Model help:HydroTrend

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HydroTrend

Climate driven hydrological transport model

Model introduction

HydroTrend is an ANSI-standard C numerical model that creates synthetic river discharge and sediment load time series as a function of climate trends and basin morphology and has been used to study the sediment flux to a basin for basin filling models. As a drainage basin simulator, the model provides time series of daily discharge hydraulics at a river mouth, including the sediment load properties. HydroTrend was designed to provide input to lake or shelf circulation and sedimentation models ([1]; [2]), and study the impact of land-sea fluxes given climatic change scenarios ([3]; [4]). HydroTrend simulates the major processes that occur in a river basin, including:

  • Glacierized areas with advances and retreats depending on the climate scenario,
  • Snow accumulation in the winter and melt in the subsequent spring/summer,
  • Rainfall over the remaining portions of the basin with canopy evaporation,
  • Groundwater recharging and discharging,
  • The impact of reservoirs.

Model parameters

Parameter Description Unit
Input directory Determine if you want to use the "GUI" interface to provide input parameter values or use a text file with the input parameters by providing the location of the file on the server. [-]
Site prefix Part of the input and output file name e.g. the name of the geographic location, or project [-]
Case prefix Part of the input and output file name that provides you the opportunity to do different scenario simulations for e.g. the same location, or project [-]
Parameter Description Unit
Run duration Number of simulation time steps [years]
Parameter Description Unit
Starting mean annual temperature Mean annual temperature at the river mouth at the start of the simulation. (Notice: this is not a spatial average basin width parameter!) [°C]
Change in mean annual temperature The trend or change per year in the annual temperature [°C/year]
Standard deviation of mean annual temperature The standard deviation about the trend line that the annual temperatures will have. [°C]
Parameter Description Unit
Starting mean annual precipitation Annual total spatial river basin average precipitation rates for the beginning of the simulation [m/year]
change in mean annual precipitation The trend or change in the total annual precipitation [m/year/year]
Standard deviation of mean annual precipitation The standard deviation about the trend line that the annual precipitation will have. [m/year]
Parameter Description Unit
Lithology factor Sediment production varies with lithology, hard versus weak lithology: (0.5 - 3)[5]:
  • L=0.5 for basins comprised principally of hard, acid plutonic and/or high-grade metamorphic rocks.
  • L=0.75 for basins comprised of mixed, mostly hard lithology, sometimes including shield material.
  • L=1.0 for basins comprised of volcanic, mostly basaltic rocks, or carbonate outcrops, or mixture of hard and soft lithologies.
  • L=1.5 for basins characterized by a predominance of softer lithologies, but having a significant area of harder lithologies.
  • L=2 for fluvial systems draining a high proportion of sedimentary rocks, unconsolidated sedimentary cover, or alluvial deposits.
  • L=3 for basins having an abundance of exceptionally weak material, such as crushed rock, or loess deposits, or shifting sand dunes.
[-]
Anthropogenic facor Anthropogenic factor (0.3 - 8.0), disturbance to landscape [5]:
  • Eh = 0.3: for basins with a high density population (PD > 200 km2) and GNP/capita > $15K/y
  • Eh = 1.0: for basins with low human footprint (PD smaller than 50 km2)
  • Eh = 2.0 - 8.0: for basins with the high density population (PD > 200 km2) and GNP/capita is lower than $1K/y
