steps n step are then input into the table:

8. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 8 INPUT FOR RTe-bookAgDegNormGravMixHyd.xls contd. The spreadsheet computes the duration of the flood hydrograph in days. The user must specify the number of times per year this hydrograph is to be cycled. The spreadsheet then computes the flood intermittency I f.

9. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 9 INPUT FOR RTe-bookAgDegNormGravMixHyd.xls contd. Grain size distributions are input next. The user specifies the number of grain sizes defining the input distributions, clicks a button to set up a table for input, and fills in grain sizes and percents finer for the gravel feed, initial surface size distribution and substrate.

10. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 10 INPUT FOR RTe-bookAgDegNormGravMixHyd.xls contd. The user then inputs the dowstream bed elevation  d, reach length L, initial bed slope S fbI, number of spatial intervals M, number of hydrograph cycles until a printout Mcycprint and number of printouts after the initial one Mprint. The user clicks the indicated button to perform a calculation. Note: the calculation may be rather slow!

11. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 11 OUTPUT OF RTe-bookAgDegNormGravMixHyd.xls The output is quite extensive, and includes the following plots. 1. A plot including a) the flow hydrograph, b) time variation of sediment feed (summed over all grain sizes) within the hydrograph and c) the time variation of total bedload transport rate (summed over all grain sizes) over the final hydrograph cycle of the run, at the farthest downstream node. 2. Long profiles of bed elevation. 3. Long profiles of bed slope. 4. Long profiles of surface geometric mean size. 5. Long profiles of bedload geometric mean size. 6. Long profiles of the ratio of the bedload transport rate to the feed rate (equal to unity everywhere at equilibrium). 7. Long profiles of a) the flow depth H at the end of the maximum flow of the final hydrograph of the run; b) the flow depth H at the end of the final flow of the final hydrograph of the run; c) Shields number  sg * based on surface geometric mean size at the end of the maximum flow of the final hydrograph of the run: d) Shields number  sg * based on surface geometric mean size at the end of the final flow of the final hydrograph of the run.

12. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 12 MORE OUTPUT OF RTe-bookAgDegNormGravMixHyd.xls Output plots continue as follows. 8.Long profiles of a) surface geometric mean size D sg at the maximum flow of the final hydrograph of the run, b) surface geometric mean size D sg at the final flow of the final hydrograph of the run, c) bedload geometric mean size D lg at the maximum flow of the final hydrograph of the run; d) bedload geometric mean size D lg at the final flow of the final hydrograph of the run. 9. Grain size distributions of a) the sediment feed, as well as the following distributions at the farthest downstream node; b) bed surface at the end of the maximum flow of the final hydrograph, c) bed surface at the end of the final flow of the final hydrograph, d) bedload at the end of the maximum flow of the final hydrograph, e) bedload at the end of the final flow of the final hydrograph.

13. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 13 APPLICATION OF THE PROGRAM: EFFECT OF THE HYDROGRAPH ON EQUILIBRIUM STREAM MORPHOLOGY No matter what the input parameters are (as long as there is some upstream feed of gravel), if the program is run for a long enough time the river reach will approach a mobile-bed equilibrium (averaged over the hydrograph). It is interesting to compare the equilibrium reached with a full hydrograph with the equilibrium reached by a constant flow equal to the average flow of the hydrograph, continued for the same duration as the hydrograph. To this end we consider a 30-day hydrograph with a minimum value of q w of 3 m 2 /s, a maximum value of 16 m 2 /s and an average value of 6 m 2 /s, as compared with a flow run constant at 6 m 2 /s for the duration of each hydrograph. The hydrograph and its average value are given in the next slide.

14. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 14 THE HYDROGRAPH

15. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 15 SEDIMENT FEED AND GRAIN SIZE DISTRIBUTIONS The sediment infeed rate q bTf is kept constant at 5x10 -5 m 2 /s at each step of the hydrograph. In the case of the full hydrograph, this leads to a final equilibrium at the upstream node with strong cyclic fluctuations; the bed will degrade significantly at the high flows and aggrade significantly at the low flows. These fluctuations will be damped out farther downstream as the river becomes free to increase its bedload transport rate in response to increasing discharge. Thus at the final equilibrium the sediment transport rate increases or decreases in accordance with the flow discharge, and bed elevation shows only minor cyclic fluctuations, at all nodes except those near the upstream end. The grain size distributions of the feed, initial surface and substrate are taken to be identical, as shown in the plot to the right.

16. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 16 OTHER INPUT PARAMETERS Time step: 1 day Number of flows in the hydrograph: 10 Number of times per year the hydrograph is cycled: 1 Downstream bed elevation: 0 m Reach length: 10,000 m Initial bed slope: 0.00262 Number of spatial intervals: 10 Mcycprint: 200 Mprint: 6 The duration of the calculation is 1200 years, enough to insure that a mobile-bed equilibrium is obtained.

17. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 17 RESULTS WITH THE FULL HYDROGRAPH The long profile has reached equilibrium.

18. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 18 RESULTS WITH THE FULL HYDROGRAPH The bed slope has equilibrated to a value S = 0.00151.

19. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 19 RESULTS WITH THE FULL HYDROGRAPH The surface geometric mean size has coarsened from an initial (unarmored) value of 28.8 mm to an equilibrium mobile armor of 49.2 mm

20. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 20 RESULTS WITH THE FULL HYDROGRAPH By the end of the run, the bedload geometric mean size is everywhere almost identical to that of the feed, i.e. 28.8 mm.

21. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 21 RESULTS WITH THE FULL HYDROGRAPH By the end of the run, the surface size distribution at the node farthest downstream hardly varies with flow in the hydrograph. The distribution of the load at the node farthest downstream fluctuates strongly with flow in the hydrograph, averaging over the hydrograph to the feed value.

22. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 22 RESULTS WITH THE FULL HYDROGRAPH q w m 2 /s q bTf m 2 /s q bT m 2 /s Sediment transport rate per unit width at downstream node q bT ; sediment feed rate q bTf, m 2 /s By the end of the run, the sediment transport rate at the downstream node (red line) is tracking the hydrograph, varying strongly with discharge.

23. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 23 RESULTS WITH CONSTANT FLOW FOR DURATION OF HYDROGRAPH: q W = AVERAGE VALUE OF ORIGINAL HYDROGRAPH Again a mobile-bed equilibrium is attained after 1200 years, but the upstream elevation of 26.2 m is much higher than the value of 15.1 m attained with the full hydrograph.

24. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 24 RESULTS WITH CONSTANT FLOW FOR DURATION OF HYDROGRAPH: q W = AVERAGE VALUE OF ORIGINAL HYDROGRAPH The slope equilibrates to a value of 0.00262, i.e. much higher than the value of 0.00151 obtained with the full hydrograph. Since a steeper slope is required to carry the same load, it can be concluded that the constant average flow of the hydrograph is less efficient at moving sediment than the full hydrograph.

25. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 25 RESULTS WITH CONSTANT FLOW FOR DURATION OF HYDROGRAPH: q W = AVERAGE VALUE OF ORIGINAL HYDROGRAPH The surface geometric mean size equilibrates to a value of 66.0 mm, i.e. much coarser than the value of 49.2 mm attained with the full hydrograph.

26. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 26 FINAL SURFACE GRAIN SIZE DISTRIBUTIONS The final surface size distribution with the full hydrograph is markedly coarser than the feed sediment (mobile-bed armor), but markedly finer than the final surface size distribution with a constant flow equal to the average of the hydrograph.

27. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 27 A QUESTION In the case of the constant hydrograph of q w = 6 m 2 /s for the entire 30 days, and a sediment feed rate q bTf of 5x10 -5 m 2 /s, the bed equilibrated at a slope S = 0.00262. What would the feed rate have to be increased to in order for the bed to equilibrate at the same slope, when subjected to the full hydrograph? The answer can be found by trial and error. In performing the calculations, it proved necessary to change the time step from 1 day to 0.25 days in order to prevent numerical instability. The required sediment feed rate q bTf is 5.6x10 -4 m 2 /s, or 11.2 times higher than if the constant flow is used. This calculation illustrates how much more efficient hydrographs are at transporting sediment than equivalent constant flows.

28. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 28 SLOPE PROFILE AT FINAL EQUILIBRIUM WITH A HYDROGRAPH The final slope profile with the full hydrograph and a feed rate q bTf = 5.6x10 -4 m 2 /s shows variation at the upstream end. This variation represents the consequence of a sediment feed rate that does not vary with flow. In fact, the profile is a snapshot of the bed at the end of the last flow of the last hydrograph; at the end of the highest flow of the last hydrograph, the upstream slope would be below 0.00262. This cyclic time variation vanishes downstream of the third node.

29. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 29 A REMARKABLE TRADEOFF The figures of Slides 21, 22 and 28 reveal an interesting feature concerning the case of a cycled hydrograph (Parker, 2004). In the simulation with a hydrograph, the flow discharge varies according to the cycled hydrograph of Slide 14, but the sediment feed rate at the upstream is held constant over the hydrograph. When mobile-bed equilibrium (averaged over the hydrograph) is reached, at and near the upstream node (M = 1) the bed degrades and coarsens at the high flows of the hydrograph (when the sediment supply is insufficient) and aggrades and becomes finer at the low flows of the hydrograph (when the sediment supply is excessive). This feature is evident in Slide 28, where the bed slope at the upstream end of the reach is high at the end (low) flow of the hydrograph. Not far downstream of the feed point, however, a remarkable tradeoff is evident at mobile-bed equilibrium: the bed slope, bed elevation and surface grain size distribution become invariant with point on the hydrograph, but the bedload transport rate increases in magnitude and becomes coarser at the high flows, and decreases in magnitude and becomes finer at the lows flows. These features are evident in Slides 21, 22 and 28, and are illustrated in more detail in the next two slides.

30. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 30 A REMARKABLE TRADEOFF contd. Once mobile-bed equilibrium is reached (averaged over the hydrograph), bed slope S and surface grain size distribution (including geometric mean size D sg ) vary cyclically near the upstream end, but obtain constant values over the hydrograph everywhere else.

31. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 31 A REMARKABLE TRADEOFF contd. Once mobile-bed equilibrium is reached (averaged over the hydrograph), total bedload transport rate q bT and bedload geometric mean size D lg are constant over the hydrograph only in a short region near the feed point; farther downstream both increase at high flow and decrease at low flow.

32. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 32 CAVEAT! The calculations presented in this chapter are subject to some error. This is best explained in terms of the cyclic aggradation and degradation that occurs near the upstream end of the reach when mobile-bed equilibrium is reached. Formally, the program should store the grain size distribution of the bed material as it aggrades, and then access this same grain size distribution as it degrades. An execution of this step requires storage of the deposited substrate in memory. This has not been implemented in RTe-bookAgDegNormGravMixHyd.xls, largely because this storage would greatly slow the execution of a program that already takes a substantial amount of time to run from Excel. Instead, when the bed degrades the substrate is assumed to have the same size distribution as specified initially as input to the program (e.g. as shown Slide 9). While the above simplification introduces some modest error into the results, the qualitative results presented here are verified by a full model that does not employ the simplification.

33. 1D SEDIMENT TRANSPORT MORPHODYNAMICS with applications to RIVERS AND TURBIDITY CURRENTS © Gary Parker November, 2004 33 REFERENCES FOR CHAPTER 19 Parker, G., 1990, Surface-based bedload transport relation for gravel rivers. Journal of Hydraulic Research, 28(4): 417-436. Parker, G., 2004, Response of the gravel bed of a mountain river to a hydrograph. Proceedings, 2004 International Conference on Slopeland Disaster Mitigation, Taipei, Taiwan, October 5-6, 11 p; also downloadable at http://cee.uiuc.edu/people/parkerg/conference_reprints.htm.http://cee.uiuc.edu/people/parkerg/conference_reprints.htm