@article {50403, title = {A bed-load transport model for rough turbulent open-channel flows on plane beds}, journal = {Earth Surface Processes and Landforms}, volume = {31}, year = {2006}, note = {//NMSU//LTER IV//entered 7/12/2006}, month = {2006}, pages = {910-928}, abstract = {

Data from flume studies are used to develop a model for predicting bed-load transport rates in rough turbulent two-dimensional open-channel flows moving well sorted non-cohesive sediments over plane mobile beds. The object is not to predict transport rates in natural channel flows but rather to provide a standard against which measured bed-load transport rates influenced by factors such as bed forms, bed armouring, or limited sediment availability may be compared in order to assess the impact of these factors on bed-load transport rates. The model is based on a revised version of Bagnold{\textquoteright}s basic energy equation ibsb = eb{\`u}, where ib is the immersed bed-load transport rate, {\`u} is flow power per unit area, eb is the efficiency coefficient, and sb is the stress coefficient defined as the ratio of the tangential bed shear stress caused by grain collisions and fluid drag to the immersed weight of the bed load. Expressions are developed for sb and eb in terms of G, a normalized measure of sediment transport stage, and these expressions are substituted into the revised energy equation to obtain the bed-load transport equation ib = {\`u} G 3{\textperiodcentered}4. This equation applies regardless of the mode of bed-load transport (i.e. saltation or sheet flow) and reduces to ib = {\`u} where G approaches 1 in the sheet-flow regime. That ib = {\`u} does not mean that all the available power is dissipated in transporting the bed load. Rather, it reflects the fact that ib is a transport rate that must be multiplied by sb to become a work rate before it can be compared with {\`u}. It follows that the proportion of {\`u} that is dissipated in the transport of bed load is ibsb/{\`u}, which is approximately 0{\textperiodcentered}6 when ib = {\`u}. It is suggested that this remarkably high transport efficiency is achieved in sheet flow (1) because the ratio of grain-to-grain to grain-to-bed collisions increases with bed shear stress, and (2) because on average much more momentum is lost in a grain-to-bed collision than in a grain-to-grain one. Copyright {\textcopyright} 2006 John Wiley \& Sons, Ltd.

}, keywords = {article, hydrology, bed-load transport, hydrology, saltation, hydrology, sediment transport, hydrology, sheet flow, journal, model, model, bed-load transport, model, hydrology}, doi = {10.1002/esp.1300}, url = {files/bibliography/JRN00434.pdf}, author = {Athol D. Abrahams and Gao, Peng} } @inbook {50402, title = {Biogeochemical fluxes across piedmont slopes of the Jornada Basin}, booktitle = {Structure and Function of a Chihuahuan Desert Ecosystem. The Jornada Basin Long-Term Ecological Research Site}, year = {2006}, month = {July 1, 2006}, pages = {150-175}, publisher = {Oxford University Press}, organization = {Oxford University Press}, chapter = {Chapter 7}, address = {New York}, abstract = {This chapter is an overview of recent studies of the movement of water, sediment, and nutrients across a principle piedmont slope, or bajada, of the Jornada Basin. Bajadas are extensive, gently sloping surfaces formed by the coalescence of alluvial fans and are a major landscape component of the basin and range province. During the past four decades a considerable body of research has elucidated the form and function of alluvial fans (Bull 1977; Blair and McPherson 1994; Harvey 1997), but less attention has been paid to bajadas. In particular, the bajadas most neglected are those where channels converge and diverge at irregular intervals downslope. This type of bajada is found at the base of Summerford Mountain, the northernmost peak of the Dona Ana Mountains on the western edge of the Jornada Basin. For convenience, this bajada is hereafter referred to as the Summerford bajada. The research has involved rainfall simulation experiments on small plots, monitoring of two small watersheds on this bajada, and computer modeling of the processes operating in these watersheds and over the bajada as a whole. A detailed understanding of the hydrology and hydraulics of overland flow on this bajada requires a numerical model of the rainfall-runoff process. The objective of this chapter is to detail the model and draw conclusions from model simulations about hydrologic transports of sediment and nutrients across this bajada. Since these piedmonts are important surfaces in this desert an understanding of their hydrologic and biogeochemical dynamics is crucial to understanding landscape dynamics in the basin and throughout arid regions.}, keywords = {alluvial, bajada, biogeochemical, coalescence, fluxes, movement, nutrients, piedmont, sediment, slopes, water}, url = {/files/bibliography/06-058.pdf}, author = {Athol D. Abrahams and Melissa Neave and W. H. Schlesinger and John Wainwright and David A. Howes and A.J. Parsons}, editor = {Kris Havstad and L. Huenneke and W. H. Schlesinger} } @article {50735, title = {Bed-load transport equation for sheet flow}, journal = {Journal of Hydrologic Engineering}, volume = {129}, number = {2}, year = {2003}, note = {//NONE//LTER IV//added 6/29/2005; updated 8/8/2006}, month = {2003}, pages = {159-163}, abstract = {