[-]
Lapse rate The change in temperature per change in elevation. Parameter used to determine the snow - rain transition zone. [°C/km]
Starting ELA Glacier equilibrium line altitude is the long-term balance point along a glacier. The ELA is where the amount of accumulated snow and ablated water are equal. [m]
Change in ELA Is the linear change per year of the equilibrium line altitude due to a shift in the climate. [m/year]
Dry precipitation (nival and ice) evaporation fraction The percentage of the dry precipitation (nival&ice) which will be evaporated. [-]
River length The length of the main stem of the river to determine the lag time before water reaches the river outlet. [km]
Mean volume of reservoir If the reservoir capacity is more than 0.5km3, Trap Efficiency (TEbasin) will be calculated based by: (TEbasin = 1.0 - (0.05 / exp(Rvol/RQbar)0.5, where Rvol = Reservoir volume and RQbar = the mean inflow discharge)[6].
If the reservoir capacity is less than 0.5km3, (TEbasin = ( 1.0 - (1.0 / (1 + 0.0021 *D * ((Rvol * 1e9) / Rarea)))) where Rvol = Reservoir volume and Rarea (km2) = drainage area above the Reservoir) and D, set to 0.1, represents the reservoir characteristics [7].
[km3]
Drainage area of reservoir The upstream area of the river basin that drains into the reservoir. [km2]
Parameter Description Unit
k River mouth velocity coefficient (Where: v=k*Qm, w=a*Qb, d=c*Qf and the discharge: Q=w*v*d.
Therefore: a*c*k = 1 and b+m+f = 1) [8].
[m/s]
m River mouth velocity exponent (Where: v=k*Qm, w=a*Qb, d=c*Qf and the discharge: Q=w*v*d.
Therefore: a*c*k = 1 and b+m+f = 1) [8].
[-]
a River mouth width coefficient (Where: v=k*Qm, w=a*Qb, d=c*Qf and the discharge: Q=w*v*d.
Therefore: a*c*k = 1 and b+m+f = 1) [8].
[m]
b River mouth width exponent (Where: v=k*Qm, w=a*Qb, d=c*Qf and the discharge: Q=w*v*d.
Therefore: a*c*k = 1 and b+m+f = 1) [8].
[-]
Average river mouth velocity The average stream velocity, used in the model to determine the flow routing [m/s]
Constant annual baseflow Defines the constant annual baseflow which occurs in the basin. This is analogous to a deep groundwater pool. Baseflow should be bigger than 0 and smaller than the total precipitation discharge. [m3/s]
Trapping efficiency Deltaic area typically trap sediment e.g. due to the low slope angle of the area. The fraction of deltaic trapping (0 - 1) can be provided here. [-]
Delta gradient Delta gradient determines the slope of the riverbed that determines the amount of bedload reaching the river mouth. [m/m]
Parameter Description Unit
Maximum groundwater storage Maximum capacity spacial averaged shallow ground water pole of the drainage basin [m3]
Minimum groundwater storage Minimum capacity spacial averaged shallow ground water pole of the drainage basin [m3]
Initial groundwater storage Spatial averaged shallow ground water pole of the drainage basin at the start of the simulation. [m3]
Groundwater coefficient The shallow groundwater (sub-surface storm flow) coefficient is used in draining the groundwater pool to the river. [m3]
Groundwater exponent The shallow groundwater (sub-surface storm flow) exponent is used in draining the groundwater pool to the river. [-]
Ksat Saturated hydraulic conductivity describes water movement through saturated media. See table for saturated hydraulic conductivity values in relation to texture. [mm/day]
Parameter Description Unit
Output directory The location where the output files will be stored. [-]
Interval between output files Specify how often you want output to be written. Notice: files will be really large if you choose to save every timestep. [-]
Mean Velocity file [-]
Mean Width file [-]
Mean Depth file [-]
Mean Water Discharge file [-]
Mean Sediment Discharge file [-]
Mean Bedload Flux file [-]