When open-channel flows become sufficiently powerful, the mode of bed-load transport changes from saltation to sheet flow. Where there is no suspended sediment, sheet flow consists of a layer of colliding grains whose basal concentration approaches that of the stationary bed. These collisions give rise to a dispersive stress that acts normal to the bed and supports the bed load. An equation for predicting the rate of bed-load transport in sheet flow is developed from an analysis of 55 flume and closed conduit experiments. The equation is i(b) = omega where i(b) = immersed bed-load transport rate; and omega = flow power. That i(b) = omega implies that e(b) = tan alpha = u(b)/u, where e(b) = Bagnold{\textquoteright}s bed-load transport efficiency; u(b) = Mean grain velocity in the sheet-flow layer; and tan alpha = dynamic internal friction coefficient. Given that tan alpha approximate to 0.6 for natural sand, u(b) approximate to 0.6u, and e(b)approximate to 0.6. This finding is confirmed by an independent analysis of the experimental data. The value of 0.60 for e(b) is much larger than the value of 0.12 calculated by Bagnold, indicating that sheet flow is a much more efficient mode of bed-load transport than previously thought.

}, keywords = {article, geomorphology, bedload transport, geomorphology, sheet flow, hydrology, bedload, hydrology, channels, hydrology, processes, hydrology, sediment transport, hydrology, sheet flow, journal, model, bedload transport rate, model, hydrology}, isbn = {0733-9429/2003/2-159-163}, doi = {10.1061/(ASCE)0733-9429(2003)129:2(159)}, url = {files/bibliography/JRN00378.pdf}, author = {Athol D. Abrahams} } @article {50736, title = {Disposition of rainwater under creosotebush}, journal = {Hydrological Processes}, volume = {17}, year = {2003}, note = {//NMSU//LTER IV//}, month = {2003}, pages = {2555-2566}, abstract = {

In desert shrubland ecosystems water and nutrients re concentrated beneath shrub canopies in {\textquoteright}resource islands{\textquoteright}. Rain falling onto these islands reaches the ground as either stemflow or throughfall and then either infiltrates into the soil or runs off as overland flow. This study investigates the partitioning of rainwater between stemflow and throughfall in the first instance and between infiltration and runoff in the second. Two series of 40 rainfall simulation experiments were performed on 16 creosotebush shrubs in the Jornada Basin, New Mexico. The first series of experiments was designed to measure the surface runoff and was performed with each shrub in its growth position. The second series was designed to measure stemflow reaching the shrub base and was conducted with the shrub suspended above the ground. The experimental data show that once equilibrium is achieved, 16\% of the rainfall intercepted by the canopy or 6.7\% of the rain falling inside the shrub area (i.e., the area inside the shrubs circumscribing ellipse) is funneled to the shrub base as stemflow. This redistribution of the rainfall by stemflow is a function of the ratio of canopy area (i.e., the area covered by the shrub canopy) to collar area (i.e., a circular area centered on the shrub base), with stemflow rate being positively correlated and throughfall rate being negatively correlated with this ration. The surface runoff rate expressed as a proportion of the rate at which rainwater arrives at a point (i.e., stemflow rate plus throughfall rate) is the runoff coefficient. A multiple regression reveals that 75\% of the variance in the runoff coefficient can be explained by three independent variables: the rainfall rate, the ratio of the canopy area to the collar area, and the presence or absence of subcanopy vegetation. Although the last variable is a dummy variable, it accounts for 66.4\% of the variance in the runoff coefficient. This suggests that the density and extent of the subcanopy vegetation is the single most important control of the partitioning of rainwater between runoff and infiltration beneath creosotebush. Although these findings pertain to creosotebush, similar findings might be expected for other desert shrubs that generate significant stemflow and have subcanopy vegetation. Copyright {\textcopyright} 2003 John Wiley \& Sons, Ltd.