Uses ports

This will be something that the CSDMS facility will add

Provides ports

This will be something that the CSDMS facility will add

Main equations

Q = Qr + Qn + Qice - QEv ± Qg = Water discharge at the river mouth [m3/s] (1)
Qs = ω B Q0.31 A0.5 R T for T ≥ 2 °C = Long-term suspended sediment load at the river mouth [kg/s] [5] (2a) or
Qs = 2ω B Q0.31 A0.5 R for T < 2 °C = Long-term suspended sediment load at the river mouth [kg/s] [5] (2b)
B = L (1 - TE) Eh = Expression that capture the importance of geology and human factors. [5] (3)
(Qs[i] / Qs) = ψ[i] (Q[i] / Q)Ca = Daily suspended sediment load at the river mouth [kg/s] [9] (4)
Qb[i] = (ρs / ρs - ρ) * (ρ g Q[i]β S eb) / (g tan λ) when u ≥ ucr = Daily bedload at the river mouth [kg/s] [10] (5)


Nomenclature

Symbol Description Unit
Q Long-term water discharge [m3/s]
Qr Water discharge generated by rainfall [m3/s]
Qn Water discharge generated by nival melt [m3/s]
Qice Water discharge generated by glacier melt [m3/s]
QEv Water discharge loss by evapo-transpiration processes [m3/s]
Qg Water discharge loss or generated by ground water [m3/s]
Qs Long-term suspended sediment load (30yrs or longer) [kg/s]
ω Constant, (0.02) [-]
A Drainage basin area [km2]
R Drainage basin relief [km]
T Drainage basin temporal and spatial mean temperature [°C]
L Lithology factor [-]
TE Trapping efficiency of reservoirs / lakes [-]
Eh Anthropogenic factor [-]
Qs[i] Daily suspended sediment load [kg/s]
Ψ[i] Daily random variable with a log-normal distribution [-]
Q[i] Daily water discharge [m3/s]
Ca Annual rating term coefficient with a normal distrbution [-]
Qb[i] Daily bedload [kg/s]
ρs Sand density [kg/m3]
ρ Fluid density [kg/m3]
g Acceleration due to gravity [m/s2]
β Bedload rating term [-]
S Slope of the riverbed [m/m]
eb Bedload efficiency [-]
λ Limiting angle of response of sediment grains lying on the river bed [-]
u Stream velocity [m/s]
ucr Critical stream velocity [m/s]

Notes

Any notes, comments, you want to share with the user

Numerical scheme


Examples

An example run with input parameters, BLD files, as well as a figure / movie of the output

Follow the next steps to include images / movies of simulations:

See also: Help:Images or Help:Movies

Developer(s)

Albert Kettner

Key HydroTrend Papers

  • Kettner, A.J., and Syvitski, J.P.M., 2008. HydroTrend version 3.0: a Climate-Driven Hydrological Transport Model that Simulates Discharge and Sediment Load leaving a River System. Computers & Geosciences, 34(10), 1170-1183, doi:10.1016/j.cageo.2008.02.008.
  • Syvitski, J.P.M., Morehead, M.D. and Nicholson, M., 1998. HYDROTREND: A Climate-driven Hydrologic-Transport Model for Predicting Discharge and Sediment Loads to Lakes or Oceans. Computers & Geosciences, 24(1), 51-68, doi:10.1016/S0098-3004(97)00083-6.
  • Syvitski, J.P.M., and J.M. Alcott, 1995. RIVER3: Simulation of River Discharge and Sediment Transport. Computers and Geosciences, 21(1), 89-101, doi:10.1016/0098-3004(94)00062-Y.

References

  1. Steckler, M., Swift, D., Syvitski, J., Goff, J., and Niedoroda, A., 1996. Modeling the sedimentology and stratigraphy of continental margins. Oceanography, 9, 183-188. [pdf]
  2. Syvitski, J.P.M., and Alcott, J.M., 1995. DELTA6: Numerical simulation of basin sedimentation affected by slope failure and debris flow runout. In Proceedings of the Pierre Beghin International Workshop on Rapid Gravitational Mass Movements, pp. 180-195. 6-10 December, 1993, Grenoble, France.
  3. Moore, R.D., 1992. Hydrological responses to climatic variations in a glacierized watershed: inferences from a conceptual streamflow model. In Using Hydrometric Data to Detect and Monitor Climate Change, Proceedings NHRI Symposium, No. 8, April (1991), pp. 9-20, NHRI Saskatoon.
  4. Syvitski, J.P.M., and Andrews, J.T., 1994. Climate change: numerical modelling of sedimentation and coastal processes, eastern Canadian Arctic. Arctic and Alpine research, 26, 199-212.
  5. 5.0 5.1 5.2 5.3 5.4 Syvitski, J.P.M. and Milliman, J.D., 2007, Geology, geography and humans battle for dominance over the delivery of sediment to the coastal ocean. J. Geology 115, 1–19. dio:10.1086/509246
  6. Vörösmarty, C.J., Meybeck, M., Fekete, B., and Sharma, K. (1997) The potential of neo-Castorization on sediment transport by the global network of rivers. Human Impact on Erosion and Sedimentation, IAHS, 245, 261-273.
  7. Verstraeten G., and Poesen, J. (2000) Estimating trap efficiency of small reservoirs and ponds: methods and implications for the assessment of sediment yield. Progress in Physical Geography, 24, 219-251. dio:10.1177/030913330002400204
  8. 8.0 8.1 8.2 8.3 Leopold, L.B. and T. Maddock, 1953. “The Hydraulic Geometry of Stream Channels and Some Physiographic Implications”, U.S. Geological Survey Professional Paper 252.
  9. Morehead, M.D., Syvitski, J.P.M., Hutton, E.W.H., Peckham, S.D., 2003. Modeling the temporal variability in the flux of sediment from ungauged river basins. Global and Planetary Change, 39, 95-110. dio:10.1016/S0921-8181(03)00019-5
  10. Bagnold, R.A., 1966. An approach to the sediment transport problem from general physics. US Geological Survey Professional Paper, 422, 1-37.

Links

Model:HydroTrend