}, keywords = {article, articles, creosotebush, hydrology, creosotebush,also SEE , hydrology, creosotebush, hydrology, infiltration, hydrology, overland flow, hydrology, resource islands, hydrology, stemflow, journal, journals, rainfall simulation, hydrology, rainwater, resource islands, hydrology}, doi = {10.1002/hyp.1272}, url = {files/bibliography/JRN00382.pdf}, author = {Athol D. Abrahams and A.J. Parsons and John Wainwright} } @article {50957, title = {A sediment transport equation for interrill overland flow on rough surfaces}, journal = {Earth Surface Processes and Landforms}, volume = {26}, year = {2001}, note = {//NONE//LTER IV//}, month = {2001}, pages = {1443-1459}, abstract = {

A model for predicting the sediment transport capacity of turbulent interrill flow on rough sur4faces is developed from 1295 flume experiments with flow depths ranging from 3.4 to 43.4 mm, flow velocities from 0.09 to 0.65 m s-1, Reynolds numbers from 5000 to 26949, Froude numbers from 0.23 to 2.93, bed slopes from 2.7{\textdegree} to 10{\textdegree}, sediment diameters from 0.098 to 1.16 mm, volumetric sediment concentrations from 0.002 to 0.304, roughness concentrations from 0 to 0.57, roughness diameters from 1.0 to 91.3 mm, rainfall intensities from 0 to 159 mm h-1, flow densities from 1002 to 1501 kg m-3, and flow kinematic viscosities from 0.913 to 2.556 x 10-6 m2 s-1. Stones, cylinders and miniature ornamental trees are used as roughness elements. Given the diverse shapes, sizes and concentrations of these elements, the transport model is likely to apply to a wide range of ground surface morphologies. Using dimensional analysis, a total-load transpot equation is developed for open-channel flows, and this equation is shown to apply to interrill flows both with and without rainfall. The euation indicates that the dimensionless sediment transport rate {\O} is a function of, and therefore can be predicted by, the dimensionless shear stress {\`e}, its critical value {\`e}c, the resistance coefficient u/u*, the inertial settling velocity of the sediment wi, the roughness concentration Cr, and the roughness diameter Dr. Testing reveals that the model gives good unbiased predictions of {\O} in flows with sediment concentrations less than 0.20. FLows with higher concentrations appear to be hyperconcentrated and to have sediment transport rates higher than those predicted by the model. Copyright {\textcopyright} 2001 John Wiley \& Sons, Ltd.

}, keywords = {article, articles, hydrology, bedload, hydrology, hillslopes, hydrology, interrill flow, hydrology, overland flow, hydrology, sediment transport, hydrology, soil erosion, journal, journals, model, hydrology, model, interrill overland flow, model, sediment transport}, doi = {10.1002/esp.286}, url = {files/bibliography/JRN00317.pdf}, author = {Athol D. Abrahams and Gary Li and Krishnan, Chitra and Atkinson, Joseph F.} } @article {51202, title = {Predicting sediment transport by interrill overland flow on rough surfaces}, journal = {Earth Surface Processes and Landforms}, volume = {23}, year = {1998}, note = {//NONE//LTER III//}, month = {1998}, pages = {481-492}, abstract = {

Modeling soil erosion requires an equation for predicting the sediment transport capacity by interrill overland flow on rough surfaces. The conventional practice of partitioning total shear stress into grain and form shear stress and predicting transport capacity using grain shear stress lacks rigor and is prone to underestimation. This study therefore explores the possibility that inasmuch as surface roughness affects flow hydraulic variables which, in turn, determine transport capacity, there may be one or more hydraulic variables which capture the effect of surface roughness on transport capacity sufficiently well for good predictions of transport capacity to be achieved from data on these variables alone. To investigate this possibility, regression analyses were performed on data from 1506 flume experiments in which discharge, slope, water temperature, rainfall intensity, and roughness size, shape and concentration were varied. The analyses reveal that 89.8 per cent of the variance in transport capacity can be accounted for by excess flow power and flow depth. Including roughness size and concentration in the regression improves that explained variance by only 3.5 per cent. Evidently, flow depth, when used in combination with excess flow power, largely captures the effect of surface roughness on transport capacity. This finding promises to simplify greatly the task of developing a general sediment transport equation for interrill overland flow on rough surfaces. {\textcopyright}1998 John Wiley \& Sons, Ltd.

}, keywords = {article, articles, hydrology, model, hydrology, sediment transport, journal, journals, model,sediment yields}, doi = {10.1002/(SICI)1096-9837(199812)23:12<1087::AID-ESP934>3.0.CO;2-4}, url = {files/bibliography/JRN00261.pdf}, author = {Athol D. Abrahams and Gary Li and Krishnan, Chitra and Atkinson, Joseph F.} }